Australian National University
crystallisation age close to emplacement age of the tuffaceous unit
Note: this interpretation prohibits zircon ages as the eruption age.
Branxton Formation
Tuffaceous siltstone within the lower Branxton Formation. Roberts et al 1996 paraphrased "Sample Z2015 from the Branxton Formation, taken at a depth of 558.5 m in Southland Kalingo DDH 18 at GR 354572 near Ellalong, NSW, comes from brown to buff tuffaceous siltstone 12 m above the top of the Greta Seam, the uppermost seam in the Greta Coal Measures in that part of the Lochinvar Anticline. Zircons in the sample are two morphological types, a dominant (~85%) group of euhedral grains whose surfaces have a mottled appearance suggesting corrosion, and a subordinate group of clear euhedral grains with no surface mottling."
Southland Kalingo DDH 18
Roberts, J., Claoué-Long, J. C. & Foster, C. B. (1996). SHRIMP zircon dating of the Permian System of eastern Australia. Australian Journal of Earth Sciences 43(4), 401-421.

laser ablation: New Wave UP-213 Nd:YAG laser probe
University of Newcastle, Australia
Louth Volcanics
Silty volcanogenic sandstone. Dwyer et al 2018 paraphrased: "Tuffs and intrusive calc-alkaline dolerites exist within drill holes MINOL33, MINOL30 and MINOL21, which are located within the geophysical anomaly associated with the Louth Volcanics. In associated tuffs, sedimentary rocks and field samples, bedding parallel and axial planar fabrics were observed (MINOL21-05, MINOL30-04, MINOL33-06, RDT7)."
State or NT agency supplied location, method unknown
Dwyer R.C., Collins W.J., Hack A.C., Hegarty R. & Huang H. (2018) Age and tectonic significance of the Louth Volcanics: implications for the evolution of the Tasmanides of eastern Australia., Australian Journal of Earth Sciences 65, 1049-1069.

Queensland University of Technology
youngest mean age populations of detrital zircons
Bondonga beds
Campbell et al. 2015 paraphrased: "Diamictites in the Bondonga beds have a mudstone matrix, and are clast-rich to clast-poor; consisting of subangular to well-rounded pebbles and cobbles of silicified sandstone, chert, volcanic and pyroclastic rocks. Both matrix- and clast-supported conglomerates were observed. Clast-supported conglomerates occur as massive outcrop exposures within the Bondonga beds, whereas matrix-supported conglomerates are poorly sorted and commonly interbedded with sandstones. Clasts range from 5 cm to 20 cm in length, and are sub-rounded to rounded pebble and cobbles of silicified sandstone, chert, volcanic rocks and pyroclastic rocks within a sandy matrix."
State or NT agency supplied location, method unknown
Campbell M., Rosenbaum G., Shaanan U., Fielding C. R. & Allen C. (2015). The tectonic significance of lower Permian successions in the Texas Orocline (Eastern Australia). Australian Journal of Earth Sciences 62(7), 789-806.

Queensland University of Technology
youngest mean age populations of detrital zircons
Bondonga beds
Campbell et al. 2015 paraphrased: "Diamictites in the Bondonga beds have a mudstone matrix, and are clast-rich to clast-poor, consisting of subangular to well-rounded pebbles and cobbles of silicified sandstone, chert, volcanic and pyroclastic rocks. Both matrix- and clast-supported conglomerates were observed. Clast-supported conglomerates occur as massive outcrop exposures within the Bondonga beds, whereas matrix-supported conglomerates are poorly sorted and commonly interbedded with sandstones. Clasts range from 5 cm to 20 cm in length, and are sub-rounded to rounded pebble and cobbles of silicified sandstone, chert, volcanic rocks and pyroclastic rocks within a sandy matrix."
Campbell M., Rosenbaum G., Shaanan U., Fielding C. R. & Allen C. (2015). The tectonic significance of lower Permian successions in the Texas Orocline (Eastern Australia). Australian Journal of Earth Sciences 62(7), 789-806.

Queensland University of Technology
youngest mean age populations of detrital zircons
Terrica beds
Campbell et al. 2015 paraphrased: "The Texas Orocline is a prominent orogenic curvature that developed during the early Permian in the southern New England Orogen. The exposures of lower Permian sedimentary successions in the vicinity of the Texas Orocline (Silver Spur, Bondonga, Pikedale, Terrica, Alum Rock and Ashford beds) approximately trace the oroclinal structure. The Silver Spur, Terrica and Alum Rock beds unconformably overlie and/or are faulted against the accretionary complex rocks of the Texas beds (Olgers et al. 1974). Clasts of chert, sandstone and volcanic rocks in the Terrica, Silver Spur and Alum Rock beds are thought to be derived from the Carboniferous Texas beds (Olgers et al. 1974). "
Campbell M., Rosenbaum G., Shaanan U., Fielding C. R. & Allen C. (2015). The tectonic significance of lower Permian successions in the Texas Orocline (Eastern Australia). Australian Journal of Earth Sciences 62(7), 789-806.

Pikedale beds
Campbell et al. 2015 paraphrased: "The Texas Orocline is a prominent orogenic curvature that developed during the early Permian in the southern New England Orogen. The Pikedale beds are lower Permian sedimentry successions which outline the Texas oroclinal structure. It was once part of a single larger basin (encompasing the Bondonga, Silver Spur, Pikedale, Terrica, Alum Rock and Ashford beds). There is an unkown but assumped fault contact with the underlying Texas beds. The sample is a sandstone extracted from the Pikedale Beds devired from the Texas Carboniferious felsic volcanics (84%) predominantly sourced proximally from within the southern New England Orogen.

Silver Spur beds
Campbell et al. 2015 paraphrased: "The Texas Orocline is a prominent orogenic curvature that developed during the early Permian in the southern New England Orogen. The exposures of lower Permian sedimentary successions in the vicinity of the Texas Orocline (Silver Spur, Bondonga, Pikedale, Terrica, Alum Rock and Ashford beds) approximately trace the oroclinal structure. The Silver Spur, Terrica and Alum Rock beds unconformably overlie and/or are faulted against the accretionary complex rocks of the Texas beds (Olgers et al. 1974). Clasts of chert, sandstone and volcanic rocks in the Terrica, Silver Spur and Alum Rock beds are thought to be derived from the Carboniferous Texas beds (Olgers et al. 1974). "
State or NT agency supplied location, method unknown

Bondonga beds
Campbell et al. 2015 paraphrased: "Diamictites in the Bondonga beds have a mudstone matrix, and are clast-rich to clast-poor, consisting of subangular to well-rounded pebbles and cobbles of silicified sandstone, chert, volcanic and pyroclastic rocks. Both matrix- and clast-supported conglomerates were observed. Clast-supported conglomerates occur as massive outcrop exposures within the Bondonga beds, whereas matrix-supported conglomerates are poorly sorted and commonly interbedded with sandstones. Clasts range from 5 cm to 20 cm in length, and are sub-rounded to rounded pebble and cobbles of silicified sandstone, chert, volcanic rocks and pyroclastic rocks within a sandy matrix."

laser ablation: New Wave UP-213 Nd:YAG laser probe
University of Newcastle, Australia
Louth Volcanics
Getty Gabbro
Volcanogenic conglomeratic sandstone. Dwyer et al 2018 parphrased: "Sample GETTY5/6-1-02 was found within an alkaline breccia sequence but only returned discordant Permo-Triassic ages. Provenance signals are similar to samples from Louth and the NLO and include Devonian to Carboniferous ages suggesting incorporation of detrital components from the Lower Devonian Louth Volcanics and the Winduck/Mulga Downs Groups."
Dwyer R.C., Collins W.J., Hack A.C., Hegarty R. & Huang H. (2018) Age and tectonic significance of the Louth Volcanics: implications for the evolution of the Tasmanides of eastern Australia., Australian Journal of Earth Sciences 65, 1049-1069.

laser ablation: New Wave UP-213 Nd:YAG laser probe
University of Newcastle, Australia
Louth Volcanics
Tuffaceous siltstone
Dwyer R.C., Collins W.J., Hack A.C., Hegarty R. & Huang H. (2018) Age and tectonic significance of the Louth Volcanics: implications for the evolution of the Tasmanides of eastern Australia., Australian Journal of Earth Sciences 65, 1049-1069.

Geoscience Australia
Inserted from Geochron Delivery (Geoscience Australia; http://www.ga.gov.au/geochron-sapub-web/), 26 November 2021
South Nicholson Group
Brown-green-white medium-grained sandstone with coarser pebbly lags and fine mud and silty intervals, with thin to thick discontinuous laminae of glauconite. Preserved soft sediment deformation, dewatering structures and rip up clasts of all types, and syneresis cracks throughout. Minerals present: clay minerals, quartz, calcite, glauconite.
Kositcin, N., Cross, A.J., Clark, A.D., Doublier, M.P., Fraser, G.L., Schofield, A., 2022. Geological framework of the concealed East Tennant area constrained by SHRIMP U-Pb zircon geochronology: Implications for Paleoproterozoic stratigraphic correlations in northern Australia. Precambrian Research, 383, 106886, 22p.

Geoscience Australia
Inserted from Geochron Delivery (Geoscience Australia; http://www.ga.gov.au/geochron-sapub-web/), 26 November 2021
South Nicholson Group
This sample is a poorly to moderately sorted, fine- to medium-grained quartzitic sandstone, comprising angular to rounded grains (sub-arkosic sandstone). The sample constituents include framework grains (70%), matrix (15%) and cement (15%). Cement is present as fine-grained white mica, with abundant hematite. Bedding is weakly defined by the fine-grained layers (2-5 mm) with a higher content of white mica. Quartz is the dominant mineral among the framework grains, with minor feldspar and lithic fragments. Feldspar grains are strongly altered by sericite and hematite. Lithic fragments were likely sourced from granitic rocks with a biotite-feldspar-quartz composition. The sample experienced low grade metamorphism and brittle fracturing.
Kositcin, N., Cross, A.J., Clark, A.D., Doublier, M.P., Fraser, G.L., Schofield, A., 2022. Geological framework of the concealed East Tennant area constrained by SHRIMP U-Pb zircon geochronology: Implications for Paleoproterozoic stratigraphic correlations in northern Australia. Precambrian Research, 383, 106886, 22p.

laser ablation: 193 nm ArF excimer laser
University of Tasmania
Bluff Quartzite
Rocky Cape Region
~800m SE of Bluff Hill Point
Halpin, J.A., Jensen, T., McGoldrick, P., Meffre, S., Berry, R.F., Everard, J.L., Calver, C.R., Thompson, J., Goemann, K., Whittaker, J.M., 2014. Authigenic monazite and detrital zircon dating from the Proterozoic Rocky Cape Group, Tasmania: Links to the Belt-Purcell Supergroup, North America. Precambrian Research, 250, 50-67.

laser ablation: 193 nm ArF excimer laser
University of Tasmania
Looneys Flat Siltstone
Rocky Cape Region
Jensen, T.L., 2011, Geochronology and geochemistry of some Horodyskia-bearing shales, NW Tasmania. University of Tasmania. Centre for Ore Deposit and Exploration Studies. B.Sc. Hons Thesis, 91pp.

laser ablation: 193 nm ArF excimer laser
University of Tasmania
Looneys Flat Siltstone
Rocky Cape Region
Halpin, J.A., Jensen, T., McGoldrick, P., Meffre, S., Berry, R.F., Everard, J.L., Calver, C.R., Thompson, J., Goemann, K., Whittaker, J.M., 2014. Authigenic monazite and detrital zircon dating from the Proterozoic Rocky Cape Group, Tasmania: Links to the Belt-Purcell Supergroup, North America. Precambrian Research, 250, 50-67.

Lagoon River Quartzite
Halpin, J.A., Jensen, T., McGoldrick, P., Meffre, S., Berry, R.F., Everard, J.L., Calver, C.R., Thompson, J., Goemann, K., Whittaker, J.M., 2014. Authigenic monazite and detrital zircon dating from the Proterozoic Rocky Cape Group, Tasmania: Links to the Belt-Purcell Supergroup, North America. Precambrian Research, 250, 50-67.

Irby Siltstone
Newhaven Rd cutting via Montumana

Cassiterite Creek Quartzite
CCQTZ
Jensen, T.L., 2011, Geochronology and geochemistry of some Horodyskia-bearing shales, NW Tasmania. University of Tasmania. Centre for Ore Deposit and Exploration Studies. B.Sc. Hons Thesis, 91pp.

Additional analysis of Jensen (2011) CCQTZ sample ID
Cassiterite Creek Quartzite
CCQTZ

Geoscience Australia
Inserted from Geochron Delivery (Geoscience Australia; http://www.ga.gov.au/geochron-sapub-web/), 26 November 2021
South Nicholson Group
This interval is a light pink, medium- to coarse-grained sandstone, with discrete (up to ~1 cm thick) very coarse-grained to pebbly layers, that, in places define cross bedding. Texturally immature feldspathic and micaceous, sub-lithic poorly sorted, sub-angular medium- to coarse-grained sandstone. Large low-angle trough cross bed sets indicate a high-energy environment, with the texturally immature and highly lithic nature of the member suggesting rapid sedimentation. The rock comprises sub-angular to sub-spherical, gravel- to pebble-sized clasts of quartz (60%), K-feldspar (20%), granitoids (15%) and other lithic fragments, including schists (5%), in a ferruginous matrix comprising quartz, K-feldspar, muscovite, silica, and hematite.
Kositcin, N., Cross, A.J., Clark, A.D., Doublier, M.P., Fraser, G.L., Schofield, A., 2022. Geological framework of the concealed East Tennant area constrained by SHRIMP U-Pb zircon geochronology: Implications for Paleoproterozoic stratigraphic correlations in northern Australia. Precambrian Research, 383, 106886, 22p.

Alroy Formation
The sample is a medium- to coarse-grained feldspar-biotite gneiss, with well-developed weak compositional banding, defined by melanosomes, leucosomes and transitional bands. The melanosomes (restite) are dominated by biotite, with minor K-feldspar and white mica. The leucosomes comprise quartz, altered and fresh feldspar, with minor biotite and white mica. The transitional bands have an intermediate composition, with semi-equal amounts of melanocratic and leucocratic components. The contacts between the bands are gradual. Micas show preferential orientation developed along the compositional banding. Accessory phases include titanite, ilmenite, apatite and zircon. Trace amounts of sillimanite occur as fibrolite aggregates in quartz. The rock experienced deformation synchronous to the metamorphism and partial melting, as evidenced by the flow foliation and symplectite reaction textures. This gneiss was intruded by granite (sample 7419715/NDIBK10.004) and quartz-feldspar-muscovite pegmatite. Hematite and sericite alteration occurs throughout the unit.

This interval is a clean, pink to cream coloured crossbedded sandstone, likely deposited in a high energy environment. It is a medium- to thickly-bedded, fine- to coarse-grained, quartz to lithic sandstone, with minor interbeds of pebble or cobble conglomerate and siltstone. The sample selected for geochronology is a cream coloured, medium-grained, silicified quartz-rich sandstone. It is moderately- to well-sorted, with sub-round to round quartz grains.

Alroy Formation
The sample is a fine- to medium-grained, laminated, tuffaceous rock. The groundmass is dominated by chlorite and sericite, with minor quartz and feldspar. The pyroclastic fragments, comprising most of the larger grains between 50 and 500 microns in size, probably with some quartz and calcite-feldspar grains, had an epiclastic origin. The most abundant minerals among the fragments are quartz, feldspar and chlorite-muscovite intergrowths, with minor calcite and amphibole. The quartz occurred as sub-euhedral and anhedral grains, up to 0.5 mm. The quartz also occurred in small crescent-shaped fragments and as several polycrystalline fragments. Fragments of feldspar were present as angular, anhedral albite with polysynthetic twinning. Some alkali feldspar occurred as euhedral to subhedral grains without twinning, and with some epidote alteration. The epidote, calcite and chlorite porphyroblasts are likely to be pseudoforms after melanocratic minerals and/or glass (e.g. there are a few grains with chlorite clearly replacing amphibole). Trace amounts of cordierite had been replaced by sericite and chlorite. A few former vesicles, up to 200 microns across, revealed the inward growth of secondary euhedral quartz crystals. Trace minerals include sulphides, leucoxene and tourmaline. Lithic metapelite fragments and some polycrystalline quartz fragments are epiclastic components. The unit experienced low grade metamorphism, with developed schistosity and axial-plane cleavage.

This sample is a moderately to well-sorted, foliated sub-arkose, with bedding and schistosity and evidence of sub-angular to sub-rounded grains. The sample comprises framework grains 73%, matrix 8% and cement 15%. The matrix is mainly composed of fine-grained quartz. Cementing material is present as recrystallised quartz, micas/clay and opaque minerals. Framework grains are dominated by monocrystalline quartz grains, with lesser plagioclase and K-feldspar. The feldspar has been altered by sericite, sausserite and iron oxides. Lithic fragments are sub-rounded and sub-angular to angular grains of granite (feldspar-quartz) and metasiltstone. Other minerals include muscovite, biotite, tourmaline, apatite and zircon. Most of the opaque grains and a proportion of the cement appeared to be represented by ilmenite, hematite and limonite. A weak foliation is defined by the preferred orientation of sericite/muscovite.

Exploration well Beachcomber 1 was drilled in 1988 to investigate the hydrocarbon potential of the large Beachcomber structure (Dee, 1988). The primary objective of the well was the Poolowanna Formation of the Pedirka Basin succession, with the Cadna-owie Formation and Algebuckina Sandstone of the Eromanga Basin as secondary targets. The well is located 46.6 kilometres NNW of Poeppels Corner 1 and approximately 450 kilometres NW of Moomba. Beachcomber 1 reached a total depth of 1826 metres in unnamed pre-Permian metasedimentary rocks (Dee, 1988). Beachcomber 1 intersected 39.5 m of siliceous metasedimentary rocks with biotite, pyrite and vein quartz at its base (Dee, 1988). Although this succession could conceivably represent basement rather than Warburton Basin sedimentary rocks, at present Beachcomber 1 sits within the interpreted margin of the western Warburton Basin (Edgoose and Munson, 2013). The sample consists of metasedimentary rock chips from the interval 1800–1825 metres and was selected to place constraints on the depositional age of this part of the Warburton Basin.
Beachcomber 1
Kositcin, N., Verdel, C., Edgoose, C., 2023. Summary of results. Joint NTGS-GA geochronology project: western Warburton Basin, March 2022-February 2023. Northern Territory Geological Survey Record, 2023-006, 16pp.

Curtin University
Cottons Breccia
King Island Region
Calver, C.R., Crowley, J.L., Wingate, M.T.D., Evans, D.A.D., Raub, T.D., Schmitz, M.D., 2013. Globally synchronous Marinoan deglaciation indicated by U-Pb geochronology of the Cottons Breccia, Tasmania, Australia. Geology, 41(10), 1127-1130.

Boise State University
SHRIMP dating in sample 4 (R008187) prompted submission of an additional aliquot of this sample to the Isotope Geology Laboratory at Boise State University (Idaho, USA) for chemical abrasion (CA) TIMS U-Pb dating.
Cottons Breccia
King Island Region
Calver, C.R., Crowley, J.L., Wingate, M.T.D., Evans, D.A.D., Raub, T.D., Schmitz, M.D., 2013. Globally synchronous Marinoan deglaciation indicated by U-Pb geochronology of the Cottons Breccia, Tasmania, Australia. Geology, 41(10), 1127-1130.

inferred emplacement age of the source rock
The youngest analysis (BH6-01-21) has an age of 239 ± 13 Ma, which is 96.3% concordant and within uncertainty of the other four youngest ages. Accordingly, 249 Ma is the inferred emplacement age of the source rock.
Conglomeratic sandy siltstone. Dwyer et al 2018 paraphrased: "Volcaniclastic and volcanogenic samples PANGBH5-04 and PANGBH6-01... are conformably interbedded with and derived from the alkaline volcanics. The main constituent of these samples is clasts and volcanic debris from the associated alkaline volcanics. Geochemically the breccias/volcaniclastics are indistinguishable from the interbedded volcanics (Crawford, 2012)."

Volcanogenic tuffaceous sandstone-conglomerate. Dwyer et al 2018 paraphrased: "Tuffs and intrusive calc-alkaline dolerites exist within drill holes MINOL33, MINOL30 and MINOL21, which are located within the geophysical anomaly associated with the Louth Volcanics. Sharp transitions from quartz-rich volcanogenic sandstones to volcaniclastic matrix through clast supported breccias intercalated with tuffaceous horizons observed in MINOL30 suggest that volcanism and sedimentation were synchronous. Vickery (2008) also suggested a syn-depositional timing for volcanism based on evidence from Louth 1–4 drill core, located at the southern extremity of the Louth Volcanics.In associated tuffs, sedimentary rocks and field samples, bedding parallel and axial planar fabrics were observed (MINOL21-05, MINOL30-04, MINOL33-06, RDT7)."

A large quantity of zircons were recovered for PANGBH7-01 but they were so fine (~ 20-30 mm) that analytical options were limited and returned mostly discordant results. This sample is located at the same approximate depth as PANGBH6-01 and appear to represent the same sequence of volcanogenic and volcaniclastic sedimentary rocks. The results from this samples are so limited that it is possible the youngest component was not analysed, and this age is considered unlikely to represent this unit's true MDA.
Sandy siltstone.

489 +/- 12 Ma - youngest concordant grain may be interpreted as the MDA.
This age of 510 +/- 8.6 Ma is a more conservative MDA estimate, using the youngest cluster of 3 analyses. Geochronology samples SW014-018 are composites of multiple intervals in order to build rock volume and the odds of recovering zircon. Composite samples were only selected from within conformable sequences with no evidence of discontinuities.
Hack et al 2018 paraphrased: "These samples are massive, strongly compacted, well-sorted, very fine-grained sandstone. [They are] predominantly composed of slightly flattened subrounded to rounded grains of quartz with highly sutured grain boundaries and internally grains show undulose extinction. Abundant quartz veins and minor finegrained secondary carbonate and chlorite occur. Zircon grains are 50-200 um for the long axis and are commonly sub-angular to well-rounded. CL imagery reveals grains commonly display broad and patchy oscillatory zoning of contrasting growth bands commonly mantled by bright high-intensity rims. Patchy homogenous to convoluted growth banding is observed in some grains."
Hack, A. C., Dwyer, R. C., Phillips, G., Whalan, S. & Huang, H. (2018). The age and tectonic significance of the Warraweena Volcanic sand-related rocks, southern Thomson Orogen. Australian Journal of Earth Sciences 65 (7-8), pp.1071-1096.

The youngest age of 423 +/- 13Ma is interpreted cautiously as the MDA. Geochronology samples ACH7-8 are composite detrital samples targeted by sand grain-sized beds and lenses within conformable sedimentary sequences in order to build rock volume and the odds of recovering zircon.
Hack et al 2018 paraphrased: "Sample ACH7-8 is a fine to medium grained quartz-rich, moderately sorted sandstone with minor (3-5 vol%) fine volcanic debris, accessory minerals (opaques, plagioclase and biotite) and secondary carbonate, sericite, chlorite, and epidote. Zircon grains are 30-120 um for the long axis and are equant to elongate euhedral to well-rounded. CL imagery reveals most internal zoning is homogenous to patchy and generally low intensity, mantled by high-intensity rims/exteriors. More euhedral grains reveal concentric to oscillatory zoning commonly mantling patchy inherited cores."
Hack, A. C., Dwyer, R. C., Phillips, G., Whalan, S. & Huang, H. (2018). The age and tectonic significance of the Warraweena Volcanic sand-related rocks, southern Thomson Orogen. Australian Journal of Earth Sciences 65 (7-8), pp.1071-1096.

The calculated mean age based on the youngest three (or more) ages that overlap in 2 sigma
Girilambone Group
Abdullah et al 2020 paraphrased "The sample is a biotite-muscovite schist. Quartz-mica domains, dominance of polycrystalline quartz"
Abdullah R., Shaanan U., Lynn K., Rosenbaum G. (2020) Provenance and deformation history of the Eastern Thomson Orogen and implications for the Paleozoic evolution of the Tasmanides (Eastern Australia), Australian Journal of Earth Sciences 67, 153-173

The calculated mean age based on the youngest three (or more) ages that overlap in 2 sigma
Girilambone Group
Abdullah et al 2020 paraphrased "The sample is a biotite-muscovite schist. Well-developed quartz-mica domains, majority of quartz are subgrains."
Abdullah R., Shaanan U., Lynn K., Rosenbaum G. (2020) Provenance and deformation history of the Eastern Thomson Orogen and implications for the Paleozoic evolution of the Tasmanides (Eastern Australia), Australian Journal of Earth Sciences 67, 153-173

Volcaniclastic breccia. Dwyer et al 2018 paraphrased: "Volcaniclastic and volcanogenic samples PANGBH5-04 and PANGBH6-01... are conformably interbedded with and derived from the alkaline volcanics. The main constituent of these samples is clasts and volcanic debris from the associated alkaline volcanics. Geochemically the breccias/volcaniclastics are indistinguishable from the interbedded volcanics (Crawford, 2012)."

University of Adelaide
Bolla Bollana Tillite
tuff
Cox, G.M., Isakson, V., Hoffman, P.F., Gernon, T.M., Schmitz, M.D., Shahin, S., Collins, A.S., Preiss, W., Blades, M.L., Mitchell, R.N., Nordsvan, A., 2018. South Australian U-Pb zircon (CA-ID-TIMS) age supports globally synchronous Sturtian deglaciation. Precambrian Research, 315, 257-263.

University of Adelaide
Tapley Hill Formation
Bolla Bollana Tillite by Cox et al. (2018). Lloyd et al. (2020) said this was "mistaken" and that the sample is Tapley Hill Formation.
tuff
Cox, G.M., Isakson, V., Hoffman, P.F., Gernon, T.M., Schmitz, M.D., Shahin, S., Collins, A.S., Preiss, W., Blades, M.L., Mitchell, R.N., Nordsvan, A., 2018. South Australian U-Pb zircon (CA-ID-TIMS) age supports globally synchronous Sturtian deglaciation. Precambrian Research, 315, 257-263.

laser ablation: ASI RESOlution 193 nm ArF Excimer laser ablation system
University of Adelaide
Maximum depositional age defined from 207Pb/235U in grain 65, even though the "preferred age" for grain 65 is actually 206Pb/238U (= 577 +/- 8 Ma).
Kanmantoo Group
Meta-greywacke, dark grey, fine to medium grained. Relatively massive, quartz veined, with minor pyrite and chalcopyrite possibly associated with fracture planes.
Berri North 1
Brotodewo, A., Wise, T., Lloyd, J., 2021. LA-ICP-MS detrital zircon geochronology from the Delamerian Orogen. Geological Survey of South Australia. Report Book, 2021/00015, 73p.

laser ablation: ASI RESOlution 193 nm ArF Excimer laser ablation system
Maximum depositional age defined from 207Pb/235U in grain 94, even though the "preferred age" for grain 94 is actually 206Pb/238U (= 512 +/- 10 Ma).
Medium-grained grey metapsammite mainly comprising quartz and feldspars
SHR 34
Brotodewo, A., Wise, T., Lloyd, J., 2021. LA-ICP-MS detrital zircon geochronology from the Delamerian Orogen. Geological Survey of South Australia. Report Book, 2021/00015, 73p.

laser ablation: ASI RESOlution 193 nm ArF Excimer laser ablation system
Maximum depositional age defined from 207Pb/206Pb in grain 77, even though the "preferred age" for grain 77 is actually 206Pb/238U (= 678 +/- 10 Ma).
Umberatana Group
Dark grey, fine-grained greywacke comprising quartz, plagioclase, biotite and other lithic fragments in a fine matrix
Brotodewo, A., Wise, T., Lloyd, J., 2021. LA-ICP-MS detrital zircon geochronology from the Delamerian Orogen. Geological Survey of South Australia. Report Book, 2021/00015, 73p.

Maximum depositional age defined from 207Pb/206Pb in grain 40, even though the "preferred age" for grain 40 is actually 206Pb/238U (= 690 +/- 19 Ma).
Umberatana Group
Dark grey, fine-grained greywacke comprising quartz, plagioclase, biotite and other lithic fragments in a fine matrix

Kanmantoo Group
Pale grey, fine-grained metapsammite comprising quartz, plagioclase and biotite
COP 50

Maximum depositional age defined from 207Pb/206Pb in grain 36, even though the "preferred age" for grain 36 is actually 206Pb/238U (= 313 +/- 5 Ma).
Innamincka Formation
Dark grey, fine-grained laminated shale.
Boxwood 1

Hack et al 2018 paraphrased: Composite sample of a locally distinctive metagreywacke. It is characterised by coarse (generally <5 mm), poorly sorted, angular to sub-rounded clasts dominated by lithic components including fragments of relatively fresh mafic groundmass and clinopyroxene and subordinate quartz. Zircon grains are 100-300 um for the long axis and are commonly sub-rounded to well-rounded with minor euhedral to subhedral grains present. More rounded grains generally have patchy to convoluted zoning with concentric primary growth zoning not well preserved. The CL imagery of the euhedral to subhedral component reveals the common presence of inherited cores mantled by oscillatory-zoned growth bands.
Hack, A. C., Dwyer, R. C., Phillips, G., Whalan, S. & Huang, H. (2018). The age and tectonic significance of the Warraweena Volcanic sand-related rocks, southern Thomson Orogen. Australian Journal of Earth Sciences 65 (7-8), pp.1071-1096.

The calculated mean age based on the youngest three (or more) ages that overlap in 2 sigma
Nebine Metamorphics
Abdullah et al 2020 paraphrased "The sample is a chlorite-biotite schist, a dominant foliation is defined by well-developed quartz-mica domains, and/or by preferred orientations of metamorphic biotite and muscovite. It is assumed that the quartz-mica domains were generated by metamorphic differentiation associated with an intense crenulation cleavage, thus representing a second-generation fabric."
AOP ALBA NO1
Abdullah R., Shaanan U., Lynn K., Rosenbaum G. (2020) Provenance and deformation history of the Eastern Thomson Orogen and implications for the Paleozoic evolution of the Tasmanides (Eastern Australia), Australian Journal of Earth Sciences 67, 153-173

Curtin University
HG metamorphism age: 1678 +/-4 Ma. MSWD = 1.6. N = 20
Pooranoo Metamorphics
Gascoyne Region
Wingate, MTD, Kirkland, CL and Johnson, SP 2014, 195849: quartzite, Star of Mangaroon Mine; Geochronology Record 1151: Geological Survey of Western Australia, 5p.

Bessie Creek Sandstone
Walton 2
Yang, B., Smith, T.M., Collins, A.S., Munson, T.J., Schoemaker, B., Nicholls, D., Cox, G., Farkas, J., Glorie, S., 2018. Spatial and temporal variation in detrital zircon age provenance of the hydrocarbon-bearing upper Roper Group, Beetaloo Sub-basin, Northern Territory, Australia. Precambrian Research, 304, 140-155.

Based on three analyses of three grains.
Bessie Creek Sandstone
Altree 2
Yang, B., Smith, T.M., Collins, A.S., Munson, T.J., Schoemaker, B., Nicholls, D., Cox, G., Farkas, J., Glorie, S., 2018. Spatial and temporal variation in detrital zircon age provenance of the hydrocarbon-bearing upper Roper Group, Beetaloo Sub-basin, Northern Territory, Australia. Precambrian Research, 304, 140-155.

Kanmantoo Group
This sample is dark grey, fine-grained, greywacke comprising quartz, plagioclase, biotite and other lithic fragments in a fine matrix. Large calcite and quartz veinlets are present.
Loxton 2

Maximum depositional age defined from 207Pb/235U in grain 28, even though the "preferred age" for grain 28 is actually 206Pb/238U (= 561 +/- 7 Ma).
Coarse-grained grey metasandstone mainly comprising quartz and feldspars with biotite, which defines a foliation at low-moderate angle to the core axis.

Callanna Group
Slightly sheared pink and grey arkosic sandstone with thin magnetite-bearing heavy mineral bands.

Curtin University
Kelly Group
medium- to coarse-grained sandstone
Pilbara Region
Geological Survey of Western Australia (GSWA)
Nelson, DR 2004, 177131: coarse-grained metasandstone, Lionel Well; Geochronology Record 529: Geological Survey of Western Australia, 6p.

Group S comprises 61 analyses of 61 zircons (Table 1), which yield 207Pb*/206Pb* dates of 2745-1039 Ma. A more conservative estimate of the maximum depositional age can be based on the weighted mean 207Pb*/206Pb* date of 1177 +/- 18 Ma (MSWD = 1.3) for the youngest coherent group of 14 analyses in Group S.
Karukali Quartzite
Musgrave Region
Wingate, MTD, Lu, Y, Quentin de Gromard, R, Howard, HM and Haines, PW 2017, 208494: quartzite, Mount Deering; Geochronology Record 1439: Geological Survey of Western Australia, 7p.

Killi Killi Formation
Tanami Region
Kirkland, CL and Wingate, MTD 2010, 177278: schistose metagreywacke, Bald Hill; Geochronology Record 922: Geological Survey of Western Australia, 4p.

pelitic and psammitic sedimentary rocks 74240
metasandstone
Yilgarn Region
Walling Rock
Geological Survey of Western Australia geochronology dataset

The weighted mean 206Pb-238U date indicated by this group is 691 +/- 22 Ma (chi-squared =0.75. N = 8).
Officer Region
NELSON, D. R., 2004, 154668: sandstone, Empress 1A; Geochronology dataset 53; in Compilation of geochronology data, June 2006 update: Western Australia Geological Survey.

Australian National University
Not explicitly stated what the age is interp'd as.
Ellrott Rhyolite
dark grey volcanic breccia
Proserpine Region
1km south-west of Tungamull, ROCKHAMPTON MGA 263094 7419384
Murray, C.G., Blake, P.R., Crouch, S.B.S., Hayward, M.A., Robertson, A.D.C., Simpson, G.A., 2012. Geology of the Yarrol Province central coastal Queensland. Queensland Geology, 13, 675pp.

Lennis Sandstone
Officer Region
Wingate, MTD, Kirkland, CL, Haines PW and Hocking, RM 2013, 199424: sandstone, Empress 1; Geochronology Record 1113: Geological Survey of Western Australia, 6p.

Juderina Formation
metasandstone
Nabberu Region
Geological Survey of Western Australia geochronology dataset

high grade metamorphic rocks 72653
pelitic metasedimentary rock
Arunta Region
Worden, K.E., Carson, C.J., Close, D.F., Donnellan, N., Scrimgeour, I.R., 2008. Summary of results. Joint NTGS-GA geochronology: Tanami Region, Arunta Region, Pine Creek Orogen and Halls Creek Orogen correlatives, January 2005-March 2007. Northern Territory Geological Survey Record, 2008-003, 180p.

Inserted from Geochron Delivery (Geoscience Australia; http://www.ga.gov.au/geochron-sapub-web/), 23 October 2019
Bullrush Conglomerate
The Bullrush Conglomerate (Rawlings et al., 2008) is conformably overlain by the Plain Creek Formation and lies unconformably on the Top Rocky Rhyolite and the Drummond Formation. Rawlings et al. (2008) describe the Bullrush Conglomerate as a crudely bedded polymict granule, pebble to cobble conglomerate, with interbedded cross-bedded quartz and lithic sandstone and siltstone. Sedimentary structures include current lineations, symmetrical ripples, and small-scale trough cross beds. The sample location is near the described type section (Rawlings et al., 2008), ca 150m downstream of the confluence of the South Nicholson River and Maloney Creek. The outcrop consists of clast- to matrix-supported rounded to angular, poorly-sorted polylithic cobble conglomerate. Rhyolite clasts locally comprise as much as 10-15% of the total clast population; the remaining clasts are dominated by sandstone, siltstone, mudstone, layered chert, milky vein quartz and possibly small fragments of mafic volcanics. Crudely defined bedding dips shallowly to moderately to the north.
South Nicholson Region
Kositcin, N., Carson, C.J., 2019. New SHRIMP U-Pb zircon ages from the South Nicholson and Carrara Range regions, Northern Territory. Geoscience Australia. Record, 2019/09, 217p.; Carson, C.J., Kositcin, N., Anderson, J.R., Henson, P.A., 2023, A revised Proterozoic tectono-stratigraphy of the South Nicholson region, Northern Territory, Australia - insights from SHRIMP U-Pb detrital zircon geochronology. Australian Journal of Earth Sciences, in press.

Pooranoo Metamorphics
Gascoyne Region
Nelson, DR 2004, 169091: metasandstone, Hogan Well; Geochronology Record 120: Geological Survey of Western Australia, 5p.

Maximum depositional age is a weighted average age c. 340 Ma. Contrasts with known deposition age of the sediment being early Triassic.
Updated from Geochron Delivery (Geoscience Australia; http://www.ga.gov.au/geochron-sapub-web/), 20 September 2019
Erskine Sandstone
fine-med grained ss
Canning Region

A more conservative estimate of the maximum depositional age can be based on the weighted mean 207-corrected 238U/206Pb* date of 849 +/- 29 Ma (MSWD = 0.77) for the two youngest analyses
Amadeus Region
Wingate, MTD, Kirkland, CL and Haines, PW 2014, 199419: sandstone breccia, Mu Hills; Geochronology Record 1192: Geological Survey of Western Australia, 5p.

A more conservative estimate of the maximum depositional age can be based on the weighted mean 207Pb*/206Pb* date of 519 +/- 3 Ma. MSWD = 0.38. N = four youngest analyses
Nambeet Formation
Canning Region
Wingate, MTD and Haines, PW 2009, 135962: sandstone, Samphire Marsh 1; Geochronology Record 777: Geological Survey of Western Australia, 5p.

Savory Region
Geological Survey of Western Australia geochronology dataset

Inserted from Geochron Delivery (Geoscience Australia; http://www.ga.gov.au/geochron-sapub-web/), 23 October 2019
GOR 3C Phase 1

84 analyses give complex peaks of ~1600 & 1800Ma & a simple peak at 2830Ma. The youngest complex peak cannot be statistically deconvolved. Manual deconvolution yields small overlapping populations. The youngest is a 3 grain peak at 1577 ? 29Ma
Hedleys Sandstone
South Nicholson Region
Magee, C.W., Withnall, I.W., Hutton, L.J., Perkins, W.G., Donchak, P.J.T., Parsons, A., Blake, P.R., Sweet, I.P., Carson, C.J., 2012. Joint GSQ-GA geochronology project, Mount Isa Region, 2008-2009. Queensland Geological Record, 2012/07, 134p.

A total of 85 analyses were collected from 83 zircon crystals. One analysis has anomalously low 206Pbc (< -2.00%). One analysis yielded an individual 207Pb/206Pb date older than 1400 Ma, but more is than 10% discordant. A further 13 analyses were acquired during instrument instability. These 15 analyses are interpreted as unreliable and are not considered further. The remaining 70 analyses are characterised by low to moderate U contents (31-640 ppm, median 188 ppm), a wide range of Th/U (0.03-1.79, median 0.68), and low 206Pbc (maximum 0.77%, median 0.02%). The 70 accepted analyses are divided into five groups: Group 1 is a single analysis with an individual 238U/206Pb date of 504 +/- 23 Ma (2sigma); Group 2 consists of 31 analyses from 31 zircons with individual 238U/206Pb dates between c. 635 Ma and 510 Ma; Group 3 consists of 27 analyses from 27 zircons with individual 238U/206Pb dates between c. 1230 Ma and 840 Ma; Group 4 is a single analysis with an individual 207Pb/206Pb date of 1431 +/- 70 Ma (2sigma); and Group 5 consists of ten analyses from ten zircons with individual 207Pb/206Pb dates pre-2000 Ma.The individual 238U/206Pb age of 504 +/- 23 Ma (2sigma) is interpreted as a maximum depositional age for the 600 m interval of the Eneabba Formation. This age is considerably older than the biostratigraphically (C. torosa Zone) determined Early Jurassic depositional age of this unit.
Updated from Geochron Delivery (Geoscience Australia; http://www.ga.gov.au/geochron-sapub-web/), 20 September 2019
Harvey 1
Queensland Department of Mines and Energy
Lewis, C.J., 2017. SHRIMP U-Pb isotopic results, GSWA Harvey 1, Western Australia. Geoscience Australia. Record, 2017/20, 110p.

felsic intrusive rock
Arunta Region
Worden, K.E., Carson, C.J., Close, D.F., Donnellan, N., Scrimgeour, I.R., 2008. Summary of results. Joint NTGS-GA geochronology: Tanami Region, Arunta Region, Pine Creek Orogen and Halls Creek Orogen correlatives, January 2005-March 2007. Northern Territory Geological Survey Record, 2008-003, 180p.

Inserted from Geochron Delivery (Geoscience Australia; http://www.ga.gov.au/geochron-sapub-web/), 23 October 2019
Ragnar 1

Tarcunyah Group
medium-grained sandstone
Paterson Region
Geological Survey of Western Australia (GSWA)
Nelson, DR 2004, 177104: fine-grained metasandstone, Nimberra Well; Geochronology Record 95: Geological Survey of Western Australia, 5p.

MOUNT PHILLIPS_185954.1
Gascoyne Region

Mount McGrath Formation
MOUNT BRUCE_169081.1
Ashburton Region
Nelson, DR 2004, 169081: pebbly sandstone, Meteorite Bore; Geochronology Record 116: Geological Survey of Western Australia, 6p.

Alternate age: 3278 +/- 21 Ma. MSWD=1.23. N=4
Several interpretations of these results are possible. The date of 3312 +/- 4 Ma (Group 1) may be interpreted as the age of igneous crystallization of the felsic volcanic precursor to the volcaniclastic sandstone, with the younger date indicated by the discordant analyses of age 3278 +/- 21 Ma (Group 2) corresponding to the timing of an ancient disturbance event during which these analysis sites lost radiogenic Pb. However, analyses belonging to Group 2 indicate generally low U and Th contents and it is unclear why these sites should have lost radiogenic Pb when those of Group 1 did not. An alternative explanation is that the date of 3278 +/- 21 Ma indicated by the weighted mean 207Pb/206Pb ratio of the four analyses of Group 2, or the younger date indicated by discordant ungrouped analysis 14.1, provides a maximum age for reworking and redeposition of a predominantly 3312 +/- 4 Ma volcanic precursor rock.
Kelly Group
volcaniclastic sandstone
Pilbara Region
Nelson, DR 2002, 169000: volcaniclastic sandstone, Cork Tree Well; Geochronology Record 166: Geological Survey of Western Australia, 4p.

Harvey 1
Queensland Department of Mines and Energy
Lewis, C.J., 2017. SHRIMP U-Pb isotopic results, GSWA Harvey 1, Western Australia. Geoscience Australia. Record, 2017/20, 110p.

Biscay Formation
GORDON DOWNS_206183.1
Halls Creek Region
Lu, Y, Wingate, MTD, Maidment, DW and Hollis, JA 2017, 206183: feldspathic metasandstone, Jubilee mine; Geochronology Record 1387: Geological Survey of Western Australia, 6p.

quartz-plagioclase-biotite-muscovite metasandstone
Yilgarn Region

quartzite
Pilbara Region
Nelson, DR 2002, 168997: quartzite, Farrel Well; Geochronology Record 165: Geological Survey of Western Australia, 4p.

Anderson, J.R., Lewis, C.J., Jarrett, A.J.M., Carr, L.K., Henson, P.A., Carson, C.J., Southby, C., Munson, T.J., 2019. New SHRIMP U-Pb zircon ages from the South Nicholson Basin, Mount Isa Province and Georgina Basin, Northern Territory and Queensland: July 2017-June 2018. Geoscience Australia. Record, 2019/10, 101p.

Reddish grey sand to gravels. Possible base of Madura or Loongana Fm. Unconsolidated.
Jagodzinski, E.A., Bodorkos, S., Crowley, J.L., Pawley, M.J., Wise, T.W., 2019. PACE Copper Coompana Drilling Project: U-Pb dating of basement and cover rocks. Geological Survey of South Australia. Report Book, 2018/00028, 211p.

Warramunga Formation
lower volcaniclastic sandstone
Sample GS20PGF084 is a thinly layered meta-siltstone/sandstone collected from the interval 468.1-473.45 m. This sample is from the hanging wall of the base metal mineralisation. The meta-sandstone layers comprise 40-50%, 10-20 micron subhedral quartz and 30-40%, 20-25 micron sericite-altered feldspar grains in a sericite-chlorite groundmass with scattered traces of 5-10 micron opaque minerals. There is an oblique, weak, spaced foliation defined by sericite that cross-cuts the bedding.
Cross, A.J., Farias, P.G., Huston, D.L., 2022. Summary of results. Joint NTGS-GA geochronology project: Rover mineral field, Warramunga Province, July-December 2020. Northern Territory Geological Survey Record, 2022-005, 31p.

Carranya Formation
Halls Creek Region
Wingate, MTD 2007, 184269: quartz sandstone, Carranya Homestead; Geochronology Record 658: Geological Survey of Western Australia, 5p.

Puna Kura Kura Formation
The Puna Kura Kura Formation is the uppermost part of the Winnall Group (Donnellan and Normington 2017). At the type section in HENBURY, the Puna Kura Kura Formation comprises well-sorted feldspathic sandstone (Donnellan and Normington 2017). The Chookla Member of the Puna Kura Kura Formation is a poorly sorted, clast- to matrix-supported conglomerate with pebble-, cobble- and small boulder-size clasts of quartzite, vein quartz, and minor basement rock (Normington et al 2018). The Puna Kura Kura Formation is probably latest Ediacaran or Cambrian based on its stratigraphic position (Verdel et al 2020). A previous detrital zircon sample (LA19CSV060) of the Puna Kura Kura Formation from LAKE AMADEUS produced a maximum depositional age of 690 +/- 10 Ma (Beyer et al 2020). This sample (LA19CSV144) of the Puna Kura Kura Formation is a moderately sorted, medium-grained, feldspathic sandstone collected from a ridge ~40 km southwest of Kings Canyon.
Amadeus Region
Kositcin, N., Verdel, C., Normington, V.J., Simmons, J.M., 2021. Summary of results. Joint NTGS-GA geochronology project: western Amadeus Basin, July-August 2020. Northern Territory Geological Survey Record, 2021-002, 25p.

vitric tuff
Nelson, DR 2001, 168909: vitric tuff, Gilbert Cairn; Geochronology Record 223: Geological Survey of Western Australia, 4p.

Using a maximum-likelihood (mixture-modelling) approach (Sambridge and Compston, 1994), the data can be deconvolved into three subcomponents (2?): at 3512 +/- 5 Ma (10 analyses), 3474 +/- 3 Ma (35 analyses), and 3448 +/- 6 Ma (4 analyses). These are interpreted as the ages of zircon-crystallizing rocks in the detrital source region(s), or as the ages of detrital components within sediments that have been reworked into this rock.
Sandstone
Geological Survey of Western Australia (GSWA)
Wingate, MTD, Kirkland, CL, Bodorkos, S, Van Kranendonk, MJ and Hickman, AH 2011, 160958: volcaniclastic metasandstone, Trendall Reserve; Geochronology Record 1070: Geological Survey of Western Australia, 6p.

Tickalara Metamorphics
DIXON RANGE_206128.1
Halls Creek Region
Lu, Y, Wingate, MTD, Kirkland, CL, Maidment, DW, Phillips, C and Hollis, JA 2016, 206128: pelitic schist, Panton mine; Geochronology Record 1341: Geological Survey of Western Australia, 6p.

New Hope Sandstone Member
Arkosic medium to coarse grained sandstone, thick to very thickly bedded with laminations in parts. Clay and quartz rich (no mica observed). Dating Objective: Maximum age of deposition.
Mount Isa Region
Lewis, C.J., Withnall, I.W., Hutton, L.J., Bultitude, R.J., Slade, A.P., Sargent, S., 2020. Summary of results. Joint GSQ-GA geochronology project: Mount Isa region, 2016-2017. Queensland Geological Record, 2020/01, 71p.

Inserted from Geochron Delivery (Geoscience Australia; http://www.ga.gov.au/geochron-sapub-web/)
Balbirini Dolostone
basal stromatolitic unit
Sample BD19TJM127 was collected from a prominent 20 m-thick interval of thinly interbedded quartz sandstone and minor dolograinstone near the base of the stromatolitic unit of the medial Balbirini Dolostone. In measured section MS 77/04 (Jackson et al 1987), which corresponds to the type section of the formation, the sampled sandstone interval is depicted as being about 60 m stratigraphically above the base of the stromatolitic unit and about 360 m above the base of the formation. The sample was collected from an east-facing scarp slope about 150 m to the southeast of the line of the measured section. In the vicinity of the sample site, the sandstone and interbedded dolograinstone beds are up to about 10 cm thick but mostly are 1-5 cm thick; bedding surfaces are planar to irregular and have current ripplemarks in places. Sandstone beds typically have a thick, red-brown to dark brown weathering rind, whereas the dolograinstone beds are grey to light yellow-brown; fresh surfaces of both rock types are mostly grey to pale brown. Both the lower and upper contacts of the sampled sandstone interval are gradational with bedded dolomitic shale and dolomudstone; contacts are marked by the alternation of finer and coarser rock types over 1-2 metres. Sample BD19TJM127 is a fine-grained dolomitic quartz-lithic sandstone. It was collected from a low-angle, planar tabular cross-bedded sandstone bed about 10 cm thick at the base of the sandstone interval. In thin section, the sample consists mostly of quartz with minor chert, rare feldspar and tourmaline, and accessory zircon. Quartz is rounded to subangular; irregular sutured grain boundaries from compaction have imparted a secondary angularity to many grains. Syntaxial quartz overgrowths form an original siliceous cement that has been partially replaced by a corrosive dolomitic cement. The age of the sampled sandstone interval is constrained by previous SHRIMP U–Pb zircon dating of tuffaceous rocks (Page et al 2000).
McArthur Region
Kositcin, N., Munson, T.J., 2020. Summary of results. Joint NTGS-GA geochronology project: Balbirini Dolostone, southern McArthur Basin, June 2019-September 2019. Northern Territory Geological Survey Record, 2020-002, 14p.

Sample 2021330157 was collected from NDI Carrara 1 from tray 216 at the depth interval 706.26-706.34 m. Sample 2021330157 is a conformable narrow band of coarse-grained, poorly-sorted textually immature sediment with sharp upper and lower contacts with the host massive shale (Crombez et al., 2022). There is some uncertainty of the volcaniclastic nature of this sample (field logged as ‘lithic tuff’), which alternatively may reflect a small debris flow or higher energy deposit within the host shale.
NDI Carrara 1
Kositcin, N., Carson, C.J., 2022, Exploring for the Future: SHRIMP U-Pb geochronology of NDI Carrara 1, South Nicholson region, Northern Territory. Geoscience Australia. Record, 2022/42.

Arenite
Yilgarn Region

Rhyolite
Wingate, MTD, Kirkland, CL, Hickman, AH and Van Kranendonk, MJ 2012, 160957: felsic volcaniclastic rock, Mount York; Geochronology Record 1069: Geological Survey of Western Australia, 4p.

volcaniclastic sandstone
Hamersley Region
Nelson, DR 2001, 168935: volcaniclastic sandstone, Sophie Tank; Geochronology Record 206: Geological Survey of Western Australia, 4p.

Data migrated from OZCHRON1. Original comment: The detrital grains in this metasediment have a complex range of ages, all of which represent older limits for the time of sedimentation. The main concentrations are at about 1900 Ma, 2500 Ma and 2600 Ma.
Updated from Geochron Delivery (Geoscience Australia; http://www.ga.gov.au/geochron-sapub-web/), 20 September 2019
Einasleigh Metamorphics
micaceous quartzite schist
Georgetown Region
Georgetown-Coen Province: Georgetown region. Percyville

Data migrated from OZCHRON1. Original comment: Fluvial channel sediment incising ignimbrites. Contains multiple zircon populations, , of 1859+/-17 Ma,1962+/-10 Ma,~2070,2170,2460,2500-2600 Ma. All are detrital zircon populations, older and unrelated to the age of the associated volcanics (1830 Ma).
Gimbat Ignimbrite Member
epiclastic sediment, South Alligator Conservation Zone
Pine Creek Region
adjacent to the Palette Fault, 1km north of Big Sunday
Jagodzinski, E.A., 1992. A study of the felsic volcanic succession south-east of Coronation Hill: palaeovolcanology, geochemistry, geochronology. Bureau of Mineral Resources, Record, 1992/09, 147p.

Stag Creek Volcanics
volcanic breccia, South Alligator Conservation Zone
Pine Creek Region
400m N of 2J access road, 1.8km east of Kambolgie Creek

Data migrated from OZCHRON1. Original comment: The only zircons measured in this mafic volcanic rock are xenocrysts that have apparent ages between 2450-2750 Ma. An unreliable analysis also at 1890 Ma.
Nungbalgarri Volcanics
altered amygdaloidal basalt, South Alligator Conservation Zone
McArthur Region
3km east of Katherine River, 1.5 km of Sleisbeck crossing

Data migrated from OZCHRON1. Original comment: Of the 45 xenocrystic zircon grains, a number are in the range 1820-1840 Ma, thus defining a likely maximum age of about 1830 Ma for the depositional age. Other xenocrystic populations are 1850-1880 Ma, 1950-2100 Ma, 2200-2300 Ma, 2450-2570 Ma.
Kombolgie Subgroup
South Alligator Conservation Zone
McArthur Region
3km east of Katherine River, 1.5 km SW of Sleisbeck crossing
Unpublished data (RW Page) in Geoscience Australias OZCHRON database. Mentioned in Neumann and Fraser 2007 http://pid.geoscience.gov.au/dataset/ga/65244

Data migrated from OZCHRON1. Original comment: This age is interpreted as a possible crystallisation age, but is rigorously a maximum age for deposition of the Kombolgie Fmn. Clear inheritance at ~1870 and 2400-2500 Ma is also observed.
McAddens Creek Volcanic Member
flow-banded rhyolite
Pine Creek Region
600 m WNW of ABC uranium prospect
Unpublished data (RW Page) in Geoscience Australias OZCHRON database. Mentioned in Neumann and Fraser 2007 http://pid.geoscience.gov.au/dataset/ga/65244

Data migrated from OZCHRON1. Original comment: Many of the 52 analyses of the detrital zircons are in the range 1830-1870 Ma, thus providing a maximum age of 1830 Ma for deposition. Other detrital groupings are around 1930-2060 Ma, 2300 Ma, 2400 Ma, 2500 Ma.
Kombolgie Subgroup
sandstone
300 m S of ABC uranium prospect

Data migrated from OZCHRON1. Original comment: Only 15 detrital zircons analysed, and some are in the range 1830-1850 Ma, giving a likely maximum age of about 1840 Ma. Other suites are 1870-1900 Ma, 2025 Ma, 2310 Ma, 2526 Ma.
Kombolgie Subgroup
sandstone
Unpublished data (RW Page) in Geoscience Australias OZCHRON database. Mentioned in Neumann and Fraser 2007 http://pid.geoscience.gov.au/dataset/ga/65244

Data migrated from OZCHRON1. Original comment: The youngest reliable detrital zircon ages are about 1860 Ma, and this is therefore a maximum depositional age. Other detrital ages are about 1890 Ma, 2300 Ma, and 2400-2500 Ma.
sandstone
Granite Hill, 4 km SSW of Jabiluka 2

Data migrated from OZCHRON1. Original comment: A few grains as young as 1810 Ma suggest this as a possible maximum age for deposition. Other detrital suites are about 1830 Ma (several grains), 1880 Ma, and 2500-2550 Ma - a similar range to that found in other Kombolgie sandstones.
Granite Hill

Data migrated from OZCHRON1. Original comment: This is unreliable maximum age for a metased. within Toole Creek Volcs, based on only 3 concordant analyses. The remainder are very discordant high-U grains with younger 207/206 apparent ages, and a few late Archaean relics (2230-2680 Ma).
Toole Creek Volcanics
pink cherty ?tuff in a sequence of porphyritic mafic volcanic
Mount Isa Region
Eastern Fold Belt. few km northeast of Cloncurry

Data migrated from OZCHRON1. Original comment: This is maximum depositional age of paragneiss, representing similar provenance as 92208020 data. Few younger zircons (1680-1700 Ma) are discordant, but may point to a younger max. age. Other detrital ages: 1750-1770 Ma, 2520-2565 Ma.
Gandry Dam Gneiss
altered, albitic muscovite gneiss

Data migrated from OZCHRON1. Original comment: All grains show sedimentary pitting. There is a wide range of ages, from ~3300 Ma to 1560+-22 Ma. 16 grains concentrate at 1624+-12 Ma. Deposition of the sedimentary precursor postdates 1560+-22 Ma.
Astrea Formation
light grey very fine laminated slate
Coen Region
Unpublished data (LP Black) in Geoscience Australias OZCHRON database. Mentioned in Neumann and Fraser 2007 http://pid.geoscience.gov.au/dataset/ga/65244

Masson Formation
quartz-rich sandstone, South Alligator Conservation Zone

Mundogie Sandstone
pebbly sandstone with faint cross beds, South Alligator Conservation Zone

Data migrated from OZCHRON1. Original comment: 'This is age of HG metamorphism from 9 high-U met'c rims (anals 5732-5740). Low-U cores (5741-5748) are 1872+/-9 Ma, and other cores in this paragneiss are 2007 to 2513 Ma.' source=ozchron-2011-08
Halls Creek Group
migmatite
King Leopold Region

Data migrated from OZCHRON1. Original comment: 'From the 52 detrital zircon analyses, 1910 Ma is a maximum age for the deposition. Other detrital components are at about 1970 Ma, 2050-2200 Ma, 2300 Ma, 2400-2500 Ma - reflecting late Archaean-Palaeoproterozoic provenance terrains.' source=ozchron-2011-08
Olympio Formation
clastic sediment
King Leopold Region

Data migrated from OZCHRON1. Original comment: 'This is a maximum depositional age for the Saunders Creek Fmn. The actual stratigraphic age is much younger (1910-1880 Ma). There are many other detrital ages groupings: 2680 Ma, 3330 Ma, 3530 Ma, 3590 Ma reflecting the unit's early-late Archaean sources.' source=ozchron-2011-08
Saunders Creek Formation
arkose
Saunders Creek Dome, 500m southeast of Bulman Waterhole

Data migrated from OZCHRON1. Original comment: This is the zircon crystallisation age of the rhyolite pebble. It is therefore a maximum for the depositional age of the unit. It is based on 23 analyses. Grain 44 is excluded (1846 Ma xenocryst).
West Branch Volcanics
porphyritic rhyolite pebbles, identical to 91779016

Australian National University
Peryhumuck Formation
calc-albitite metasiltstone, Peryhumuck Fm
Brown-pale grey, layered, medium to fine-grained calcalbitic rock. This sample displays an inequigranular sutured granoblastic metamorphic texture. Albite is abundant, forming anhedral ragged grains that form an inequigranular sutured mosaic throughout the rock. Minor quartz grains are irregularly distributed through the mosaic. Actinolite forms small to large randomly oriented subhedral to fibrous prismatic grains and aggregates, and uncommon discontinuous veinlet fillings. Diopsidic clinopyroxene forms ragged grains and aggregates that display the characteristic high relief, water-clear pale green colour, and high birefringence of this mineral. Opaques (possibly ?magnetite) form blocky subhedral crystals and aggregates that are irregularly scattered through the rock. Apatite is present in minor amount as small equant subhedral grains. Sphene forms small subhedral to euhedral crystals. Epidote is uncommon, occurring as pleochroic yellow small aggregates. No primary minerals or textures are preserved, but the primary rock may have formed as a calc-silicate feldspathic sediment. Regional metamorphism has caused complete recrystallisation, generating the massive inequigranular sutured granoblastic assemblage of albite + actinolite + diopside + minor quartz + opaques (?magnetite) + trace apatite + sphene + epidote.
Broken Hill Region
Mount Howden
Jagodzinski, E.A., Kositcin, N., Michael, U., Bodorkos, S., 2023, 2023 data release of U-Pb dates for the Curnamona Province in South Australia: advances in the stratigraphy of the Olary Domain. Australian Earth Sciences Convention, Perth, June 2023. Geological Society of Australia Abstracts, Poster.

George Mine Formation
quartz-albite granofels, George Mine Formation
Layered white, medium-grained quartz-albite granofels, interlayered with composite gneiss. This sample displays a sutured granoblastic metamorphic texture with weak foliation. Quartz and plagioclase are abundant: quartz forms equant anhedral weakly strain-shadowed grains and plagioclase forms twinned anhedral grains that form a sutured granoblastic mosaic throughout the rock. Biotite occurs in minor amount as well-shaped plates, pleochroic pale brown to very pale yellow, that are sparsely scattered through the rock and display a preferred orientation (foliation). Muscovite forms uncommon platy flakes. Rutile occurs in trace amount as equant anhedral grains. Zircon is present in significant amount for an accessory phase: most grains display subrounded prism shapes, and some display thin overgrowths on larger cores. This sample is considered to have formed as a quartzo-feldspathic arenaceous sediment, originally composed of subequal quartz and plagioclase clastic grains, with minor detrital clays, and accessory clastic rutile and zircon. Regional metamorphism has caused suturing of felsic grains, and development of new foliated biotite and minor muscovite.
Broken Hill Region
Mulga barite mine area
Jagodzinski, E.A., Kositcin, N., Michael, U., Bodorkos, S., 2023, 2023 data release of U-Pb dates for the Curnamona Province in South Australia: advances in the stratigraphy of the Olary Domain. Australian Earth Sciences Convention, Perth, June 2023. Geological Society of Australia Abstracts, Poster.

Cathedral Rock Formation
basal quartzite, Cathedral Rock Formation
0.5 m thick layer, pale-brown, coarse-grained, feldspathic quartzite interbedded with schists and intruded by small pegmatitic bodies. This sample displays a massive (non-foliated) sutured granoblastic metamorphic texture. Quartz is abundant, forming anhedral lobate grains in a sutured granoblastic mosaic throughout the rock. Plagioclase is less abundant, forming smaller anhedral grains that tend to occur between the quartz grains. Muscovite forms scattered large randomly oriented platy flakes. Rutile is present in significant amount as equant anhedral grains. Zircon forms small subhedral to subrounded grains. Interpretation: This sample is considered to have formed as an arenaceous sediment composed of abundant quartz and lesser plagioclase grains, with accessory rutile and zircon clastic grains, and minor clays. Regional metamorphism caused suturing of the clastic felsic grains, producing a sutured granoblastic assemblage of quartz + plagioclase + minor muscovite. The primary rutile appears to have undergone grain modification, but primary zircon survived essentially unaffected.
Broken Hill Region
about 1 km south of Mulga Bore
Jagodzinski, E.A., Kositcin, N., Michael, U., Bodorkos, S., 2023, 2023 data release of U-Pb dates for the Curnamona Province in South Australia: advances in the stratigraphy of the Olary Domain. Australian Earth Sciences Convention, Perth, June 2023. Geological Society of Australia Abstracts, Poster.

Data migrated from OZCHRON1. Original comment: This zircon crystallisation age (good depositional age) is based on 22 of the 24 data points and has 207/206 grouping within experimental error (MSWD 1.21). Two rejected analyses are discordant.
Wollogorang Formation
green tuffaceous siltstone
BMR Mount Young No. 2 (66.2 m)
Page, R.W., Jackson, M.J., Krassay, A.A., 2000. Constraining sequence stratigraphy in north Australian basins: SHRIMP U-Pb zircon geochronology between Mt Isa and McArthur River. Australian Journal of Earth Sciences, 47(3), 431-459.

Data migrated from OZCHRON1. Original comment: 'Only the most euhedral (immature) zircons were sampled to provide this coherent age for the suite. This is a maximum age for the deposition of this lower part of the Olympio Formation, and is based on 16 data points. Analysis 69-2 is older at 1918 Ma.' source=ozchron-2011-08
Olympio Formation
low-grade metamorphic

Data migrated from OZCHRON1. Original comment: Maximum depositional age of clastic interbed (pinkite rock) within dolomite sequence, Attack Creek Formation.
Attack Creek Formation
Laminated silicieous siltstone. Fine quartz in matrix of calcite-quartz-hematite-chlorite.
Tennant Creek Region
Compston, D.M., 1994, The geochronology of the Tennant Creek Inlier and its ore deposits, Northern Territory. Ph.D. Thesis, Australian National University, 216p.

Data migrated from OZCHRON1. Original comment: Maximum depositional age of quartzite within Hayward Creek Formation, Tomkinson Creek Beds.
Hayward Creek Formation
Mature quartzite composed mainly of rounded quartz grains with a hematite-stained siliceous cement and accessory zircon.
Tennant Creek Region
North of Tennant Creek
Compston, D.M., 1995. Time constraints on the evolution of the Tennant Creek Block, northern Australia. Precambrian Research, 71, 107-129.

Data migrated from OZCHRON1. Original comment: This crystallisation age is also an excellent depositional age for the tuff, and is based on all 25 data points (MSWD 0.53). Deletion of two very discordant analyses makes no age difference. Excellent agreement with Record 728.
Wollogorang Formation
green tuffaceous siltstone
BMR Mount Young No. 2 (68.3 m)
Page, R.W., Jackson, M.J., Krassay, A.A., 2000. Constraining sequence stratigraphy in north Australian basins: SHRIMP U-Pb zircon geochronology between Mt Isa and McArthur River. Australian Journal of Earth Sciences, 47(3), 431-459.

Data migrated from OZCHRON1. Original comment: This is a zircon crystallisation age for felsic volcanic debris in the conglomeratic arkose. Thus it is a maximum depositional age, but is in agreement with the Tanumbirini Rhyolite age (1713+/-7 Ma). The result is based on all 22 data points.
North Australian Basins Resource Evaluation Project (NABRE)
Nyanantu Formation
arkosic conglomeratic debris, felsic predominantly
Scrutton Range area
Page, R.W., Jackson, M.J., Krassay, A.A., 2000. Constraining sequence stratigraphy in north Australian basins: SHRIMP U-Pb zircon geochronology between Mt Isa and McArthur River. Australian Journal of Earth Sciences, 47(3), 431-459.

Data migrated from OZCHRON1. Original comment: Maximum deposition age of the sandstone
Mount Barren Group
Fine-grained sandstone
Fraser Region
Fine-grained sandstone, No Tree Hill

Kaluweerie Conglomerate
conglomeratic metasandstone, flat lying, even-grained, texturally and compositionally immature, meta
Kaluweerie. 0.5km N of E-W trending qz vein and 3.5km fom sample 142859

Detention Subgroup
This sample of the Detention Subgroup was collected from a quarry near the intersection of Newhaven road with Newhaven track. This is a quite pure (99.05% SiO2), even grained quartzite,
NW Tasmania. Quarry near intersection of Newhaven Road & Newhaven Track.
Black, L.P., Calver, C.R., Seymour, D.B., Reed, A., 2004. SHRIMP U-Pb detrital zircon ages from Proterozoic and Early Palaeozoic sandstones and their bearing on the early geological evolution of Tasmania. Australian Journal of Earth Sciences, 51(6), 885-900.; Black, L.P., Seymour, D.B., Corbett, K.D., Cox, S.E., Streit, J.E., Bottrill, R.S., Calver, C.R., Everard, J.L., Green, G.R., McClenaghan, M.P., Pemberton, J., Taheri, J., Turner, N.J., 1997. Dating Tasmania's oldest geological events. Australian Geological Survey Organisation. Record, 1997/15, 57p.

Jacob Quartzite
This sample, of the relatively pure (98.59% SiO2), even-grained Jacob Quartzite, was collected from a gravel quarry adjacent to the Meunna Hills road.
NW Tasmania. gravel quarry on Meunna Hills road
Black, L.P., Calver, C.R., Seymour, D.B., Reed, A., 2004. SHRIMP U-Pb detrital zircon ages from Proterozoic and Early Palaeozoic sandstones and their bearing on the early geological evolution of Tasmania. Australian Journal of Earth Sciences, 51(6), 885-900.; Black, L.P., Seymour, D.B., Corbett, K.D., Cox, S.E., Streit, J.E., Bottrill, R.S., Calver, C.R., Everard, J.L., Green, G.R., McClenaghan, M.P., Pemberton, J., Taheri, J., Turner, N.J., 1997. Dating Tasmania's oldest geological events. Australian Geological Survey Organisation. Record, 1997/15, 57p.

Ulverstone Metamorphics
This very pure (99.57% SiO2), well sorted quartzite was collected from Picnic Point at Ulverstone.
Dundas Region
NW Tasmania. Picnic Point, Ulverstone
Black, L.P., Calver, C.R., Seymour, D.B., Reed, A., 2004. SHRIMP U-Pb detrital zircon ages from Proterozoic and Early Palaeozoic sandstones and their bearing on the early geological evolution of Tasmania. Australian Journal of Earth Sciences, 51(6), 885-900.; Black, L.P., Seymour, D.B., Corbett, K.D., Cox, S.E., Streit, J.E., Bottrill, R.S., Calver, C.R., Everard, J.L., Green, G.R., McClenaghan, M.P., Pemberton, J., Taheri, J., Turner, N.J., 1997. Dating Tasmania's oldest geological events. Australian Geological Survey Organisation. Record, 1997/15, 57p.

Data migrated from OZCHRON1. Original comment: 'This is a maximum age for the member Pmt3, based on only five detrital zircon grains in the age range 1626-1633 Ma. Other detrital populations: about 1670 Ma, 1750 Ma, 1850 Ma, 2000-2300 Ma, 2780-2950 Ma.'
North Australian Basins Resource Evaluation Project (NABRE)
Termite Range Formation
quartz sandstone wacke
Mount Isa Region
about 7km east of Lawn Hill station. southwestern end of Ploughed Mountain

OZCHRON original comment: 'Only data after the arc dropout (analyses 310.1 onwards) are included in the age calculations. Cathodoluminescence identifies two age populations, at 431.7+-3.3 Ma and 440.0+-4.5 Ma, both of which provide older limits for the formation of this rock.' Lyons et al 2000: SHRIMP U-Pb dating of detrital zircons gave a bimodal distribution, 440 Ma and 432 Ma (L.P. Black, pers. comm., 1998). Thus the maximum age for the Burcher Greywacke is no more than mid-Early Silurian.
Burcher Greywacke
metagreywacke
Lachlan Region
Beside road 36.8 km N of west Wyalong
Lyons, P., Raymond, O.L. & Duggan, M.B. (compiling editors) 2000. Forbes 1:250,000 Geological Sheet SI55-7, 2nd Edition, Explanatory Notes. Australian Geological Survey Organisation, Record 2000/20.

Data migrated from OZCHRON1. Original comment: 'This is the syndepositional age of the tuff's magmatic zircons; MSWD = 0.68. Many of the data are discordant. Other zircon ages in the tuff are 1800-1860 Ma and 1760-1800 Ma.'
Wollogorang Formation
Green tuff, 5 cm, even, unif sharp contacts, same strat pos'n as HC-1 samples 1-5

Data migrated from OZCHRON1. Original comment: A very approximate age only, the error is 1 sigma, and only 6 grains found in the rock. Other detrital ages are 1756, 1822, 1862 Ma.
Lynott Formation
silt layer below the pink tuff
Leila Hill

Original comments: This is a maximum depositional age, based on 21 data points. They do not, however, form a single population in 207/206, but the 8 most concordant are a single pop'n (1659+/-10 Ma) suggesting this is a reliable strat'c age
Toole Creek Volcanics
cherty siliceous sediment in the mafic pile
Eastern Fold Belt. ~18 km east-southeast of Cloncurry

Data migrated from OZCHRON1. Original comment: This is the 207/206 age of one zircon in the shale, hence a maximum age for the sediment. Only a few detrital zircons are present, including one at 1801+/-10 Ma and another at 1901+/-106 Ma. Ages and morphology very diff. from tuff zircons.
Barney Creek Formation
non tuffaceous shale, shale at 66 metres
At HYC mine
Page, R.W., Sweet, I.P., 1998. Geochronology of basin phases in the western Mt Isa Inlier, and correlation with the McArthur Basin. Australian Journal of Earth Sciences, 45(2), 219-232.

Data migrated from OZCHRON1. Original comment: This maximum depositional age for the feldspathic reworked tuff is based on the two youngest detrital grains in the rock, consistent with 8082. Other detrital age groupings: about 1780 Ma, 1830-1870 Ma, 1940 Ma, 2530 Ma.
Corella Formation
tuffaceous sandstone
1 km west of Mount Morah mine

Oonah Formation
This is a very impure quartzite (79.84% SiO2) that is probably best described as a quartz wacke. It was collected from a turbiditic sequence in the Montana Flats area, adjacent to the Heemskirk road, about 7 km N of Zeehan. The angular to moderately rounded quartz grains in this rock coexist with biotite, muscovite, chlorite and ?limonite.
Dundas Region
NW Tasmania. Heemskirk Road, 1.9 km S of Piney Creek

Mary Metamorphic Complex
Tyennan Group and correlates
This quite pure quartzite (98.86% SiO2) was collected from an old quarry adjacent to the Lyell Highway at the beginning of the walking track to Frenchmans Cap. The angular quartz grains in this rock are fairly poorly sorted.
Tyennan Region
NW Tasmania. Frenchmans Cap walking track carpark, Lyell Highway.

Data migrated from OZCHRON. Original comment: 'There is a distinct range of zircon ages, with groups at 502.6 +/- 4.9 Ma (11 analyses), 430.5 +/- 6.2 Ma (5 analyses) and 416.3 +/- 6.5 Ma. The latter two are only statistically resolvable.' Lyons et al 2000: 'Fossils within the Derriwong Group indicate an age range from Pridoli, possibly as early as Ludlow (Late Silurian), to Lochkovian (early Early Devonian)."
Derriwong Group
coarse red/grey massive sandstone
Lachlan Region
Grenfell/Parkes. Weerona
Lyons, P., Raymond, O.L. & Duggan, M.B. (compiling editors) 2000. Forbes 1:250,000 Geological Sheet SI55-7, 2nd Edition, Explanatory Notes. Australian Geological Survey Organisation, Record 2000/20.

Data migrated from OZCHRON. Original comment: '40 of the 43 analyses yield an age of 431.1+-6.7 Ma, which should provide an older limit for the deposition of this sandstone.'
Cuga Burga Volcanics
fine- to coarse-grained crystal-lithic rhyolitic volcaniclastic.
Lachlan Region
Lachlan Fold Belt
Black, L. P. 1998. A summary of SHRIMP zircon U/Pb isotopic data for samples from the Dubbo 1:250 000 sheet area. Geological Survey of New South Wales Report GS1998/127. & Meakin N.S. and Morgan E.J. (compilers) 1999. Dubbo 1:250 000 Geological Sheet SI/55-4, 2nd Edition. Explanatory Notes. Geological Survey of New South Wales, Sydney, xvi + 504 pp.

Data migrated from OZCHRON. Original comment: 'All but the two oldest ages are used to derive an age of 432.0+-2.6 Ma for the youngest zircon component in this volcaniclastic rock. The data were obtained on SHRIMP II, and are of higher quality than previously acquired SHRIMP I data.'
Cuga Burga Volcanics
fine- to coarse-grained crystal-lithic rhyolitic volcaniclastic.
Lachlan Fold Belt
Geoscience Australia, 2007. Geoscience Australia SHRIMP U-Pb Geochronology Interim Data Release July 2007. Geoscience Australia, Canberra.

Data migrated from OZCHRON1. Original comment: This is the age of the younger of only two grains (error 1 sigma), has no stratigraphic meaning; the other is 1867 Ma.
Lynott Formation
silt layer above the pink tuff
Leila Hill

Cistern Formation
volcaniclastic sedimentary rock, from a volcanigenic sandstone layer about 500m thick - Cistern F
Hamersley Region
Nelson, DR 1998, 142842: volcaniclastic sedimentary rock, Nunyerry Gap; Geochronology Record 379: Geological Survey of Western Australia, 4p.

Data migrated from OZCHRON1. Original comment: This is a maximum age for the unit, but may be a reasonable depositional age for unit Pmh6 at top of Lawn Hill Formation. Zircon is probably derived from Pmh6 underlying tuffs. Age is based on 26 coherent data points; other detritals 1691 Ma, 1822 Ma.
North Australian Basins Resource Evaluation Project (NABRE)
Constance Sandstone
feldspathic sandstone
about 24km south of Century mine. 1.5km west of the Riversleigh-Lawn Hill track
Jackson, M.J., Sweet, I.P., Page, R.W., Bradshaw, B.E., 1999. The South Nicholson and Roper Groups: evidence for the early Mesoproterozoic Roper Superbasin. IN Bradshaw, B.E. and Scott, D.L. (editors) Integrated Basin Analysis of the Isa Superbasin using Seismic, Well-log and Geopotential Data: An Evaluation of the Economic Potential of the Northern Lawn Hill Platform. Australian Geological Survey Organisation, Record, 1999/19, 36-45.; Page, R.W., Jackson, M.J., Krassay, A.A., 2000. Constraining sequence stratigraphy in north Australian basins: SHRIMP U-Pb zircon geochronology between Mt Isa and McArthur River. Australian Journal of Earth Sciences, 47(3), 431-459.

Data migrated from OZCHRON1. Original comment: This age is given by the youngest two grains in this tuffaceous sediment. It is only a maximum age and is not stratigraphically useful. Other, older detrital zircons are between 1800 and 1880 Ma, about 2000 Ma, and 2390 Ma.
Fish River Formation
green tuffaceous shale
South Nicholson Region
Lawn Hill Platform. at Gorge Creek waterhole

Data migrated from OZCHRON1. Original comment: This immature silty tuff contains sub-rounded zircons; 1 grain is 1653 Ma, thus giving imprecise maximum age. Great majority of detrital grains are older with groups at: 1700-1730 Ma, 1750 Ma, 1800 Ma, 1850-1900 Ma, 2100-2300 Ma, 2500 Ma, 3100 Ma.
Mallapunyah Formation
green tuffaceous siltstone
Georgina Region
Kilgour River area. Point 10 on gamma traverse, on hillside

Data migrated from OZCHRON1. Original comment: This is considered a maximum age for the upper part of the Termite Range Fmn. It is based on 15 sub-concordant data points. It may be the depositional age. Inherited zircons about 1690 and 1870 Ma are also present in the rock.
Termite Range Formation
Dark grey lithic quartz wacke near the top of the Termite Range Formation (Pmt3) has a microfabric with resorbed ?high-temperature quartz (?phenocrysts) in a wispy altered groundmass that resembles altered shard-like material. This gives it a strongly tuffaceous imprint.
Page, R.W., Sweet, I.P., 1998. Geochronology of basin phases in the western Mt Isa Inlier, and correlation with the McArthur Basin. Australian Journal of Earth Sciences, 45(2), 219-232.

Data migrated from OZCHRON. Original comment: '41 of the 42 analyses yield an age of 258.2+-2.2 Ma for the formation of this rock. The outlying analysis is a little younger than the others.'
Illawarra Coal Measures
ash tuff
Sydney Region
F-ply of Ulan seam, Charbon box cut, Illawarra Coal Measures
Black, L. P. 1998. A summary of SHRIMP zircon U/Pb isotopic data for samples from the Dubbo 1:250 000 sheet area. Geological Survey of New South Wales Report GS1998/127. & Meakin N.S. and Morgan E.J. (compilers) 1999. Dubbo 1:250 000 Geological Sheet SI/55-4, 2nd Edition. Explanatory Notes. Geological Survey of New South Wales, Sydney, xvi + 504 pp.

Data migrated from OZCHRON1. Original comment: Maximum age for the deposition of this sediment
Wilthorpe Formation
Coarse-grained fragmental chert, An unusual sedimentary rock containing chert clasts
Nabberu Region
Coarse-grained fragmental chert, Beatty Park Bore

Data migrated from OZCHRON1. Original comment: 'This is a maximum depositional age, and other detrital grains in this tuffaceous sediment have ages of 1765+/-10 Ma (7 grains clustered), and between 1790 and 2480 Ma.'
Lady Loretta Formation
tuffite

Fraser Formation
Tentative correlation with the Rocky Cape Group.
Siltstone and fine-grained quartz sandstone. Tentative correlation with Rocky Cape Group.
King Island Region
Eastern King Island.
Black, L.P., Calver, C.R., Seymour, D.B., Reed, A., 2004. SHRIMP U-Pb detrital zircon ages from Proterozoic and Early Palaeozoic sandstones and their bearing on the early geological evolution of Tasmania. Australian Journal of Earth Sciences, 51(6), 885-900.

Data migrated from OZCHRON1. Original comment: This is emplacement age of McIntosh intrusion, derived from the U-Pb age of 14 concordant zircons (order 1-14) crystallised in leucosome sweat of country rock. Migmatite (#15-38) has maximum age of 1865+/-2 Ma, and 2250 and 2610 Ma grains.
unnamed migmatite
Paramigmatite at contact of McIntosh intrusion.

Data migrated from OZCHRON1. Original comment: 'This is a maximum age for deposition, but is poorly defined because it is based on only six analyses. Other detrital suites in this tuffaceous sediment are about 1770 Ma old, 1970 Ma old, and 2730 Ma old.' The Age_Ma is c. 1650
Lady Loretta Formation
also known as tuff T7

Data migrated from OZCHRON1. Original comment: This is a maximum age for deposition, but is poorly defined because it is based on only six analyses. Other detrital suites in this tuffaceous sediment are about 1770 Ma old, 1970 Ma old, and 2730 Ma old.
Lady Loretta Formation
also known as tuff T7

Data migrated from OZCHRON1. Original comment: This is considered a maximum depositional age, but its agreement with 94779103 suggests it may also be the actual depositional age. It is base on 9 analyses. Inherited grains at 1681 and 1710 Ma are also present in the rock.
Termite Range Formation
Poorly sorted light grey ?tuffaceous siltstone close to the base of the Termite Range Formation (unit Pmt1) about 15 km SE of the Century zinc deposit.
Page, R.W., Sweet, I.P., 1998. Geochronology of basin phases in the western Mt Isa Inlier, and correlation with the McArthur Basin. Australian Journal of Earth Sciences, 45(2), 219-232.

Data migrated from OZCHRON1. Original comment: This age is based on 20 data points from euhedral zircons in the tuffaceous siltstone. It is thus a maximum depositional age, but it could be close to the actual age. Older detrital grains are 1646 Ma (same as tuff 8080), 1689 Ma, 1770 Ma.
Answer Slate
siltstone
south of Cloncurry
Neumann, N.L., 2007. Time-Space evolution of the Mount Isa Inlier and southern McArthur Basin. IN: Neumann, N.L. and Fraser, G.L. (eds). Geochronological synthesis and Time-Space plots for Proterozoic Australia. Geoscience Australia. Record, 2007/06, 52-73.

Data migrated from OZCHRON1. Original comment: This is a reliable crystallisation age for the clast and is based on 11 concordant data points. Five xenocrysts range in age from 1862-2531 Ma.
Mitakoodi Quartzite
conglomerate above the rhyolite
Quamby-Malbon zone; Eastern Fold Belt

Mitakoodi Quartzite
conglomerate
Quamby-Malbon zone; Eastern Fold Belt

Data migrated from OZCHRON1. Original comment: This is strictly a maximum age for deposition of the unit as it is based on only a few grains that were found in the rock. However, the replicate analyses are uniform in 207/206, except for one older grain (202) which is about 1755 Ma old.
Answer Slate
bedded fine-grained cherty tuff and brecciated tuff
Quamby-Malbon zone; Eastern Fold Belt. 2 km NE of Buka Rock, and ~15 km N of Kuridala

Data migrated from OZCHRON1. Original comment: This is a maximum depositional age derived from the four youngest analyses of the zircon suite. The largest detrital age peak is at 1840 Ma and also at 1860-1890 Ma. Other detrital ages: 1940-2000, 2100, 2520, 2690, 3110 Ma.
Quilalar Formation
purple feldspathic sandstone
south of Alhambra station. few metre above 95208061

Data migrated from OZCHRON1. Original comment: This age is common to detritals in the other Quilalar sandstone (95208062) and confirms this as a good maximum depositional age for the unit. Other detrital zircon age peaks at 1840 and 1900 Ma were also in 8062; other ages: 2200, 2540, 2610, 2800 Ma.
Quilalar Formation
south of Alhambra station

Data migrated from OZCHRON1. Original comment: This is the age of the youngest (detrital) zircon population in this paragneiss, and is therefore a maximum age for deposition of this supracrustal sequence. Most detritals are in a suite 1851+/-4 Ma; older zircons 1870, 1910, 1950, 2020, 2560, 2690 Ma.
May Downs Gneiss
banded biotite-rich gneiss with partial melt veins
about 8 km west of Mount Isa

Data migrated from OZCHRON1. Original comment: The ages of zircon in this rock range from about 1600 to 2500 Ma. The deposition of the precursor of this metasediment is likely to have occurred after 1600 Ma.
Holroyd Group
schist
Coen Region
Coen Inlier, North Queensland. Halls Creek, near Pollappa Falls

Data migrated from OZCHRON1. Original comment: The zircons define a complex 1750-1500 Ma history, with other events extending back through 1700 Ma and 1800 Ma, to at least 2100 Ma.
Einasleigh Metamorphics
leucogneiss
Georgetown Region
Einasleigh Region

Data migrated from OZCHRON1. Original comment: The fine-grained zircon of originally igneous origin in this rock has probably been through a sedimentary cycle. All of the 207/206 ages (except for the anomalous 942 Ma for analysis 39.1) should yield maximum ages for this rock.
Einasleigh Metamorphics
leucogneiss
Georgetown Region
Einasleigh Region

Data migrated from OZCHRON1. Original comment: This is rigorously a maximum age for felsic volcanics at Mt Roseby SSE of Dugald River. If these rocks are felsic volcanics, the 18 data points that define the result do provide an igneous and stratc age for this part of Corella Fmn.
Corella Formation
flow-banded porphyritic rhyolite
Eastern Fold Belt. Mt Roseby belt, few km east of Dugald River deposit
Page, R.W., Sun, S-S., 1998. Aspects of geochronology and crustal evolution in the Eastern Fold Belt, Mt Isa Inlier. Australian Journal of Earth Sciences, 45(3), 343-361.

Data migrated from OZCHRON1. Original comment: This tuff is solely populated by detrital (inherited) zircons of the one age at around 1830 Ma. This is a maximum age for deposition. Inheritance of this age was also found in sample 9101 (whose stratigraphic age is 1595 Ma).
Lawn Hill Formation
Lower part of the Lawn Hill Formation, close to the boundary between units Pmh2 and Pmh3 (Bulmung Sandstone Member) of Sweet and Hutton (1982). This fine-grained pale green tuffaceous sedimentary rock is 0.9 m thick, within an intercalated shale/siltstone sequence about 500 m stratigraphically below the Century orebody. It is an epiclastic rock containing reworked lithic fragments in a fine quartzo-feldspathic groundmass altered to carbonate minerals and fine white mica.

Data migrated from OZCHRON1. Original comment: Zircons in this rock range in age from about 1200 to 2700 Ma. Because the majority of these, and especially the youngest grains, bear the imprint of sedimentary pitting, the precursor of this metasediment was deposited after 1148+- 40 Ma
Sefton Metamorphics
meta conglomerate
Coen Region
Coen Inlier, North Queensland. West Claudie River

* have combined 3 different sub-samples and selected youngest constraint (note have doubled age error to 2sigma). Data migrated from OZCHRON1. Original comment: 'This is a very approximate age and the error is 1sigma only. Only 3 grains found in the rock.'; Data migrated from OZCHRON1. Original comment: 'A very approximate age only, the error is 1sigma, and only 6 grains found in the rock. Other detrital ages are 1756, 1822, 1862 Ma.'; Data migrated from OZCHRON1. Original comment: 'This is the age of the younger of only two grains (error 1sigma), has no stratigraphic meaning; the other is 1867 Ma.'
Lynott Formation
pink tuff, 2cm thick
Leila Hill

Data migrated from OZCHRON1. Original comment: This imprecise age is a maximum estimate for the age of this unit. Only a few zircons were found in this rock, and this age represents the youngest. Other inherited grains present have 207/206 ages of ~1950 Ma, 2480 Ma, 2524 Ma.
Killi Killi Formation
very weathered igneous, probably too coarse to be extrusive.
Tanami Region

Data migrated from OZCHRON1. Original comment: This is the maximum depositional age for the unit, and is based on 8 virtually concordant analyses from immature (~euhedral) detrital grains. Another detrital suite of 7 grains is 1950-2125 Ma and these are obviously rounded/abraded.
Killi Killi Formation
tuffaceous sandstone
Tanami Region

Data migrated from OZCHRON1. Original comment: The zircons in this leucogneiss range in age from about 1900 Ma to 2800 Ma. These provide a maximum age estimate for the time of deposition.
quartz-plagioclase-magnetite leucogneiss
East of Fernhill.

Data migrated from OZCHRON1. Original comment: 'This high-grade metapsammite contains a single population of detrital zircons, and this age of 1866 Ma is a maximum age for deposition of the unit.' source=ozchron-2011-08
Tickalara Metamorphics
garnitiferous granulite

Whey Whey Member
Whey Whey Member, Peryhumuck Fm, Ethiudna Subgroup
Grey, coarse-grained muscovite-biotite psammopelitic schist, very deformed, foliated with 5mm-thick, biotite-rich layering. This sample retains a foliated metamorphic texture, modified by retrogressive alteration. Feldspar is moderately abundant, forming anhedral blocky grains of microperthite and twinned albite. Quartz forms anhedral grains. Together the felsic minerals appear to form a more-or-less equigranular coarse-grained granoblastic mosaic. Muscovite forms large plates aligned in the trace of foliation, and pleochroic tan brown to pale yellow biotite flakes also lie in the foliation. Blocky opaque crystals (?magnetite) are sparsely scattered through the rock. Fine-grained sericite is moderately abundant, concentrated in subparallel diffuse bands composed of tiny sericite flakes and larger euhedral pale yellow epidote crystals, with minor ragged sphene grains. This sample may have formed as a feldspathic sandstone, but most primary textures have been destroyed in response to a dynamic regional metamorphic event which generated the medium-grained foliated granoblastic assemblage of K-feldspar + quartz + plagioclase + muscovite + biotite + minor opaques (?magnetite). At a later time, alteration generated fine-grained dense bands subparallel to the foliation, composed of fine-grained sericite+ epidote + trace sphene.
Adelaide Region
Walparuta area, Olary province

Data migrated from OZCHRON1. Original comment: This is rigourously a maximum age for this part of the Soldiers Cap Group. It is based on a single population of 16 analyses (chi sq 0.92). Inclusion of 9 discordant points does not alter the age. Inheritance between 1740 Ma and 2640 Ma is indicated.
Soldiers Cap Group
recrystallised fine cherty felsic volcanic, screen in Saxby Granite
Eastern Fold Belt. Foxes Creek

Data migrated from OZCHRON1. Original comment: This is the age of the youngest detrital zircon group, and therefore is a maximum age for deposition. Other detrital components are 1733+/-8 Ma, 1765+/-25 Ma, and one grain is 2452 Ma old.
Soldiers Cap Group
feldspathic garnetiferous schist, possibly tuffaceous
Eastern Fold Belt. eastern side of main ridge at Fairmile deposit
Page, R.W., Sun, S-S., 1998. Aspects of geochronology and crustal evolution in the Eastern Fold Belt, Mt Isa Inlier. Australian Journal of Earth Sciences, 45(3), 343-361.

Data migrated from OZCHRON1. Original comment: This is a maximum depositional age for the immature ?tuffaceous sediment, and is based on 16 data points, generally euhedral zoned grains. Another main group of detrital grains is close to 1720 Ma, based on 38 of 43 points. Older detritals: 1770, 2674 Ma.
Soldiers Cap Group
porphyroblastic feldspathic psammite, ?tuffaceous
Eastern Fold Belt. about 3 km north of Mount Ulo

Data migrated from OZCHRON1. Original comment: Maximum depositional age of altered mineralised Warramunga Formation at the Eldorado deposit.
Warramunga Formation
Gold ore replacing greywacke, Warramunga Formation. Hematite-chlorite-muscovite-quartz with trace chalcopyrite-pyrite-bismuth-gold-zircon. Eldorado Anomaly 2, drillhole 15.
Eldorado 2 DDH 15
Compston, D.M., 1994, The geochronology of the Tennant Creek Inlier and its ore deposits, Northern Territory. Ph.D. Thesis, Australian National University, 216p.; Compston, D.M., 1995. Time constraints on the evolution of the Tennant Creek Block, northern Australia. Precambrian Research, 71, 107-129.

Data migrated from OZCHRON1. Original comment: This is the igneous crystallisation age of the zircon in the original rhyolite. The age of this rhyolite pebble therefore is a maximum depositional age for the unit.
West Branch Volcanics
porphyritic rhyolite pebbles, identical to 91779016

Data migrated from OZCHRON1. Original comment: 'This metaturbidite contains a single suite of detrital zircons, providing a maximum age for deposition of the unit.' source=ozchron-2011-08
Tickalara Metamorphics
schistose metagreywacke

Data migrated from OZCHRON1. Original comment: ignimbrite. 1831 Ma. 16 grains combine to give an age of 1844+/-12 Ma, but this is probably composed of 2 separate populations, and 9 grains belong to inherited population of 1859+/-7 Ma. Other inheritance ages at 1962 Ma and >= 2000 Ma.
Gimbat Ignimbrite Member
quartz feldspar porphyry, South Alligator Conservation Zone
Jagodzinski, E.A., 1992. A study of the felsic volcanic succession south-east of Coronation Hill: palaeovolcanology, geochemistry, geochronology. Bureau of Mineral Resources, Record, 1992/09, 147p.

Maximum depositional age, defined by two-component mixture modelling of 21 analyses, which yielded clusters at ca 1729 Ma (48%) and ca 1762 Ma (52%)
Whey Whey Member
feldspathic quartzite, Whey Whey Member, Peryhumuck Formation
Thin bed (30 cm) of fine-grained, cross-bedded biotite-muscovite quartzite within coarse-grained pelitic schist. This sample displays a weakly foliated granoblastic metamorphic texture. Quartz is abundant, forming equant anhedral grains in a granoblastic mosaic throughout the rock. Albite is present in lesser amount, forming anhedral grains in cuspate interstitial aggregates between the quartz grains. Many of the albite grains have undergone partial to severe replacement by small sericite flakes. Some slightly larger muscovite flakes are interleaved with pleochroic reddish tan brown to very pale yellow biotite flakes whose preferred orientation defines a weak foliation. Tiny subrounded zircon grains are sparsely scattered through the rock. This sample is considered to have initially formed as a feldspathic arenite composed of abundant quartz grains, lesser plagioclase grains, and a moderate amount of detrital clays and trace zircon grains. Regional metamorphism in the presence of a directed stress regime generated the new foliated assemblage of quartz + plagioclase + muscovite + biotite. The white mica formed in part by replacement of the plagioclase.
Adelaide Region
Walparuta area, Olary province

Bewooloo Member
metasiltstone, Bewooloo Member, Toraminga Fm
Dark grey, laminated, very fine grained, feldspar-rich metasiltstone, with fine laminations; chery and partly albitised. This sample displays a very fine-grained sutured microgranular metamorphic texture. Albite dominates the rock, forming tiny anhedral grains that form a sutured microgranular mosaic throughout the rock. Opaques occur in different forms: i) minute (micron-sized) equant grains are sparsely sprinkled through the rock, and their varied abundance contributes to layering; ii) larger equant crystals are sparsely and irregularly scattered through the rock; iii) minute opaque films are developed around grain margins in diffuse patches up to ~1-2 mm in size. Sericite forms tiny flakes that tend to be concentrated in particular horizons poor in opaques. Quartz is present as uncommon larger grains in pressure shadows at ends of some larger opaque grains. Rutile occurs in trace amount as small deep red granules that are sparsely scattered through the rock. This sample formed as a thinly layered rock, possibly a felsic tuffaceous deposit. It underwent pervasive alteration in response to a regional metamorphic event, generating the fine-grained assemblage of albite + minor opaques+ sericite + quartz + trace rutile.
Adelaide Region
Western Weekeroo Inlier

Mooleulooloo Formation
Page et al. (2005, Econ Geol, p. 663) paraphrased: "Metasedimentary rocks of the Mooleulooloo Formation were sampled [98185019] in order to better define the age of the Mount Howden Subgroup. A weakly laminated, 10-cm-thick, cream coloured layer in feldspathic psammites was sampled near the hinge zone in the southeast limb of the Mount Howden synform, 1.5 km southeast of Mount Howden."
Mount Howden

Data migrated from OZCHRON1. Original comment: This is a maximum depositional age for the sediment, although not precise. Other detrital ages are 1750 and 1774 Ma.
pink ?tuffaceous bands 4cm thick surrounded by biotite schist, same as Garry Davidson's ST204

Data migrated from OZCHRON1. Original comment: All 25 detrital grains from this deformed, meta-sediment range in age from 1200 Ma to 1900 Ma. Deposition therefore occurred no earlier than 1200 Ma.
Bowry Formation
Strongly deformed metasedimentary rock sampled on the S bank of Rocky River, about 10 m from the site of the deformed and altered granitic rock (dated as 93220005) on the N bank. The two rocks are quite difficult to distinguish in outcrop and in hand specimen; however, they are readily distinguishable by thin-section examination and their chemical compositions. The metasedimentary rock contains 89.08% SiO2 and 3.71% Al2O3 (compared to 66.81% and 12.61% respectively for the granite), indicating that the sedimentary precursor was probably an impure quartz sandstone.
South bank of Rocky River, about 10 m from site 93220005.
Black, L.P., 1994. The significance of current and proposed SHRIMP dating. Mineral Resources Tasmania Report, 1994/16, 20p.

Data migrated from OZCHRON1. Original comment: This paragneiss contains a number of different inheritance / provenance ages. Grains between 1830-1850 Ma (average 1840 Ma) provide a maximum age for the sequence. Other inheritance:1860-1900 Ma, ~1930 Ma, ~1990 Ma, 2170 Ma, 2500-2600 Ma.
Double Crossing Metamorphics
weathered coarse ?sillimanite feldspathic gneiss
Eastern Fold Belt. about 8km west of Selwyn mine
Page, R.W., Sun, S-S., 1998. Aspects of geochronology and crustal evolution in the Eastern Fold Belt, Mt Isa Inlier. Australian Journal of Earth Sciences, 45(3), 343-361.

Data migrated from OZCHRON1. Original comment: Only six zircon grains present in this sample. This age is a maximum depositional age for this sericitic schist, but is unreliable and based on only one grain. Other grains show a large uninterpretable spread in ages.
Mount Norna Quartzite
weathered feldspathic sericite schist, ?tuffaceous, 20m north of 8032
Eastern Fold Belt. Monakoff prospect, 20km ENE of Cloncurry

Data migrated from OZCHRON1. Original comment: This U-Pb age for the detrital zircons is a maximum age for the Tommy Creek sequence. It agrees well with the 1626+/-4 Ma age for the igneous rocks in the sequence, and proves this is as young as or younger than cover sequence 3.
Lalor beds
calcareous feldspathic brecciated volcanic
Eastern Fold Belt. Tommy Creek area

Data migrated from OZCHRON1. Original comment: Maximum depositional age of coarse greywacke of the Warramunga Formation at the White Devil mine.
Warramunga Formation
Greywacke, Warramunga Formation. Angular quartz-plagioclase-chert clasts in matrix of foliated chlorite-sericite-quartz. Trace magnetite-zircon.
White Devil DDH 146
Compston, D.M., 1995. Time constraints on the evolution of the Tennant Creek Block, northern Australia. Precambrian Research, 71, 107-129.; Compston, D.M., 1994, The geochronology of the Tennant Creek Inlier and its ore deposits, Northern Territory. Ph.D. Thesis, Australian National University, 216p.

Data migrated from OZCHRON1. Original comment: 8 grains yield an age of 501+-9 Ma, which represents an older limit for the deposition of this volcaniclastic rock. 6 other grains delineate a 579+-12 Ma population. Zircons ranging in age from 1000 Ma to 3100 Ma are also present.
Towanway Tuff
Stuart-Smith and Black (1999) described the original sample as 'dacitic crystal lithic volcanic sandstone'. In thin section, this rock is a coarse grained mafic volcaniclastic arenite which comprises ovate feldspar and pyroxene crystals in a highly chlorite altered groundmass of finer feldspar.
Willaura South. Gully, 750 m NE of 'Binbook'
Stuart-Smith, P.G., Black, L.P., 1999. Willaura, Sheet 7422, Victoria, 1:100 000 Map Geological Report. Australian Geological Survey Organisation, Record, 1999/38, 50p.

Data migrated from OZCHRON1. Original comment: 'Reliable age for this tuff in the Breakaway Shale. It is based on 86 data points which are mostly concordant and a tight cluster in 207/206 (chi sq. 1). 3 older detrital grains: 1754, 1788, 1867Ma.
Breakaway Shale
banded tuffac. pink-grey silt, hi gamma
Paroo Range sec 7/ stn 14.2; 12kg

Towanway Tuff
Stuart-Smith and Black (1999) described the original sample as 'dacitic crystal lithic volcanic sandstone'. In thin section, this rock is a coarse grained mafic volcaniclastic arenite which comprises ovate feldspar and pyroxene crystals in a highly chlorite altered groundmass of finer feldspar.
Willaura South. Gully, 750 m NE of 'Binbook'
Lewis, C.J., Cayley, R.A., Duncan, R.J., Schofield, A., Taylor, D.H., 2016. New SHRIMP U-Pb zircon ages from the Stavely region, western Victoria: July 2014-June 2016. Geoscience Australia. Record, 2016/27, 203p.

Data migrated from OZCHRON1. Original comment: 'composite zircon population from igneous lithologies betweenok 3100-3500Ma dep as sediment after 3100Ma with subsequent overgrowth of new zircon in situ ca 2680Ma (virtually every zircon has an isotopically distinct core-rim relationship)' source=ozchron-2011-08
pelitic granulite (OPX-GNT-CRD-BT-QZ) -[informal_name: Mt. Narryer quartzite]-
400m exposure striking 040 approx 3.5km WSW Mt.Dugel
Kinny, P.D., Wijbrans, J.R., Froude, D.O., Williams, I.S., Compston, W., 1990. Age constraints of the geological evolution of the Narryer Gneiss Complex, Western Australia. Australian Journal of Earth Sciences, 37(1), 51-69.

Data migrated from OZCHRON1. Original comment: Maximum depositional age for coarse greywacke of the Warramunga Formation at Eldorado.
Greywacke, Warramunga Formation. Angular quartz-plagioclase chert clasts in matrix of foliated chlorite-sericite-quartz. Trace magnetite-zircon.
Eldorado 2 DDH 15
Compston, D.M., 1995. Time constraints on the evolution of the Tennant Creek Block, northern Australia. Precambrian Research, 71, 107-129.

Data migrated from OZCHRON1. Original comment: The zircons in this leucogneiss mostly range in age from about 2700 Ma to 1900 Ma, which represent maximum values for the time of deposition.
foliated quartz-plagioclase-magnetite leocogneiss
200 m SSW of Frasers Well

Data migrated from OZCHRON1. Original comment: The zircons in this leucogneiss have a large range of ages. Those between 1850 Ma and 2800 Ma are thought to be of detrital origin. Younger grains, especially those forming peaks at about 1567 Ma and 1543 Ma, probably formed within the leucogneiss.
quartz-plagioclase-magnetite leucogneiss
Blacksoil Creek 100 m upstream from junction with Percy River.

Data migrated from OZCHRON1. Original comment: Near concordant analyses yield ages of about 1550 to 1800 Ma (three are considerably older, at 2300-2500 Ma). All define a maximum age for the deposition of this metasediment, which contains only a small quantity of zircon.
Sefton Metamorphics
quartzite
Coen Inlier, North Queensland. North tributary to Sefton Creek

Data migrated from OZCHRON1. Original comment: This is maximum age for deposition of paragneiss formerly part of the Soldiers Cap Group. Based on a group of 16 detrital grains. Youngest 12 are 1672+/-5 Ma. Other detrital group 1715+/-5 Ma. Also 1816, 2368, 2427, 3246 Ma grains.
Gandry Dam Gneiss
biotite-rich quartzofeldspathic psammitic gneiss

Data migrated from OZCHRON1. Original comment: The rock contains only a few xenocrystic zircons, ranging in 207/206 age from 1888 Ma to 2365 Ma. None are reliable ages except as a guide to inheritance ages, and 1888 Ma is a maximum age for volcanism, which probably occurred ~1710 Ma.
Katherine River Group
hematised andesitic lava, amygdaloidal, feldspar phenocrysts
Pietsch, B.A., Plumb, K.A., Page, R.W., Haines, P.W., Rawlings, D.J., Sweet, I.P., 1994. A revised stratigraphic framework for the McArthur Basin, NT. In: Australian Mining Looks North - The Challenges and Choices (ed. Hallenstein, C.P.). 1994 AusIMM Annual Conference, Darwin, 5-9 August 1994. AusIMM. Publications, 5/94, 135-138.

Data migrated from OZCHRON1. Original comment: 'This very immature detrital zircon suite in the gritstone contains mainly euhedral zircon. This maximum depositional age is based on 20 analyses. Grain 20 is younger (1815 Ma) but of no real significance. Grain 17 is ~2530 Ma old.' source=ozchron-2011-08
Olympio Formation
coarse grained weakly metamorphosed

Needles Quartzite
This sample is a very pure, ripple-marked quartzite from a quarry in the Jubilee region of southern Tasmania. Pitting is variably developed on the quartz grains, which are all well rounded.
Tyennan Region
Jubilee region of southern Tasmania.

Maximum depositional age for supracrustal precursor
Gandry Dam Gneiss
The felsic Gandry Dam Gneiss (e.g. Beardsmore et al., 1988) is part of the Soldiers Cap Group in the southern part of the Eastern Fold Belt, and has been metamorphosed to upper amphibolite to granulite facies. The analysed sample is an altered porphyroblastic, garnetiferous felsic gneiss which crops out near Maramungee Creek (Page and Sun, 1998 AJES), and was interpreted by Blake et al. (1983) to represent a minor felsic volcanic component of the paragneiss sequence.
Carpentaria Lowlands Region
Eastern Fold Belt. southwest of Percol Plains, 150 m south of Marramungee Creek.

Data migrated from OZCHRON1. Original comment: Recrystal. volcaniclastic contains a simple zircon suite, based on 30 concordant SHRIMP analyses, reliable age (strictly maximum) for ig. crystallisation and hence this part of stratigraphy. Curved data fit gives same age. Mismapped should be Argilla Fm
weakly brecciated KF-hbl-plag-bio amphibolite?

Data migrated from OZCHRON1. Original comment: Three rather discordant zircon analyses define this very imprecise and somewhat unreliable age, which may be taken as a maximum age for deposition. Other zircons in this schist reflect a provenance (source) about 1750 Ma old.
Mount Norna Quartzite
strongly foliated brown weathered schist
Eastern Fold Belt. 18 km southeast of Cloncurry

Data migrated from OZCHRON1. Original comment: 'This igneous crystallisation age (maximum) is based on 22 concordant data points. Another 15 data points are inherited with an age of 1906+/-3 Ma - the latter have distinctively high Th/U/.' source=ozchron-2011-08
Biscay Formation
Nb tuff
Brockman prospect

The Bullion Schist is a shale-dominated sediment package (now schists) local to the Barrow Creek region 100 km southwest of the Davenport Region and 30 km southwest of the Strezlecki Volcanics dated at 1805 +6/-3 Ma.. The top and base are not exposed and the structural or stratigraphic relationship with adjacent units is unknown. On the basis of lithologies, and tight folding indicating early deformation, it has been tentatively correlated with units of the Arunta Region Lander Package to the south, or with the Warramunga Formation of the Tennant Region to the north. . Smith (2001) attempted to obtain a detrital zircon age spectrum for the Bullion Schist but found insufficient grains in a pelitic schist. The sample used in this study is a rare intercalation of psammite, interpreted as a storm deposit in the otherwise shale-dominated sequence. The detrital zircon age pattern has much in common with Davenport Region sandstone horizons, characterised by 1850-1880 Ma detritus and with a subordinate presence of older Proterozoic and Archaean components, including a prominent grouping at ca. 2600 Ma. The detail of the youngest end of the spectrum shows the dominance of the 1850-1880 Ma group, but also the presence of a sparse younger group that forms a continuum with older grains but extends to younger ages ca. 1830-1850 Ma. The statistically youngest coherent group of 6 grains has an average age of 1833 ± 11 Ma and the youngest individual grain is 1824 ± 10 Ma, giving alternative 95% confidence maximum deposition ages of, respectively, 1844 Ma or 1834 Ma. This youngest component is not the same as the distinctly younger 1800-1820 Ma grains found in higher units of the Hatches Creek Group such as the Coulters Sandstone (probably derived from proximal volcanism of that age). Instead this detrital zircon content identifies the Bullion Schist with the lower Ooradidgie Group, which has youngest zircons in the age range 1830-1850 Ma consistent with derivation from the ca. 1840 Ma contemporaneous felsic volcanism preserved as the Epenarra Volcanics.
Bullion Schist
psammite
Arunta Region
Claoue-Long, J.C., Maidment, D.W., Donnellan, N., 2008. Stratigraphic timing constraints in the Davenport Province, central Australia: A basis for Palaeoproterozoic correlations. Precambrian Research, 166(1-4), 204-218.

Data migrated from OZCHRON1. Original comment: Maximum age for the deposition of this sediment
Ravelstone Formation
Meta-quartz wacke, Disconformably overlies mafic volcanic rocks of Narracoota Fm.
Nabberu Region
Meta-quartz wacke, Murphy Well

Nicker beds
quartz sandstone
Worden, K.E., Carson, C.J., Close, D.F., Donnellan, N., Scrimgeour, I.R., 2008. Summary of results. Joint NTGS-GA geochronology: Tanami Region, Arunta Region, Pine Creek Orogen and Halls Creek Orogen correlatives, January 2005-March 2007. Northern Territory Geological Survey Record, 2008-003, 180p.

The sample comprises three distinct age clusters, a dominant grouping at ~2.50 Ga and two minor groupings at ~3.50-3.32 Ga and ~1.91 Ga. The ~1.91 ga group is made up of euhedral crystals and crystal fragments with preserved faces. Nine analyses on eight grains have the same radiogenic 207Pb/206Pb within analytical uncertainty (MSWD = 1.7), and give a weighted mean age of 1913 +/- 18 Ma. Cross, A.J. and Crispe, A.J., 2007. SHRIMP U-Pb analyses of detrital zircon: a window to understanding the Paleoproterozoic development of the Tanami Region, northern Australia. Mineralium Deposita, 42, 27-50.
Mount Charles Formation
siltstone
Jims Pit - Tanami Corridor
Cross, A.J., Crispe, A.J., 2007. SHRIMP U-Pb analysis of detrital zircon: a window to understanding the Paleoproterozoic development of the Tanami Region, northern Australia. Mineralium Deposita, 42(1-2), 27-50.

Walparuta Formation
Thin (40 cm) boudinaged layer in unit dominated by layered pelite, psammopelite with occasional psammite layers, locally graded. White, foliated, medium-grained quartz-feldspar-mica rock, initially interpreted as metagranite. This sample displays a partly-preserved framework-supported clastic sedimentary texture, modified by moderately strong metamorphic foliation and partial recrystallisation. Quartz forms large equant grains, but some are slightly elongated in the trace of a moderately strong foliation. Plagioclase forms anhedral grains that form a moderately coarse mosaic between the quartz grains. Muscovite occurs as large plates concentrated in thin folia that contribute to the foliation through the rock, but also as small flakes sprinkled through the plagioclase mosaic. Chlorite is subequal in abundance to muscovite, and like that mineral also forms pleochroic green larger plates interleaved with the foliated muscovite, and smaller well-shaped flakes sprinkled through the plagioclase mosaic. Opaques occur in trace amount as small anhedral grains associated with the muscovite-chlorite folia. Tourmaline forms uncommon but well-crystallised stumpy prisms pleochroic in drab greens. This sample is considered to have formed as a framework-supported coarse-grained clastic sediment composed of abundant quartz and feldspar grains, accompanied by lesser detrital clay materials. Dynamic regional metamorphism in the greenschist facies caused partial recrystallisation to form the foliated assemblage of plagioclase + quartz + muscovite + chlorite + trace opaques + tourmaline.
approx 600m north of 5871

Main provenance at 1880-1805 Ma, with other clusters at 2180-2050 Ma, 2480-2430 Ma and 2580-2500 Ma. Youngest 6 grains give 1819 +/- 13, whereas youngest grain is 1804 +/- 24 Ma.
Ware Group and correlatives
Helena Creek sandstone
-[informal_name: Helena Creek sandstone]-
Winnecke Region
Styles Creek area
Worden, K.E., Claoue-Long, J.C., Scrimgeour, I.R., 2006. Summary of results. Joint NTGS-GA geochronology project: Pine Creek Orogen, Tanami Region, Arunta Region and Amadeus Basin, July-December 2004. Northern Territory Geological Survey Record, 2006-006, 68p.

Provenance ranges from ~2940 to 1840 Ma, with most prominent peak at 1880-1840 Ma. Youngest grain: 1826 +/- 22.
Lander Rock Formation
Mount Thomas Quartzite [Lander Rock Beds]
quartz psammite
North Arunta
Worden, K.E., Claoue-Long, J.C., Scrimgeour, I.R., Lally, J.H., 2004. Summary of results. Joint NTGS-GA geochronology project: August 2003-December 2003. Northern Territory Geological Survey, 2004-004, 34p.

Cues Formation
Stevens et al. (2008, AJES) paraphrased: "Potosi-type gneiss in the Cues Formation occurs as lenticular bodies up to 20 m thick and 100 m long, generally associated with metabasic rocks. Laing et al. (1984), Laing (1996) and Stevens & Barron (2002) showed that similar Potosi-type gneiss in the Hores Gneiss was volcanic in origin, on the basis of preserved volcanic textures. Although no such textures have yet been documented from Potosi-type gneiss in the Cues Formation, two samples were studied with the aim of at least determining maximum ages for deposition of the Cues Formation succession. (The most likely alternative origin for Potosi-type gneiss is sandstone incorporating some volcanic detritus.) A Potosi-type gneiss (2002185812) was collected from a body 100 m long and 15 m wide, interlayered with basic granulite in the closure of the Broken Hill Synform. This darkish, medium-grained quartz-feldspar-biotite gneiss with abundant garnet porphyroblasts to 20 mm contains no magmatic zircon, and is therefore unlikely to be magmatic or even dominantly volcaniclastic in origin. Its protolith is more likely to have been an immature sedimentary rock."
Broken Hill Synform, east of Broken Hill township, and ~65 m north of 2002185815.
Stevens, B.P.J., Page, R.W., Crooks, A., 2008. Geochronology of Willyama Supergroup metavolcanics, metasediments and contemporaneous intrusions, Broken Hill, Australia. Australian Journal of Earth Sciences, 55(3), 301-330.

Moyle River Formation
Litchfield Region
Western side of Victoria River Fault.

Wingate, MTD, Bodorkos, S and Bagas, L 2009, 178803: sandstone, drillhole CYDD87, Coyote Mine; Geochronology Record 827: Geological Survey of Western Australia, 5p.

Wildman Siltstone
tuffaceous siltstone
Crater Lake Rd. New rail cutting (Gingers Cut)
Worden, K.E., Claoue-Long, J.C., Scrimgeour, I.R., Lally, J.H., 2004. Summary of results. Joint NTGS-GA geochronology project: August 2003-December 2003. Northern Territory Geological Survey, 2004-004, 34p.

Most inherited cores have ages between 1880 and 1625 Ma, with other analyses at ~2930 Ma, ~2140 Ma, ~2185 Ma, ~2210 Ma, 2320-2305 Ma (2), 2490 Ma and 2520 Ma.
Yaya Metamorphic Complex
This sample is from the Inyalinga Granulite.
Sample from Hill 830.
Scrimgeour, I.R., Kinny, P.D., Close, D.F., Edgoose, C.J., 2005. High-T granulites and polymetamorphism in the southern Arunta Region, central Australia: Evidence for a 1.64Ga accretional event. Precambrian Research, 142(1-2), 1-27.

Dominant provenance at ~1870 Ma, with older grains at 2020-1960 Ma (3), ~2090 Ma, ~2170 Ma, 2540-2460 Ma (3) and ~2660 Ma.
Lander Rock Formation
-[informal_name: Unnamed]- Stratigraphic unit inferred from 1:1M scale Surface Geology of Australia GIS dataset
North Arunta
Worden, K.E., Claoue-Long, J.C., Scrimgeour, I.R., Lally, J.H., 2004. Summary of results. Joint NTGS-GA geochronology project: August 2003-December 2003. Northern Territory Geological Survey, 2004-004, 34p.

The Unimbra Sandstone is the basal unit of the Hatches Creek Group, mapped as overlying the Ooradidgie Group above a regional unconformity. The sample chosen for detrital zircon study is a medium grained quartzite. The Concordia diagram shows the detrital zircon age spectrum to be very simple: it is dominated by grains in the age range ca. 1840-1890 Ma with subordinate older Proterozoic and Archaean populations up to 3000 Ma, including a prominent presence of late Archaean detritus ca. 2500-2700 Ma old. The youngest single grain is imprecisely measured at 1835 ± 40 Ma (2¿) while the next-youngest grain is 1838 ± 16 Ma (2¿), imposing 95% confidence maximum ages of, respectively, 1875 Ma and 1854 Ma. Alternatively, an average calculated from the youngest coherent group of grains extends to 21 analyses with MSWD = 1.7 and a mean age of 1858 ± 6 Ma (95% confidence maximum is 1864 Ma). This detrital age spectrum is not distinguishable from the provenance content in the underlying Warnes Sandstone and is consistent with recycling of Ooradidgie Group sediments into the overlying Unimbra Sandstone. The absence of younger juvenile material could be explained by the fact that the proximal younger volcanism (represented here by the Treasure and ArabuljaVolcanics) commenced after the Unimbra Sandstone was deposited.
Unimbra Sandstone
Davenport Region
Claoue-Long, J.C., Maidment, D.W., Donnellan, N., 2008. Stratigraphic timing constraints in the Davenport Province, central Australia: A basis for Palaeoproterozoic correlations. Precambrian Research, 166(1-4), 204-218.

The detrital zircon age spectrum is essentially identical to that of the underlying Coulters Sandstone, characterised by 1840-1880 Ma detritus with a subordinate presence of older populations to ca. 2600 Ma. The detail of the youngest end of the spectrum shows the dominance of the 1840-1880 Ma group of grains, with the sparse presence of a very few younger detrital grains. Just two grains in the age range 1800-1820 Ma were found (less than 5% of the sandstone content), but they match the slightly more abundant youngest group found in the Coulters Sandstone; a third grain is imprecisely measured and its age could belong to either the <1840 Ma group or the younger population. Grains of 1800-1820 Ma age are expected to be present from erosion and redeposition of the contemporaneous felsic volcaniclastics, but the sediment content is clearly dominated by other detrital inputs.
Errolola Sandstone
Davenport Region
Claoue-Long, J.C., Maidment, D.W., Donnellan, N., 2008. Stratigraphic timing constraints in the Davenport Province, central Australia: A basis for Palaeoproterozoic correlations. Precambrian Research, 166(1-4), 204-218.

This sample of Coulters sandstone was taken a few metres above the top of the Arabulja Volcanics, at a site where dacitic autobreccia and thin-bedded volcanic ash are overlain by medium-grained Coulters Sandstone containing abundant pink clasts derived from the underlying dacite. The sample was chosen to test whether juvenile zircons from the immediately underlying volcanic would appear in the measured detrital zircon age pattern. The Concordia diagram shows the detrital age spectrum to be very similar to that in the underlying Unimbra Sandstone, dominated by 1840-1880 Ma detritus with a subordinate presence of older Proterozoic and Archaean components, including a prominent grouping at ca. 2600 Ma. In addition to the 1840-1880 Ma dominant population, seven grains were found (12% of the spectrum) with younger ages in the range ca. 1800-1820 Ma. Individually these are not precise age constraints, but their ages are consistent with derivation from the immediately underlying 1814 ± 3 Ma Arabulja Volcanics. In detail, the youngest individual grain is 1809 ± 18 Ma while the group of the 7 youngest grains has MSWD = 0.8 and mean age of 1809 ± 6 Ma. These data are consistent with the Coulters Sandstone ultimately deriving from the same provenance as underlying units (perhaps by recycling of earlier sedimentary packages) with the addition of a small component of juvenile material from the contemporaneous felsic volcanism.
Coulters Sandstone
Davenport Region

The rocks at this location are deformed into upright folds but the regional metamorphic grade is greenschist to lower amphibolite facies and the outcrop consists of cleaved siltstones and more massive sandstone beds. A sample of medium-grained sandstone was obtained to study the relationship between zircon ages in the Ngadarunga granite (sample 2008082039) and in country rock unaffected by the granite intrusion. A random sample of 52 ages of detrital zircon grains was measured . The age spectrum is very similar to that found in the granite, with a presence of Archaean grains (including one grain more than 3 Ga old) and progressively increasing abundance towards Proterozoic ages. There is also the same dominance of ages in a continuum from ca. 2.0-1.8 Ga. However, there is some difference in the detail of the youngest end of the age spectrum. In the granite there is a significant presence of zircons in the age range from 1825-1860 Ma, but this component is less evident in the sandstone. The three youngest analyses are a weak constraint because they have low precision and analytical error overlaps the period ca. 1800-1870 Ma; a younger component could be masked within the low precision of these analyses. The youngest 16 zircons in the sediment have individual ages in the range ca. 1830-1900 Ma and reproduce acceptably (MSWD 1.5) about a mean age of 1868 ± 7 Ma, while inclusion of the next-oldest grain introduces excess statistical dispersion.
Lander Rock Formation
Claoue-Long, J.C., Edgoose, C., 2008. The age and significance of the Ngadarunga Granite in Proterozoic central Australia. Precambrian Research, 166(1-4), 219-229.

Tommie Wattie Formation
Within upper pelitic unit, Tommie Wattie Formation
Pale brown, fine-grained metapsammite layer 0.5 m thick. This sample displays a moderately foliated equigranular granoblastic metamorphic texture. Quartz and plagioclase are subequal in abundance, forming equant anhedral small grains that form a granoblastic mosaic throughout the rock. Biotite forms small but well-shaped plates, pleochroic from dark tan brown to straw yellow: their preferred orientation defines a moderate foliation through the rock. Muscovite is less abundant, forming larger plates that are variably oriented with respect to the foliation. Garnet occurs in minor amount as small equant subhedral grains sparsely scattered through the rock. Opaques form small scattered grains. Zircon is uncommon, forming tiny angular to subrounded grains. This sample is considered to have formed as a relatively well-sorted arenaceous sediment, originally composed of abundant crystal clastic fragments (quartz = plagioclase >> zircon) accompanied by minor detrital clays. Complete recrystallisation occurred in response to a low-grade (upper greenschist facies) regional metamorphic event, generating the new foliated granoblastic assemblage of quartz + plagioclase + biotite + minor muscovite + garnet + opaques. Trace primary clastic zircon survived this event.

Prot. Synth. age recalculated from original data. Provenance ranges from 3150 to 1835 Ma, with continuum from 2125 to 1835 Ma, and other peaks at 2210-2165 Ma (7), ~2315 Ma, 2450-2420 Ma (3), ~2495 Ma, 2585-2535 Ma (5), ~2715 Ma, ~2750 Ma, ~2865 Ma and ~3150 Ma. Youngest individual: 1835 +/- 38 Ma.
schist
Arunta South
Cross, A.J., Claoue-Long, J.C., Scrimgeour, I.R., Close, D.F., Edgoose, C.J., 2005. Summary of results. Joint NTGS-GA geochronology project: southern Arunta Region. Northern Territory Geological Survey Record, 2004-003, 61p.

Constantine Sandstone
poorly sorted medium-grained subarkose
1km East of Egina Well
Nelson, DR 1999, 142188: subarkose, Egina Well; Geochronology Record 401: Geological Survey of Western Australia, 4p.

Hermit Creek Metamorphics
Psammitic meta-sediment (mid-upper amphibolite facies)
Litchfield Region
North of Giants Reef Fault. Outcrop

Prot. Synth. age recalculated from original data. Dominant provenance clusters at 1800-1780 Ma and 1830-1810 Ma, with other analyses at ~1750 Ma, 1900-1860 Ma and ~1990 Ma. Age is based on youngest 6 individuals. Youngest individual: 1724 +/- 38 Ma.
Amphibolite facies psammopelites
Worden, K.E., Claoue-Long, J.C., Scrimgeour, I.R., Doyle, N., 2006. Summary of results. Joint NTGS-GA geochronology project: Pine Creek Orogen and Arunta Region, January-June 2004. Northern Territory Geological Survey Record, 2006-005, 39p.

Prot. Synth. Age calculated from six youngest analyses. Dominant provenance cluster at 1890-1840 Ma, with other clusters at ~1680 Ma, 1800-1740 Ma, ~2000 Ma, ~2200 Ma and ~2500 Ma. Age based on 6 youngest individuals. Youngest individual: 1666 +/- 32 MA.
Sandy Blight Quartzite
Sandy Blight quartzite
The sample comprises crystalline metasedimentary quartzite containing a variably defined muscovite foliation. The sample was taken on the northeastern side of a ridge of crystalline quartzite. In the lower parts of the ridge (10 m below where the sample was taken), the outcrop comprises quartz-muscovite phyllite with a bedding-parallel cleavage, with 5-20 cm thick quartzite interbeds. Metamorphic grade appears to be greenschist facies. The transition from interlayered phyllite and quartzite to massive quartzite is abrupt and conformable.
Worden, K.E., Claoue-Long, J.C., Scrimgeour, I.R., Doyle, N., 2006. Summary of results. Joint NTGS-GA geochronology project: Pine Creek Orogen and Arunta Region, January-June 2004. Northern Territory Geological Survey Record, 2006-005, 39p.

Korsh et al 2009: Detrital zircons from 11 samples were analysed by Geoscience Australia using the SHRIMP II machine at Australian National University, Canberra and the SHRIMP B machine at Curtin University, Perth. The preferred interpretation is of 26 individual ages yielding a weighted mean age of 320 +/- 2 Ma for the dominant detriatal zircon population in this rock.
Coramba beds
petrographic unit C
New England Region
Korsch R.J., Adams C.J., Black L.P., Foster D.A., Fraser G.L., Murray C.G., Foudoulis C. & Griffin W.L. (2009) Geochronology and provenance of the Late Palaeozoic accretionary wedge and Gympie Terrane, New England Orogen, Eastern Australia., Australian Journal of Earth Sciences 56, 655-685.

Korsh et al 2009: Detrital zircons from 11 samples were analysed by Geoscience Australia using the SHRIMP II machine at Australian National University, Canberra and the SHRIMP B machine at Curtin University, Perth. A population of 23 Carboniferous individual zircon analyses define an age of 323 +/- 3 Ma.
Coramba beds
lithic sandstone
New England Region
Korsch R.J., Adams C.J., Black L.P., Foster D.A., Fraser G.L., Murray C.G., Foudoulis C. & Griffin W.L. (2009) Geochronology and provenance of the Late Palaeozoic accretionary wedge and Gympie Terrane, New England Orogen, Eastern Australia., Australian Journal of Earth Sciences 56, 655-685.

Surprise Creek Formation
Pink, well-sorted f.g. sandstone, planar-tubular cross-bedded, sampled approx 20m above basal conglomerates
Mellish Park. Western side of Fiery Creek
Neumann, N.L., Southgate, P.N., Gibson, G.M., 2009. Defining unconformities in Proterozoic sedimentary basins using detrital geochronology and basin analysis - An example from the mount Isa Inlier, Australia. Precambrian Research, 168(3-4), 149-166.

Age spectrum is between 2215 and 1610 Ma, with dominant population at 1780-1750 Ma and other clusters at 1710-1690 Ma and 1880-1850 Ma. Youngest concordant grain is used for age. Discordia is defined with intercepts of 1638 +/- 22 Ma and 457 +/- 120 Ma.
Walungurru Volcanics
The sample is a porphyritic or volcaniclastic rock of dacitic composition from the southern Kintore Range (site MR02DJR013). The rock is dark and very fine grained, with quartz and feldspar phenocrysts and flattened possible fiamme or shards. The rock shows apparent flow banding and may have an ignimbritic origin. Previous attempts to date the Walungurru Volcanics (Worden et al., NTGS Record 2006-005) have yielded inherited populations.
western Arunta
Worden, K.E., Claoue-Long, J.C., Scrimgeour, I.R., 2006. Summary of results. Joint NTGS-GA geochronology project: Pine Creek Orogen, Tanami Region, Arunta Region and Amadeus Basin, July-December 2004. Northern Territory Geological Survey Record, 2006-006, 68p.

75 analyses are from ~2585 to 1650 Ma, with dominant clusters at ~1700?1650, ~1810?1790 and ~1870?1840 Ma. The weighted mean age for youngest cluster is 1674?6 Ma (n = 27, MSWD= 0.82)
Warrina Park Quartzite
Quartzite above pebbly unit
Leichhardt River Fault Trough. Oxide Creek
Neumann, N.L., Southgate, P.N., Gibson, G.M., 2009. Defining unconformities in Proterozoic sedimentary basins using detrital geochronology and basin analysis - An example from the mount Isa Inlier, Australia. Precambrian Research, 168(3-4), 149-166.

Moondarra Siltstone
Very fine grained siltstone, rythmites, laminated, thinly bedded
Leichhardt River Fault Trough. Oxide Creek

This sample is the lowest observable sandstone horizon in a transect through the top of the Lander Package sandstones. The detrital zircon age spectrum is illustrated differs significantly from the regional Lander Rock Formation. There are age components in common ¿ from ca. 1840 - 2700 Ma, but the proportions of the populations are distinctly different, and they extend to younger ages. Instead of a single dominant 1840-1880 Ma population and thin presence of older grains, this provenance has ages distributed across several populations, with the youngest group no larger than others, and a prominent age group at ca. 2500 Ma. The age of the youngest individual grain was duplicated and is 1814 ± 36 Ma (2¿), imparting a 95% confidence maximum deposition age of 1854 Ma. There are 5 grains with ages younger than ca. 1820 Ma, and statistical coherence extends to the youngest 7 grains whose mean age is 1821 ± 14 Ma. This gives a distinctly younger maximum age than that of the regional Lander Rock Formation samples. It is evident that this sediment has a provenance with similar age components to that yielding the Lander Rock Formation, but in different proportions, and that it contains an important younger component in the age range 1800-1820 Ma.¿
Claoue-Long, J.C., Edgoose, C., Worden, K., 2008. A correlation of Aileron Province stratigraphy in central Australia. Precambrian Research, 166(1-4), 230-245.

This is the second coarsening-upwards sandstone cycle in a transect and its provenance age spectrum is similar to that of the unit below, with detrital ages distributed across the range ca. 1800-2700 Ma and a prominent population at ca. 2500 Ma. The younger age component ca. 1800-1820 Ma is present, if sparsely represented by just two dated grains, and the maximum deposition age is similar to that of the underlying sample.
Claoue-Long, J.C., Edgoose, C., Worden, K., 2008. A correlation of Aileron Province stratigraphy in central Australia. Precambrian Research, 166(1-4), 230-245.

This is the fifth coarsening-upwards sandstone cycle in a transect and its provenance age spectrum is similar to that of underlying units, with ages distributed across the range ca. 1820-2700 Ma and a prominent ca. 2500 Ma population. The youngest age component is represented by a single dated grain ca. 1820 Ma.
Claoue-Long, J.C., Edgoose, C., Worden, K., 2008. A correlation of Aileron Province stratigraphy in central Australia. Precambrian Research, 166(1-4), 230-245.

Stratigraphically above the Mount Thomas Quartite is pelite of the Pine Hill Formation, which includes two thin sandstone horizons. One of these was sampled and the detrital zircon age spectrum differs significantly from that in the underlying quartzite. A ca. 1790-1820 Ma age component is not present. Instead, the youngest individual zircon is 1832 ± 20 Ma (2¿) and the youngest statistically coherent group of 6 grains has a mean age of 1846 ± 10 Ma. The distribution of the age spectrum across groupings ca. 1830-2700 Ma is similar to that of sandstones underlying the unconformity, with a prominent presence of ca. 2500 Ma grains.
Reynolds Range Group

Cores have a range in age from ~3365 to ~1840 Ma.
migmatitic metasedimentary rock
Sampled from near the northern edge of the Lake Mackay sheet.
Kinny, P.D., Scrimgeour, I.R., 2002. SHRIMP U-Pb geochronology of Arunta Province samples from the Mount Liebig and Lake Mackay 1:250 000 mapsheets. Northern Territory Geological Survey, Technical Note, 2002-015, 21p.

Delny Gneiss
unnamed psammite
The Delny Metamorphics are distributed across central and east-central ALCOOTA, where they comprise a composite unit of metasedimentary, siliciclastic sedimentary rocks and lesser mafic igneous rocks. The metasedimentary succession includes felsic gneiss, biotite-muscovite schist, minor quartzite and rare calc-silicate. Much of the schist and gneiss contains coarse clots of muscovite, interpreted to represent retrogressed andalusite porphyroblasts, and rare sillimanite has been noted. The succession in the sample area is intruded by the similarly deformed Crooked Hole Granite (sampled, but as yet undated). The sample of metasedimentary rock was collected close to the contact with this granite. The Delny Metamorphics in the sample area have a strong northeast-trending, steeply dipping fabric. The succession in the sample area has been metamorphosed to low-pressure, lower amphibolite facies (biotite-muscovite +/- andalusite assemblage), with indications of the grade increasing slightly to the west (through the presence of rare sillimanite). The zircons were analysed to determine a detrital zircon age spectrum.
Carson, C.J., Claoue-Long, J.C., Stern, R.A., Close, D.F., Scrimgeour, I.R., Glass, L.M., 2009. Summary of results. Joint NTGS-GA geochronology project: Arunta and Pine Creek regions, July 2006-May 2007. Northern Territory Geological Survey Record, 2009-001, 77p.

Zircons in leucosome developed in partially melting granulite facies Anira Metamorphics metasediments. Metamorphic age interpreted as crystallisation age of leucosome. Detrital zircons with max dep age from zircon cores.
Anira Metamorphics
Stratigraphic unit inferred from 1:1M scale Surface Geology of Australia GIS dataset
Carson, C.J., Claoue-Long, J.C., Stern, R.A., Close, D.F., Scrimgeour, I.R., Glass, L.M., 2009. Summary of results. Joint NTGS-GA geochronology project: Arunta and Pine Creek regions, July 2006-May 2007. Northern Territory Geological Survey Record, 2009-001, 77p.

Prot. Synth. age recalculated from original data. Concordant analyses yielded age spectrum between 2740 and 1630 Ma, with peaks at ~1800 Ma and ~1860 Ma and a continuum from 2150 to 1930 Ma and clusters at 2500-2400 and ~2720 Ma. One concordant outlier at ~1630 Ma has uncertain origin and cited age is based on six next youngest analyses.
Mount Thomas Quartzite
Strongly foliated crystalline metasedimentary quartzite, Mt Thomas Quartzite? Associated with marble and calc-silicates

Bimba Formation
Weakly weathered (jarosite bearing), quartz-plagioclase-mica psammopelitic schist. This sample displays a medium-grained foliated granoblastic metamorphic texture. Clear quartz and twinned plagioclase form an equigranular sutured granoblastic mosaic throughout the rock. Biotite builds well-shaped large flakes that are pleochroic from reddish brown to straw yellow, and their strong preferred orientation defines a strong foliation through the rock. Muscovite forms large plates similar to biotite, aligned in the trace of the foliation, but it also forms smaller flakes as part of the equilibrium assemblage. Scattered through the rock are blocky to anhedral solution cavities (after ?sulphide) which have been lined or completely filled by very fine-grained dense microgranular yellow jarosite. This sample may have formed as a mixed pelitic arenaceous sediment, but all primary textures have been destroyed by recrystallisation in response to a dynamic regional metamorphic event with associated directed stress regime, probably in the amphibolite facies, producing the foliated granoblastic metamorphic assemblage of quartz + plagioclase + biotite + muscovite + ?sulphide. Subsequent weathering generated jarosite after the minor ?sulphide grains.
Ameroo Hill area

Depositional age calculated from youngest zircon.
Unnamed unit
-[informal_name: Unnamed unit]-
Fiddlers Lake metamorphic complex (informal)
Cross, A., Claoue-Long, J.C., Scrimgeour, I.R., Crispe, A., Donnellan, N., 2005. Summary of results. Joint NTGS-GA geochronology project: northern Arunta and Tanami regions, 2000-2003. Northern Territory Geological Survey Record, 2005-003, 69p.

Data migrated from OZCHRON1. Original comment: 'This age is based on 10 data points, mostly discordant but with recent Pb loss evident (chi-sq. = 1.07). Higher Th/U (altered) zircon grains have scattered older ages.'
Green tuff, ?hematitic, even

Data migrated from OZCHRON1. Original comment: This is a maximum depositional age for the Mullera Formation, and the rock contains older detrital components at 1780-1800 Ma, and 1850-1870 Ma. This is the only sample not to contain a 1680 Ma detrital input.
Mullera Formation
Grey-green carbonaceous siltstone.
BHP DDA 127
Jackson, M.J., Sweet, I.P., Page, R.W., Bradshaw, B.E., 1999. The South Nicholson and Roper Groups: evidence for the early Mesoproterozoic Roper Superbasin. IN Bradshaw, B.E. and Scott, D.L. (editors) Integrated Basin Analysis of the Isa Superbasin using Seismic, Well-log and Geopotential Data: An Evaluation of the Economic Potential of the Northern Lawn Hill Platform. Australian Geological Survey Organisation, Record, 1999/19, 36-45.

Prot. Synth. age recalculated from original data. Concordant analyses yielded age spectrum between 2740 and 1630 Ma, with peaks at ~1800 Ma and ~1860 Ma and a continuum from 2150 to 1930 Ma and clusters at 2500-2400 and ~2720 Ma. One concordant outlier at ~1630 Ma has uncertain origin and cited age is based on six next youngest analyses.
Mount Thomas Quartzite
Strongly foliated crystalline metasedimentary quartzite, Mt Thomas Quartzite? Associated with marble and calc-silicates
Neumann, N.L., Fraser, G.L., 2007. Geochronological synthesis and Time-Space plots for Proterozoic Australia. Geoscience Australia. Record, 2007/06, 216p.

Younger single grain exists at 1628 +/- 26 Ma (2s)
Mount Thomas Quartzite
Strongly foliated crystalline metasedimentary quartzite, Mt Thomas Quartzite? Associated with marble and calc-silicates
Worden, K.E., Claoue-Long, J.C., Scrimgeour, I.R., 2006. Summary of results. Joint NTGS-GA geochronology project: Pine Creek Orogen, Tanami Region, Arunta Region and Amadeus Basin, July-December 2004. Northern Territory Geological Survey Record, 2006-006, 68p.

maximum depositional age for the protolith
Cues Formation
Stevens et al. (2008, AJES) paraphrased: "Potosi-type gneiss in the Cues Formation occurs as lenticular bodies up to 20 m thick and 100 m long, generally associated with metabasic rocks. Laing et al. (1984), Laing (1996) and Stevens & Barron (2002) showed that similar Potosi-type gneiss in the Hores Gneiss was volcanic in origin, on the basis of preserved volcanic textures. Although no such textures have yet been documented from Potosi-type gneiss in the Cues Formation, two samples were studied with the aim of at least determining maximum ages for deposition of the Cues Formation succession. (The most likely alternative origin for Potosi-type gneiss is sandstone incorporating some volcanic detritus.) Sample 2002185803, a Potosi-type gneiss from the Old Coolgardie Tank area, is a dark, medium- to fine-grained quartz-feldspar-biotite gneiss with scattered garnets to 4 mm. It was taken from a small body associated with leucogneiss and abundant metabasic rocks, about 180 m west of amphibolite sample 2002185804."
1 km SE of old Coolgardie tank
Stevens, B.P.J., Page, R.W., Crooks, A., 2008. Geochronology of Willyama Supergroup metavolcanics, metasediments and contemporaneous intrusions, Broken Hill, Australia. Australian Journal of Earth Sciences, 55(3), 301-330.

62 concordant analyses yield ages between ~3050 and 1740 Ma.
Torpedo Creek Quartzite
Pink coloured massive quartzite with no mineral banding, Lower quartzite at base of TCQ
Leichhardt River Fault Trough. Gunpowder North
Neumann, N.L., Southgate, P.N., Gibson, G.M., 2009. Defining unconformities in Proterozoic sedimentary basins using detrital geochronology and basin analysis - An example from the mount Isa Inlier, Australia. Precambrian Research, 168(3-4), 149-166.

The weighted mean age for the youngest 6 grains; a dominant cluster at ~1840-1780Ma and a smaller one at ~1870-1850Ma
Surprise Creek Formation
Pink-grey coloured sandstone, banded, bed thickness=1.5m, Sample above major surface in cliff face
Leichhardt River Fault Trough. Bull Creek Syncline

based on weighted mean of 2 individual young grains out of 74.
Torpedo Creek Quartzite
Pink-grey, medium-fine grained sandstone, ?heavy mineral bands, Sample from 2m thick trough cross-stratified bed
Leichhardt River Fault Trough. Crocodile Waterhole

metamorphosed psammite
Amadeus Region
Beyer, E.E., Hollis, J.A., Whelan, J.A., Glass, L.M., Donnellan, N., Yaxley, G., Armstrong, R., Allen, C.M., Schersten, A., 2013. Summary of results. NTGS laser ablation ICPMS and SHRIMP U-Pb, Hf and O geochronology project: Pine Creek Orogen, Arunta Region, Georgina Basin and McArthur Basin; July 2008-May 2011. Northern Territory Geological Survey Record, 2012-007, 205p.

This is interpreted as the time of igneous crystallisation of the volcanic component within the rock and is considered to approximate the time of deposition of the volcanigenic sediment.
Cleaverville Formation
volcanigenic sedimentary rock from succession of banned iron-fm, ?Cleaverville Formation
Hamersley Region
Nelson, DR 1998, 142830: volcanigenic sedimentary rock, Mount Ada; Geochronology Record 390: Geological Survey of Western Australia, 4p.

Coolbro Sandstone
fine- to medium-grained sandstone
Paterson Region

Nguman Metamorphics
Rennie Metamorphics
The Nguman Metamorphics occur within the Haasts Bluff Domain in MOUNT RENNIE and comprise variably quartzose to feldspathic biotite-muscovite schist and metapsammite, with minor quartzite, mafic amphibolite and tremolite schist. The unit has strong similarities with the Lizard Schist and Ikuntji Metamorphics in MOUNT LIEBIG, and is therefore considered likely to form part of the Iwupataka Metamorphic Complex. The sample is a crystalline quartzite from a succession of interlayered quartzite and quartz-muscovite schist that has a strongly developed north-northeast-dipping foliation. The contact between these sedimentary rocks and an adjacent coarsely porphyritic biotite granite is defined by a near-vertical shear zone (Cross et al., NTGS Record 2004-003).
Southern Arunta
Cross, A., Claoue-Long, J.C., Scrimgeour, I.R., Close, D.F., Edgoose, C.J., 2005. Summary of results. Joint NTGS-GA geochronology project southern Arunta Region. Northern Territory Geological Survey Record, 2004-003, CD, 61p.

The Triassic age for this tuff is unexpected, but unambiguous, and suggests that the sampled rock does not form part of the Areyonga Formation as interpreted, but may belong to a younger succession
Areyonga Formation
tuffaceous siltstone - Areyonga Formation (?)
Tuffaceous siltstone within Areyonga Formation (?)
tentatively assigned to this unit by Youles (1967).
Ringwood copper prospect

This medium-grained sandstone sample is from exposures of bedded sandstones at low metamorphic grade (greenschist facies or below) in the northern Anmatjira Range, about 10 km from granulite-grade and partially-melted equivalents adjacent to metabasite intrusions on Mount Stafford. Detrital zircons in this sample were measured at optimum analytical precision using SHRIMP RG, using long count times on all Pb peaks to maximise the per-spot precision of measured ages. The result is a highly-resolved age spectrum. There is a clear dominance of zircons in the age range ca. 1845-1890 Ma (44% of the sample), and a discontinuous thin presence of older zircons to ca. 2700 Ma with no prominent groupings. The youngest individual zircon grain imparts a 95% confidence maximum deposition age of 1858 Ma, and the youngest statistically-coherent group of 20 grains gives a 95% confidence maximum deposition age of 1869 Ma (Table 1). Importantly, the per-spot precision is sufficient to resolve the dominant 1890-1845 Ma detrital group as not a single crystallisation age, but as dispersed beyond measurement errors indicating that it comes from a diversity of sources formed over a 40 Ma period. Clearly, the provenance of this sediment was dominated by crystalline rocks formed in a thermal event ca. 1890-1845 Ma, with a subordinate presence of earlier Proterozoic and late Archaean components.
Mount Stafford Member

The Weldon Metamorphics on the west side of the Anmatjira Range comprise granulite grade metasediments and are in fault contact with lower grade Lander Rock Formation. The area comprises metabasic and metapelitic rocks with felsic gneisses, intruded by granites. These rocks have experienced two high-grade thermal events. Some metamorphism and anatexis is associated with intrusion of the adjoining Possum Creek Charnockite at ca. 1780-1770 Ma (Collins and Williams, 1995). The area was subsequently re-metamorphosed to granulite grade during the 1600-1580 Ma Chewings Event (Collins and Williams, 1995) which more pervasively affected the southeast Reynolds Range. A psammitic lithology was sampled from a granulite grade exposure of mixed psammitic and pelitic lithologies containing melt segregations. During analysis metamorphic zircon rims were avoided, and probing was confined to zircon cores representing the original detrital zircon content of the metasediment. It comprises a dominant distribution of ages in the age rang eca. 1840-1900 Ma, with subordinate older groupings up to ca. 2700 Ma. The youngest individual zircon is 1836 ± 32 Ma and the mean age of the youngest coherent group of 11 grains is 1871 ± 8 Ma. This provenance pattern is clearly similar to that in unmetamorphosed Lander Rock Formation, and supports the assigment of the Weldon Metamorphics to a Lander Rock Formation protolith. Four analyses overlapped into metamorphic areas of the zircon crystals. In this example they are readily identified on chemical grounds by extreme low Th/U ratios below 0.05 typical of metamorphic zircon. Their apparent ages will be mixtures of core and overgrowths, but their age range from 1799 ± 7 Ma (¿) to 1587 ± 7 Ma (¿) is consistent with metamorphic overprinting extending to the ca. 1600-1580 Ma Chewings Event.
metasedimentary rock

A sample of quartzite 4 m from the psammite 2001082057 was sampled to check the consistency of provenance pattern. The detrital age pattern compares closely with that found elsewhere in unmetamorphosed Mount Thomas Quartzite: distribution of ages across a series of populations in the range ca. 1840-2700 Ma, with a prominent presence of grains ca. 1800-1880 Ma and a youngest coherent group of grains having a mean age of 1816 ± 8 Ma. This pattern and the maximum deposition age both support the findings in the psammite.
Reynolds Range Group
metasedimentary rock

tentatively represents maximum age of deposition
Kurrawang Formation
sandstone, geochron - detrital zircon (max dep age)
Sircombe, K.N., Cassidy, K.F., Champion, D.C., Tripp, G., 2007. Compilation of SHRIMP U-Pb geochronological data Yilgarn Craton, Western Australia, 2004-2006. Geoscience Australia. Record, 2007/01, 182p.

Detrital provenance spectrum between ca 1766?2646 Ma
sedimentary rocks 72683
Big Red Sandstone
-[informal_name: Big Red Sandstone]- Stratigraphic unit inferred from 1:1M scale Surface Geology of Australia GIS dataset
Nongra Region
South central Birrindudu

Zircons from the Bigie Formation were analysed during two SHRIMP sessions. More than 60 grains were analysed during the first session (February 2004, SHRIMP II) to generate a detrital age spectrum. During this session, only grains with surface imperfections were avoided. All analyses were made on zircons from the higher-quality non-magnetic fraction. This approach would have increased the chance of not finding all components of the provenance populations. The second session (May 2004, SHRIMP RG) involved the re-analysis of the youngest grains identified in the first session. These analyses were made in approximately the same place as the original, but with a larger ion beam, longer counting times on 204Pb, 207Pb and background, and more scans, in order to test the age reproducibility of these grains and to determine a more precise maximum age of deposition.
Bigie Formation
The upper Bigie Formation sample from Mistake Creek is a medium-grained, trough cross-bedded quartzo-feldspathic sandstone (2003169027), sampled about 40 m above the central Bigie conglomerate. Beds are about 30 cm thick, and contain heavy mineral bands.
Leichhardt River Fault Trough. Mistake Creek
Neumann, N.L., Southgate, P.N., Gibson, G.M., Mcintyre, A., 2006. New SHRIMP geochronology for the Western Fold Belt of the Mt Isa Inlier: developing a 1800-1650 Ma event framework. Australian Journal of Earth Sciences, 53(6), 1023-1039.

age calculated from youngest two analyses
Mundogie Sandstone
Coarse clastic sediment sampled from a conglomeratic bed.
Kakadu. Outcrop by Kakadu Highway

Peryhumuck Formation
laminated metasiltstone, Peryhumuck Formation
Dark brown, platy laminated metasiltstone. The sample displays a foliated granoblastic metamorphic texture. Small grains of albite and lesser quartz form a fine-grained equigranular mosaic throughout the rock. They possibly represent primary clastic grains, now modified by suturing in response to metamorphic recrystallisation. Foliated flakes of muscovite and lesser pleochroic drab greenish brown biotite form a strong penetrative foliation through the rock. Chlorite forms pleochroic pale green flakes sparsely scattered through the rock, and locally concentrated along foliation-parallel segregation bands with quartz and biotite. Opaques (possibly ?ilmenite) form small lath-like grains, oriented in the trace of the foliation. Epidote occurs as scattered small subhedral granules, grains and local coarser aggregates with chlorite. Zircon occurs as rare tiny rounded grains that appear to be preferentially located in opaque-rich laminae (?primary heavy mineral-rich laminae). Tourmaline forms rare small green grains. This sample is considered to have formed as a fine-grained pelitic sediment, probably composed of small crystal fragments of plagioclase and quartz, with accompanying fine detrital clay materials. The rock underwent recrystallisation in response to a regional metamorphic event in the greenschist facies, generating the foliated assemblage of albite + muscovite + biotite + quartz + chlorite + opaques (?ilmenite) + epidote + trace tourmaline.
Olary

Maximum depositional age, defined by three-component mixture modelling of 15 analyses which yielded clusters at ca 1769 Ma (40%), 1791 Ma (16%) and 1812 Ma (44%).
Walparuta Formation
Thin (30cm) boudinaged layer in unit dominated by layered pelite, psammopelite with occasional psammite layers, locally graded. White, medium grained quartz-feldspar-mica rock, initially interpreted as metagranite. This sample displays a foliated metamorphic texture with partly preserved precursor coarse framework-supported clastic sedimentary texture. Quartz and plagioclase are abundant. Quartz forms equant rounded to anhedral grains distributed uniformly through the rock. Plagioclase forms smaller anhedral grains that form a granoblastic mosaic between the larger quartz grains, but some plagioclase also forms larger anhedral grains moulded on the quartz grains. Muscovite is moderately abundant, as large plates aligned in the trace of penetrative structure (foliation), and also as smaller flakes sprinkled through the plagioclase mosaic. Biotite mostly forms larger plates, similar to the large muscovite plates, and also contributes to the foliation through the rock. Chlorite forms small well-shaped pleochroic green flakes irregularly scattered through the finer-grained mosaic. This sample is considered to have formed as a coarse arenaceous clastic sediment, originally composed of closely-packed grains of quartz and feldspar, accompanied by a moderate amount of detrital clay materials. Regional metamorphism with accompanying directed stress regime caused moderately strong recrystallisation, generating the weakly foliated granoblastic assemblage of plagioclase + quartz + muscovite + biotite + chlorite. Some of the primary clastic texture was preserved.
SE Walparuta Inlier

felsic volcanic and volcaniclastic rocks 74288
Dacite breccia -[informal_name: Gindalbie Domain]-
Dacite breccia, Wild Dog Dam

Plumbago Formation
Page et al. (2005, Econ Geol, p. 663) paraphrased: "Walparuta Creek section: This site is located in the Walparuta inlier, 20 km southwest of the Ameroo Hill location. The gray, graphite-bearing psammopelite [99185534] was sampled from the overturned eastern limb of the Dead Horse synform, about 5 m stratigraphically above the calc-silicate rock of the Bimba Formation. The presence of sillimanite and andalusite is consistent with middle- to upper-amphibolite facies metamorphic grade."
Olary Domain

George Mine Formation
quartz-albite granofels, George Mine Formation
Layered white, quartz-albite granofels, interlayered with composite gneiss. Metamorphic grade is lower to middle amphibolite facies. The rock displays a more-or-less equigranular sutured granoblastic metamorphic texture, with moderate foliation. Felsic minerals dominate the rock, including equant anhedral twinned plagioclase grains, clear anhedral to lobate quartz grains, and minor anhedral K-feldspar grains (microcline). Together the felsic minerals form a sutured granoblastic mosaic. Biotite occurs in minor amount as well-shaped flakes, pleochroic from tan brown to straw yellow, whose preferred orientation defines a foliation through the rock. Muscovite is uncommon, forming larger platy flakes irregularly scattered through the rock. Rutile forms minor anhedral grains, and zircon forms rare small subrounded grains. This sample is considered to have formed as an arenaceous clastic sediment, originally composed of mostly felsic crystal fragments (quartz > plagioclase >> K-feldspar) with minor detrital clays. The rock underwent suturing in response to a low-grade regional metamorphic event (biotite grade, presumably greenschist) of quartz + plagioclase + K-feldspar + biotite + minor muscovite. Most of the rutile and zircon are likely to be of relict primary clastic origin.
Mulga Bore

Prot. Synth. age recalculated from original data. Main provenance cluster at 1910-1840 Ma, with smaller populations at ~1930 Ma, ~2010 Ma, ~2100 Ma, ~2200 Ma and 2500-2450 Ma. Age is based on six youngest grains of main cluster. Single analysis at ~1775 Ma of unknown significance.
metamorphosed psammite
Aileron Province

Korsh et al 2009: Detrital zircons from 11 samples were analysed by Geoscience Australia using the SHRIMP II machine at Australian National University, Canberra and the SHRIMP B machine at Curtin University, Perth. The age estimate for the peak of this sample is 332 +/- 3 Ma (n=5, MSWD=0.69, POE=0.63). This age excludes the youngest individual age of 319 +/- 5 Ma as it deviates from the Gaussian mean by three standard errors/about 15 Ma.
Neranleigh-Fernvale beds
fine grained sandstone
Proserpine Region
Broken Head, south of Byron Bay
Korsch R.J., Adams C.J., Black L.P., Foster D.A., Fraser G.L., Murray C.G., Foudoulis C. & Griffin W.L. (2009) Geochronology and provenance of the Late Palaeozoic accretionary wedge and Gympie Terrane, New England Orogen, Eastern Australia., Australian Journal of Earth Sciences 56, 655-685.

Cleaverville Formation
Nimingarra Formation
Nelson, DR 1998, 143994: quartzite, Kitty's Gap; Geochronology Record 266: Geological Survey of Western Australia, 4p.

Bigie Formation
Reddish-brown, medium-grained feldspathic sandstone with numerous heavy-mineral bands at 386 m in the Hidden Treasure measured section. This level produced a pronounced spike on the gamma-ray log, but it is not related to an obvious lithologic change.
section HT 00/01 @ 257i (hot gamma)
Jackson, M.J., Southgate, P.N., Black, L.P., Blake, P.R., Domagala, J., 2005. Overcoming Proterozoic quartzite sand-body miscorrelations: integrated sequence stratigraphy and SHRIMP U-Pb dating of the Surprise Creek Formation, Torpedo Creek and Warrina Park Quartzites, Mt Isa Inlier. Australian Journal of Earth Sciences, 52(1), 1-25.

3 interpretations of data. Prot. Synthesis age based on youngest six individuals; major provenance is at 1895-1830 Ma, with subordinate modes or individual grains at 2385-2190 Ma (5), 2480-2410 Ma (8), 2530-2495 Ma (8) and 2720-2655 Ma (2).
Madigan beds
Madigan beds = Killi Killi Fm. equiv. at Callie
Cross, A., Claoue-Long, J.C., Crispe, A.J., 2003. Summary of results. Joint NTGS-GA geochronology project: Tanami Region 2001-2002. Northern Territory Geological Survey Record, 2003-006, 39p.

This sample is of ferruginised medium grained sandstone a few metres below the unconformity with the overlying Reynolds Package. It contains a similar range of detrital zircon ages to underlying units, but in slightly different proportions. The youngest age component is represented by 13% of the analysed zircons in the age range 1800-1830 Ma, with the remaining provenance spectrum similar to that of underlying units in having ages distributed across several populations ca. 1840-2700 Ma and a prominent ca. 2500 Ma group. The age of the youngest individual grain was duplicated and has a mean of 1795 ± 2 Ma (2¿), imparting a 95% confidence maximum deposition age of 1807 Ma, while the 13 grains in the youngest population are a statistically coherent group with a mean age of 1808 ± 5 Ma, giving a 95% confidence maximum deposition age of 1813 Ma.¿¿¿

Provenance ranges from 2940 to 1840 Ma, with most prominent peak at ~2500 Ma and a less prominent grouping between 1980 and 1840 Ma. Youngest grain: 1811 +/- 42.
quartz psammite
Wabudali Range

Prickle Hill"" sandstone
Prickle Hill Sandstone
Medium- to coarse-grained, poorly sorted, foliated metasandstone, intruded locally by pegmatite and regionally by granite (including a dated sample of granite ENE of Mount Davidson: GA 2001082550, NTGS NA01MG140).
North Arunta
Cross, A., Claoue-Long, J.C., Scrimgeour, I.R., Crispe, A., Donnellan, N., 2005. Summary of results. Joint NTGS-GA geochronology project: northern Arunta and Tanami regions, 2000-2003. Northern Territory Geological Survey Record, 2005-003, 69p.

The 207Pb/206Pb ratio for the session is scattered slightly beyond acceptable dispersion (1.357 for 70 observations), as measured by repeat analyses of QGNG. A scatter of about this magnitude will also apply to the 207Pb/206Pb ratios of the unknowns.
Hermit Creek Metamorphics
Mid-upper amphibolite facies metasediment
Litchfield Region
13km south of Mulluk Mulluk Billabong. Outcrop by track
Worden, K.E., Claoue-Long, J.C., Scrimgeour, I.R., Doyle, N., 2006. Summary of results. Joint NTGS-GA geochronology project: Pine Creek Orogen and Arunta Region, January-June 2004. Northern Territory Geological Survey Record, 2006-005, 39p.

A lithology assigned as metamorphosed Lander Package was sampled where psammitic and pelitic granulites contain garnet- and cordierite-bearing partial melt segregations. Structureless pods of metabasite are also present. During analysis, metamorphic zircon rims were avoided, and probing was targetted at zircon cores representing the original detrital zircon content of the metasediment. The resulting age spectrum is dominated by detrital ages in the range 1840-1880 Ma, with a subordinate presence of older populations to ca. 2700 Ma. It is clearly similar to the provenance spectrum in unmetamorphosed Lander Rock Formation elsewhere and supports the lithologically-based correlation that has been made previously. This dataset is, however, partially compromised by the difficulty of distinguishing inherited from metamorphic zircon ages in a granulite grade metasediment. Four analyses targetted within zircon cores are not different from other anlyses in compositional indicators such as Th/U ratio, but their ages are distinctly young in the range from 1763 ± 6 Ma (¿) to 1800 ± 11 Ma (¿). If accepted as original detrital ages these would indicate deposition after the 1800-1820 Ma Stafford Event, whereas unmetamorphosed Lander Rock Formation were deposited before the Stafford Event. The possibility that these four analyses include a cryptic component of metamorphic alteration cannot be ruled out. If these four young ages are disregarded, the maximum deposition age of the sample is consistent with a correlation to the Lander Rock Formation.
metasedimentary rock

3 interpretations of data. Prot. Synthesis age based on youngest six individuals; major provenance is at 2030-1830 Ma, with subordinate modes or individual grains at 2030-2080 Ma (3), ~2210-2180 Ma (5), 2545-2495 Ma (6), ~2700 Ma and ~3090 Ma.
Drill Core TDH01 110.6-116.6m Titania Prospect
Cross, A., Claoue-Long, J.C., Crispe, A.J., 2003. Summary of results. Joint NTGS-GA geochronology project: Tanami Region 2001-2002. Northern Territory Geological Survey Record, 2003-006, 39p.

Data migrated from OZCHRON1. Original comment: 'This is the age of the main magmatic population in the tuff, based on 22 concordant data points; MSWD = 1.34. Rounded detrital grains are present; one is 2240 Ma old.'
Green tuff, 36cm, even, unif sharp contacts, ~9066,9067 Mt Young 2

Data migrated from OZCHRON1. Original comment: 'Many of the data are discordant, but this is a reliable maximum depositional age based on 19 concordant (of the 41) data points.'
Green tuff, +pink rock, mixed over 1 metre, 70m above other five

Data migrated from OZCHRON1. Original comment: As this is the youngest detrital component, and is the major population in the sediment, then 1680 Ma is a maximum age for deposition. Older detrital populations are 1770 Ma, 1820 Ma, 1880 Ma.
Mullera Formation
Grey carbonaceous siltstone.
BHP DDA 127
Jackson, M.J., Sweet, I.P., Page, R.W., Bradshaw, B.E., 1999. The South Nicholson and Roper Groups: evidence for the early Mesoproterozoic Roper Superbasin. IN Bradshaw, B.E. and Scott, D.L. (editors) Integrated Basin Analysis of the Isa Superbasin using Seismic, Well-log and Geopotential Data: An Evaluation of the Economic Potential of the Northern Lawn Hill Platform. Australian Geological Survey Organisation, Record, 1999/19, 36-45.

Data migrated from OZCHRON1. Original comment: This is the major and youngest detrital zircon population, and therefore is a maximum age for deposition of the Mullera Formation. Older detrital suites are 1780 Ma, 1850-1900 Ma, and 2260 Ma.
Mullera Formation
Grey carbonaceous shale.
BHP DDA 149
Jackson, M.J., Sweet, I.P., Page, R.W., Bradshaw, B.E., 1999. The South Nicholson and Roper Groups: evidence for the early Mesoproterozoic Roper Superbasin. IN Bradshaw, B.E. and Scott, D.L. (editors) Integrated Basin Analysis of the Isa Superbasin using Seismic, Well-log and Geopotential Data: An Evaluation of the Economic Potential of the Northern Lawn Hill Platform. Australian Geological Survey Organisation, Record, 1999/19, 36-45.

Data migrated from OZCHRON1. Original comment: Only four grains were able to be analysed, and this the youngest age analysis, gives a maximum age that is consistent with the 1680 Ma maximum ages derived from five of the Mullera Fmn samples.
Carbonaceous shale with high gamma response.

Data migrated from OZCHRON1. Original comment: This possible maximum age for Mullera Fmn deposition comes from only one analysis, considered reliable. However, the major detrital populations are similar to the other rocks with ages at 1680 Ma, 1780 Ma, and 1840 Ma.
Pyritic grey shale.

Data migrated from OZCHRON1. Original comment: This is an imporatnt detrital age population and is therefore the sediments maximum depositional age. Other provenance domains that have contributed input are about 1780 Ma and 1850 Ma - similar to most of the other Mullera Formation sediments.
Pyritic grey shale.

Quartpot Pelite
foliated paragneiss contains < 40x20 cm mica-rich lenses
3m diameter, 1m high boulder on S side of small rocky hill. ~25m from hill top & ~4km S-SW of Pannikin Bore

Maximum age of deposition (single analysis at 1708 +/- 36 Ma, 2sigma).
Tommie Wattie Formation
metasandstone, Tommie Wattie Formation
Medium-grained metasandstone. This sample displays a equigranular granoblastic metamorphic texture, dominated by quartz and plagioclase. The quartz forms anhedral grains that form sutured patches that possibly represent relict primary clastic grains. Plagioclase forms anhedral grains and microgranular mosaics between the quartz grains. Biotite forms randomly oriented pleochroic dark brown to pale yellow flakes, with a weak tendency to be concentrated along subparallel laminae (possibly relict primary layering). Chlorite forms small randomly oriented green flakes. Opaques form small blocky grains and aggregates; some formed angular grains (?chalcopyrite) that have undergone complete replacement by dense dark red goethite of weathering origin. Sericite forms small ragged flakes sprinkled through the rock. Zoisite occurs as uncommon small equant subhedral grains. Calcite forms uncommon small ragged grains. Zircon occurs in trace amount as small subrounded grains of probable relict primary clastic origin. This sample is considered to have formed as a psammitic sediment composed of abundant quartz and feldspar grains, with minor argillaceous materials. The rock recrystallised under regional metamorphic conditions in the greenschist facies, generating the new assemblage of quartz + plagioclase + biotite + chlorite + sericite+ opaques + trace zoisite + calcite.
NE Weekeroo inlier. vicinity of Whey Whey Creek

gneiss, granulite, migmatite 74310
contains scattered clots of amphibole after pyroxene
saddle between two hill, ~5km N of Dingo Bore

Cathedral Rock Formation
feldspathic quartzite, Cathedral Rock Formation
Pale brown feldspathic quartzite. The sample displays a more-or-less equigranular sutured granoblastic metamorphic texture. Quartz and twinned albite form a sutured granoblastic mosaic throughout the rock, and are considered to represent primary clastic grains modified by grain boundary migration during metamorphic modification. Opaques (probably ?magnetite) form minor scattered subhedral blocky crystals. Muscovite occurs in trace amount as scattered ragged flakes, and pleochroic tan brown biotite occurs as local small flakes and aggregates. Zircon is present in trace amount as small subrounded to rounded grains of inferred primary clastic origin. This sample is considered to have formed as an arenaceous clastic deposit of quartz and feldspar grains, accompanied by minor zircon grains. Regional metamorphism caused suturing of the quartz and plagioclase grains, accompanied by sparse pervasive development of minor opaques (?magnetite), muscovite and biotite.
Walparuta, Olary province

Walparuta Formation
15 cm thick medium to fine-grained psammite layer interbedded with psammopelitic schist. This sample displays a foliated granoblastic metamorphic texture. Quartz is abundant, forming equant anhedral grains that build a granoblastic mosaic throughout the rock. Many grains are partly elongated in the trace of the foliation. Chlorite is moderately abundant, forming pleochroic green flakes whose strong preferred orientation contributes to definition of a strong penetrative foliation. Biotite occurs in lesser amount as pleochroic brown flakes, in places interleaved with chlorite but elsewhere forming aggregates. Garnet forms equant subhedral crystals whose very pale pink to buff appearance suggests an almandine-rich composition. Opaques (probably ?ilmenite) occur in trace amount as small lath-like crystals embedded in chlorite, biotite and garnet. This sample formed as a clastic sediment of uncertain composition: a siliceous pelitic composition is possible, with moderately abundant clastic quartz accompanied by a moderate amount of detrital clays. Low-grade regional metamorphism (greenschist facies, garnet garnet grade) caused complete recrystallisation to form the foliated granoblastic assemblage of quartz+chlorite+biotite + trace opaques (?ilmenite).
Walparuta area, Olary province

Data migrated from OZCHRON1. Original comment: Maximum age for deposition of the precursor sandstone
Jones Creek Conglomerate
Metasandstone, Cross-bedded
Metasandstone, Jones Creek
Nelson, DR 2000, 118937: metasandstone, Jones Creek; Geochronology Record 465: Geological Survey of Western Australia, 5p.

Oonah Formation
Muscovite-rich quartz wacke, from the east bank of the Heazlewood River. Upper part of the Oonah Formation.
Dundas Region
East bank of the Heazlewood River.
Black, L.P., Calver, C.R., Seymour, D.B., Reed, A., 2004. SHRIMP U-Pb detrital zircon ages from Proterozoic and Early Palaeozoic sandstones and their bearing on the early geological evolution of Tasmania. Australian Journal of Earth Sciences, 51(6), 885-900.

Data migrated from OZCHRON1. Original comment: Estimate of time of metamorphism
Rudall Complex
Garnet microgneiss, Poorly exposed
Paterson Region
Garnet microgneiss, Harbutt Range
Nelson, DR 1996, 112160: garnet microgneiss, Harbutt Range; Geochronology Record 489: Geological Survey of Western Australia, 4p.

Data migrated from OZCHRON1. Original comment: Maximum age of deposition of the sandstone precursor to the quartzite
Mount Barren Group
Metasandstone
Fraser Region
Metasandstone, Barrens Beach

Maximum deposition age defined by youngest grain at 1816 +/- 20 Ma.
Purple green sandstone. May be hematitic/glauconitic.
Nongra Region
South central Birrindudu.

Upper PCO Succession

Welltree Metamorphics
Mid-upper amphibolite facies metamorphism

Maximum depositional age, defined by three-component mixture modelling of the youngest 28 analyses, which yielded clusters at ca 1782 Ma (22%), 1801 Ma (50%) and 1835 Ma (28%).
Oonartra Creek Formation
Oonartra Creek Formation, Raven Hill Subgroup, Saltbush Group
The sample comes from a thin, brown, medium-grained psammite layer interlayered with psammopelitic-pelitic (sillimanite-bearing) schist. This sample displays a foliated granoblastic metamorphic texture. Quartz and plagioclase are abundant, forming equant anhedral grains in a sutured granoblastic mosaic throughout the rock. Biotite forms well-shaped flakes whose preferred orientation defines a moderately strong foliation. Muscovite is less abundant but form relatively large plates, also aligned in the foliation; locally the muscovite is interleaved with biotite. Garnet is present in minor amount as equant anhedral grains that are irregularly scattered through the rock, with a tendency to be more abundant in some horizons than others. Chlorite occurs as minor small pleochroic green flakes that lie in equilibrium texture with adjacent biotite flakes, suggesting all phyllosilicates formed synchronously. Opaques (probably ?ilmenite) occur as tiny grains that tend to be associated with biotite and chlorite. Zircon occurs as tiny subrounded grains. This sample is considered to have formed as an arenaceous (psammitic) sediment composed of clastic grains (quartz, plagioclase, trace zircon) with some detrital clay materials. Regional metamorphism in the middle to upper greenschist facies (garnet grade) caused suturing and recrystallisation, producing the foliated granoblastic assemblage of quartz + plagioclase + biotite + minor muscovite + garnet + chlorite + opaques (?ilmenite).
Mount Mulga Bore area

George Mine Formation
migmatitic paragneiss, George Mine Formation, Wiperaminga Subgroup.
White, medium-grained, quartz-albite (biotite) granofels. This sample displays a sutured granoblastic metamorphic texture. Quartz and plagioclase dominate the rock: quartz forms anhedral lobate grains with mild shadowy strain extinction, and plagioclase forms anhedral twinned grains. Opaques (probably mainly ?magnetite) are disseminated through the rock as small to large subhedral blocky crystals, locally concentrated along planes interpreted to represent primary bedding planes. Muscovite forms scattered large porphyroblastic plates without preferred orientation. Zircon is present in significant amount for an accessory phase, forming small subrounded grains (some with core-and-rim zoned forms): although distributed sparsely through the rock, the zircon grains are loosely concentrated along some of the inferred bedding planes. This sample is considered to have formed as a well-sorted, compositionally mature arenaceous clastic sediment that was originally composed of abundant quartz and lesser plagioclase grains, accompanied by accessory clastic zircon grains. It is possible that some primary clastic Fe-Ti oxide grains were present, but this is difficult to prove. Regional metamorphism caused suturing of the felsic grains, generating the new assemblage of quartz + plagioclase + minor opaques (?magnetite) + muscovite. The pervasive presence of the opaques suggests that some metasomatic modification of the primary rock occurred during this metamorphic event, which locally resulted in concentration of new opaques along precursor bedding planes.
Cathedral Rock, Olary Province

Data migrated from OZCHRON1. Original comment: 'Represents a grouping of 8 concordant analyses from 4 grains - it is a useful maximum age for deposition as the 4 grains are euhedral. Detrital grains in this rock are: 1745, 1785+/-5, 1850, 1870-1880Ma.
Moondarra Siltstone
MFS; very hi gamma alt. shaley, package; 8cm layer
Paroo Range sec 3/ stn 260, 7kg; yellow-br, oxidised

Weighted mean of 6 grains forming a cluster younger than the main group; 66 analyses yield ages from ~2550 to 1645Ma;
Warrina Park Quartzite
White coloured, massive quartzite with pink mineral bands, Sampled above 354m conglomerate associated with valley infill
Leichhardt River Fault Trough. Bull Creek Syncline

Data migrated from OZCHRON. Original comment: 'These detrital zircons yield a spread of ages, with a complex young concentration that can be statistically resolved into 468.8+-6.2 Ma and 481.4+-6.2 Ma ages.'
Wagga Group
quartz metasandstone, horizon in slate and metasandstone
Tallimba Road adjacent to Spackmans Lane Turnoff
Geoscience Australia, 2007. Geoscience Australia SHRIMP U-Pb Geochronology Interim Data Release July 2007. Geoscience Australia, Canberra.

Maximum depositional age, derived via two-component mixture modelling of the youngest 18 analyses which yielded clusters at ca 1726 Ma (20%; interpreted as a maximum depositional age) and ca 1750 Ma (80%; interpreted as a provenance cluster).
Ethiudna Subgroup
albite-rich rock veining the Montstephen Metabasalt. This sample forms part of a coarse-grained albite + actinolite matrix at brecciated contact between albitised amphibolite and metasediment. This sample displays an inequigranular or patchy granoblastic alteration texture. Albite dominates the rock, and occurs in two forms: i) Some albite occurs as tiny ragged grains that form dense sutured microgranular granoblastic mosaics in diffuse patches up to several millimetres in size. This albite has the appearance of representing altered host rock. ii) Much albite occurs as larger subhedral prisms of random orientation, which appear to be concentrated in indistinct patches, bands or veins. These albite crystals contain diffuse clouds of tiny fluid inclusions, consistent with crystallisation in the presence of a hydrothermal fluid. Actinolite occurs in minor amount, forming local large (several millimetres long) subhedral pale green prisms concentrated with the coarser-grained albite prisms. Sphene occurs in significant amount for an accessory phase, forming subhedral lozenge-shaped crystals and aggregates. Quartz occurs in minor amount as angular interstitial grains between plagioclase prisms. Apatite occurs in trace amount as local large ragged grains. The primary origin of this sample remains obscure, but it possibly represents an albitised rock which has undergone strong pervasive alteration and veining, resulting in development of patches and veins of albite + actinolite + minor sphene + quartz+ apatite.
Western Weekaroo Inlier

Maximum depositional age, as measured on mount Z3393 during the 3 September 1999 analytical session.
Plumbago Formation
Page et al. (2005, Econ Geol, p. 663) paraphrased: "Mount Howden section: The sample of the Plumbago Formation in the Mount Howden section was taken from a 3- to 5-m-thick, graphitic, laminated metasiltstone directly overlying carbonate units of the Bimba Formation at the Mount Howden cobalt mine. The zircons extracted from this rock (sample 98185016) are encrusted by unevenly thick, discontinuous, altered high-U rims. Some zircon rims form thick, bulbous edges that distort the grain shapes. Elsewhere in the Curnamona province, such high-U metamorphic rims have been shown to have formed at ca. 1600 Ma (e.g., Page and Laing, 1992)." This sample displays a fine-grained weakly foliated metamorphic texture, modified by sericitic overprinting. Quartz is moderately abundant, forming small clear anhedral grains that form a granoblastic mosaic throughout the rock. Sericite forms small randomly oriented flakes which are concentrated in ragged patches between the quartz grains: the sericite appears to have replaced a precursor interstitial phase (eg ?plagioclase). Opaques (?graphite) are moderately abundant, forming small randomly oriented flakes that are distributed more-or-less uniformly throughout the rock. Biotite is present as pleochroic drab brown flakes whose preferred orientation defines a weak foliation: the drab yellow-brown colour of the flakes suggests they have suffered mild modification in response to alteration. This sample is considered to have formed as a fine-grained carbonaceous pelitic sediment. It has suffered complete recrystallisation in response to a regional metamorphic event, generating the new weakly foliated assemblage of quartz + ?plagioclase + opaques (?graphite) + biotite. Subsequent retrogressive alteration generated fine-grained randomly oriented sericite after the precursor ?plagioclase.
Mount Howden

Main group of zircons define continuum between ~1810 and 1980 Ma; other provenance at ~2000 Ma, 2200-2100 Ma, 2520-2450 Ma, ~2710 Ma and ~2900 Ma.
Wilson Airstrip
Smith, J., 2001. Summary of results. Joint NTGS-AGSO age determination program 1999-2001. Northern Territory Geological Survey Record, 2001-007, 53p.

Data migrated from OZCHRON1. Original comment: This maximum depositional age is not very reliable, as it is based on only one SHRIMP analysis of a detrital zircon. Other detrital grains have ages of about 1700 Ma, 1760-1780 Ma, 1855 Ma, 2475 Ma.
Riversleigh Siltstone
ash tuff
15m above SBQ - Riversleigh contact

Using a maximum-likelihood mixture-modelling approach (Sambridge and Compston, 1994), Martin et al. (2007) determined a maximum depositional age of 1785 +/- 7 Ma from the same data.
Irregully Formation
Sample GSWA 152954 was taken from a thin, massive to planar-laminated, dolomitic sandstone bed close to base of the Irregully Formation, approximately 6 km south-southwest of Minnie Springs. This unit is overlain by trough cross-stratified dolomitic litharenite with trough axes aligned approximately north-northeast-south-southwest. The paleocurrent direction at this site is probably similar to that in the underlying Yilgatherra Formation in this area, which was directed to the northeast off a local paleotopographic high (Martin and Thorne, 2004). In thin section, the sample consists of medium- to coarse-grained, sub angular mono- and poly-crystalline quartz, minor K-feldspar, lithic grains comprising hematite and minor quartz, and dololutite clasts in a matrix of dololutite and recrystallised sparry dololutite. There is no detrital tourmaline or zircon in thin section.
Wingate, MTD, Bodorkos, S and Sircombe, KN 2007, 152954: dolomitic sandstone, Minnie Springs; Geochronology Record 696: Geological Survey of Western Australia, 5p.

Martin et al. (2007) derived a maximum depositional age of 1613 +/- 33 Ma from the same data.
Backdoor Formation
Sample GSWA 156541 was taken in the same general vicinity as GSWA 148976, but at a slightly higher stratigraphic level. The sample is of thick bedded, fine-grained quartz sandstone, with a paleocurrent vector mean towards the south.
Bangemall Region
Wingate, MTD, Bodorkos, S and Sircombe, KN 2007, 156541: quartz sandstone, Edney Hill; Geochronology Record 697: Geological Survey of Western Australia, 6p.

Maximum depositional age, defined by two-component mixture modelling of 13 analyses, which yielded clusters at ca 1728 Ma (52%) and ca 1760Ma (48%).
Cathedral Rock Formation
basal quartzite, Cathedral Rock Formation
medium-grained basal quartzite (3m thick, laterally extensive lens). Pale brown, re-crystallised (i.e. internal bedding not visible), coarse-grained, quartzite with feldspathic matrix. This sample displays a sutured granoblastic metamorphic texture, with indistinctly preserved primary clastic sedimentary texture. Quartz is abundant, forming equant anhedral grains with sutured grain boundaries. Tartan-twinned K-feldspar (microcline) is much less abundant, forming anhedral cuspate grains that fill interstices between the quartz grains. Opaques (probably ?magnetite) occur in minor amount as scattered equant blocky crystals. Biotite forms pleochroic tan brown to pale yellow randomly oriented flakes, locally forming small aggregates. Muscovite forms plates which may interleave with biotite, but also form discrete ragged plates and local small finer-grained aggregates. Zircon forms scattered small subrounded to rounded grains whose shapes are consistent with a clastic sedimentary origin. This sample is considered to have formed as an arenaceous sediment composed mostly of quartz, accompanied by minor K-feldspar and trace clays and clastic zircon. Regional metamorphism caused suturing of the clastic felsic grains, generating the new sutured granoblastic assemblage of quartz + K-feldspar + minor opaques (?magnetite) + biotite + muscovite.
Walparuta, Olary province

Data migrated from OZCHRON1 Original comment: Despite fact that these are zoned generally euhedral zircons, it is considered that entire population is derived from a proximal source & this is Maxdep age. Large errors - mixing of older & younger group?
Riversleigh Siltstone
Laminated banded pink silt. (younger), 96/59 McConachie
PC-3, Police Ck - stn 55

Bewooloo Member
metasandstone, Bewooloo Member, Toraminga Formation
Pale brown, thin, medium-grained, flaser and ripple-cross-bedded metasandstone lenses, interbedded with darker brown, fine-grained, micaceous metasandstone. Stratigraphically overlies the Weekeroo amphibolite. This sample displays a fine-grained massive granoblastic metamorphic texture, with indistinct mineralogical lamination. Quartz is abundant, forming tiny equant anhedral grains distributed more-or-less uniformly throughout the rock. Biotite occurs as small but well-shaped flakes, pleochroic from dark reddish tan brown to pale yellow: all are randomly oriented, except for a trace of oriented biotite concentrated along thin discordant quartz-filled fractures. Muscovite forms small flakes, comparable in small size and random orientation to biotite. Some thin laminae and discontinuous lens-like pods are rich in muscovite and devoid of biotite. Garnet is present in significant amount, forming small equant subhedral crystals (probably almandine-rich) that are distributed more-or-less throughout the rock, but locally are loosely concentrated along some biotite-rich laminae. Accessory small opaque grains are sparsely and irregularly scattered through the rock. This sample is considered to have formed as a fine-grained pelitic sediment, composed mostly of tiny quartz particles and detrital clay materials. Primary layering was defined by thin layers and small podiform lenses of subtly different compositions with respect to the clay components. The rock recrystallised in response to a regional metamorphic event, generating the new granoblastic greenschist facies assemblage of quartz + biotite + muscovite + garnet + trace opaques. There is no obvious foliation of the phyllosilicate minerals.
western Weekeroo Inlier

GSQ compilation, 2016 and Original Reference
Surprise Creek Formation
Well-sorted, fine- to medium-grained cross-bedded, feldspathic quartz sandstone, containing numerous heavy-minerals bands, located about 140 m above the base of the Surprise Creek Formation in the Hidden Treasure section.
section HT 00/01 @ 561i
Jackson, M.J., Southgate, P.N., Black, L.P., Blake, P.R., Domagala, J., 2004, Overcoming Proterozoic quartzite sandbody miscorrelations: Integrated Sequence Stratigraphy and SHRIMP U:Pb Dating of the Surprise Creek Formation, Torpedo Creek and Warrina Park Quartzites, Mt Isa Inlier. In: Southgate, P.N., Large, R., Golding, S.D., Kyser T.K., Ord, A., Blake, P.R., 2004, Fluid Flow Modelling in the Mt Isa and McArthur Basins. Final Report to AMIRA P552 (confidential)..

Well-sorted, fine- to medium-grained cross-bedded, feldspathic quartz sandstone, containing numerous heavy-minerals bands, located about 140 m above the base of the Surprise Creek Formation in the Hidden Treasure section.
section HT 00/01 @ 561i
Jackson, M.J., Southgate, P.N., Black, L.P., Blake, P.R., Domagala, J., 2005. Overcoming Proterozoic quartzite sand-body miscorrelations: integrated sequence stratigraphy and SHRIMP U-Pb dating of the Surprise Creek Formation, Torpedo Creek and Warrina Park Quartzites, Mt Isa Inlier. Australian Journal of Earth Sciences, 52(1), 1-25.

79 analyses out of 87 used. Dominant cluster 1810-1760Ma and 4 younger individuals modelled to give this age
Gunpowder Creek Formation
Fine-medium grained sandstone, plannar laminated, 30-40m thick bed sampled
Leichhardt River Fault Trough. Crocodile Waterhole

8 individuals are younger than the main range, with a weighted mean 207Pb/206Pb age of 1768 +/- 8 Ma (2s, MSWD = 0.52), interpreted to be the maximum depositional age for the Whitworth Quartzite at Mistake Creek.
Whitworth Quartzite
The Whitworth Quartzite overlies the Bortala Formation and was sampled from a 20 cm-thick bed in the Mistake Creek section (AM/03/02 i=106) where it crops out as pink fine-grained, well-sorted sandstone (2003169025).
Leichhardt River Fault Trough. Mistake Creek
Neumann, N.L., Southgate, P.N., Gibson, G.M., Mcintyre, A., 2006. New SHRIMP geochronology for the Western Fold Belt of the Mt Isa Inlier: developing a 1800-1650 Ma event framework. Australian Journal of Earth Sciences, 53(6), 1023-1039.

Data migrated from OZCHRON1. Original comment: Maximum age for the deposition of this arenite
Mount Leake Formation
Glauconite-bearing arenite
Glauconite-bearing arenite, Bilyuin

Quartpot Pelite
layered heterogeneous paragneiss (diatexite)
150m NE of small rocky hill, ~7km SW of Lucys Bore

Cues Formation
Stevens et al. (2008, AJES) paraphrased: "Potosi-type gneiss in the Cues Formation occurs as lenticular bodies up to 20 m thick and 100 m long, generally associated with metabasic rocks. Laing et al. (1984), Laing (1996) and Stevens & Barron (2002) showed that similar Potosi-type gneiss in the Hores Gneiss was volcanic in origin, on the basis of preserved volcanic textures. Although no such textures have yet been documented from Potosi-type gneiss in the Cues Formation, two samples were studied with the aim of at least determining maximum ages for deposition of the Cues Formation succession. (The most likely alternative origin for Potosi-type gneiss is sandstone incorporating some volcanic detritus.) A Potosi-type gneiss (2002185812) was collected from a body 100 m long and 15 m wide, interlayered with basic granulite in the closure of the Broken Hill Synform. This darkish, medium-grained quartz-feldspar-biotite gneiss with abundant garnet porphyroblasts to 20 mm contains no magmatic zircon, and is therefore unlikely to be magmatic or even dominantly volcaniclastic in origin. Its protolith is more likely to have been an immature sedimentary rock."
Broken Hill Synform, east of Broken Hill township, and ~65 m north of 2002185815.
Bodorkos, S., Fitzherbert, J.A., 2022. Timing and significance of pre-Olarian metamorphism in the Willyama Supergroup, Broken Hill, Australia. Precambrian Research, 378, 106772, 9p.

Redan Gneiss
Stevens et al. (2008, AJES) paraphrased: "The thinly layered gneiss at Love's (1992) GC1 site was resampled from the location 2 km WNW of Redan homestead (note: not east, as stated in Love 1992). Our sample at the GC1 site (Sample 2002185813) is an oligoclase-microcline-quartz-epidote-hornblende-magnetite gneiss ("calc-albitite") with minor sphene and apatite, displaying well developed bedding lamination, like that shown in Stevens & Corbett (1993 figure 4).
Murray Region
Redan homestead area. 2km west of Redan homestead
Stevens, B.P.J., Page, R.W., Crooks, A., 2008. Geochronology of Willyama Supergroup metavolcanics, metasediments and contemporaneous intrusions, Broken Hill, Australia. Australian Journal of Earth Sciences, 55(3), 301-330.

Maximum depositional age, as measured on mount Z3393 during the 12 July 1999 analytical session.
Plumbago Formation
Page et al. (2005, Econ Geol, p. 663) paraphrased: "Mount Howden section: The sample of the Plumbago Formation in the Mount Howden section was taken from a 3- to 5-m-thick, graphitic, laminated metasiltstone directly overlying carbonate units of the Bimba Formation at the Mount Howden cobalt mine. The zircons extracted from this rock (sample 98185016) are encrusted by unevenly thick, discontinuous, altered high-U rims. Some zircon rims form thick, bulbous edges that distort the grain shapes. Elsewhere in the Curnamona province, such high-U metamorphic rims have been shown to have formed at ca. 1600 Ma (e.g., Page and Laing, 1992)." This sample displays a fine-grained weakly foliated metamorphic texture, modified by sericitic overprinting. Quartz is moderately abundant, forming small clear anhedral grains that form a granoblastic mosaic throughout the rock. Sericite forms small randomly oriented flakes which are concentrated in ragged patches between the quartz grains: the sericite appears to have replaced a precursor interstitial phase (eg ?plagioclase). Opaques (?graphite) are moderately abundant, forming small randomly oriented flakes that are distributed more-or-less uniformly throughout the rock. Biotite is present as pleochroic drab brown flakes whose preferred orientation defines a weak foliation: the drab yellow-brown colour of the flakes suggests they have suffered mild modification in response to alteration. This sample is considered to have formed as a fine-grained carbonaceous pelitic sediment. It has suffered complete recrystallisation in response to a regional metamorphic event, generating the new weakly foliated assemblage of quartz + ?plagioclase + opaques (?graphite) + biotite. Subsequent retrogressive alteration generated fine-grained randomly oriented sericite after the precursor ?plagioclase.

Gorge Creek Group
clastic quartz-rich metamorphosed sandstone of Corboy Formation, Corboy Formation

Gorge Creek Group
medium-grained quartz metasandstone at the top of Cundaline Fm
Nelson, DR 1998, 143996: quartzite, Shay Gap; Geochronology Record 268: Geological Survey of Western Australia, 4p.

Warrawoona Group - metamorphosed mafic rocks
clean, c-gr basal quartz metasandstone.
Nelson, DR 1998, 143995: quartzite, Friendly Stranger Mine; Geochronology Record 267: Geological Survey of Western Australia, 4p.

Croydon Group
Poorly exposed and weathered felsic tuffaceous unit
Poorly exposed, low and rubbly outcrop. 1.5km W Cattle Well, 75m NE Yarrie Mine powerline access track
Nelson, DR 1999, 142867: volcaniclastic sedimentary rock, Cattle Well; Geochronology Record 378: Geological Survey of Western Australia, 4p.

Main 1820 to 1770Ma cluster. Mixture modelling suggests populations at 1762+/-18Ma (2s, 16% of analyses) & 1793+/-6Ma (2s, 84%). The younger population, together with the age constraints of the youngest individuals, suggests a max dep age of 1762+/-18Ma
Bigie Formation
The Bigie Formation comprises rift-related immature conglomerates and sandstones, and rests unconformably to disconformably on a variety of older stratigraphic units of the Quilalar Formation and Haslingden Group in the Leichhardt River Fault Trough and Lawn Hill Platform (Derrick 1982; Betts et al. 1999). This sample is from the Mistake Creek section, below a polymict conglomeratic unit, and comprises a medium grained, quartzofeldspathic sandstone containining scattered clay clasts and heavy mineral bands.
Leichhardt River Fault Trough. Mistake Creek
Neumann, N.L., Southgate, P.N., Gibson, G.M., Mcintyre, A., 2006. New SHRIMP geochronology for the Western Fold Belt of the Mt Isa Inlier: developing a 1800-1650 Ma event framework. Australian Journal of Earth Sciences, 53(6), 1023-1039.

5 grains yield 207Pb/206Pb ages younger than the main range, and the weighted mean age for this cluster is 1763 +/- 8 Ma (2s; MSWD = 0.94). This age is interpreted to be the maximum depositional age for the Quilalar Formation at Mistake Creek.
Quilalar Formation
The Quilalar Formation from the Mistake Creek section (AM/03/03 i=180) was sampled from the topset of a 40 cm-thick bed, about 10 m above the contact with the underlying Lochness Formation of the Myally Subgroup, where it crops out as pink coarse- to fine-grained quartzo-feldspathic sandstone (2003169028).

Sunset Pound Sandstone
-[informal_name: Sunset Pound Sandstone]- Stratigraphic unit inferred from 1:1M scale Surface Geology of Australia GIS dataset
Nongra Region
South central Birrindudu

youngest peak of <2200 Ma data, maximum depositional age of protolith
Fog Bay Metamorphics
biotite gneiss
Fog Bay
Carson, C.J., Claoue-Long, J.C., Stern, R.A., Close, D.F., Scrimgeour, I.R., Glass, L.M., 2009. Summary of results. Joint NTGS-GA geochronology project: Arunta and Pine Creek regions, July 2006-May 2007. Northern Territory Geological Survey Record, 2009-001, 77p.

Data migrated from OZCHRON1. Original comment: Maximum age for the deposition of this arenite
Mount Leake Formation
Fine-grained quartzite sandstone
F-grd quartzite sandstone, Murchison River-Fortnum access road

Data migrated from OZCHRON1. Original comment: Maximum age for the deposition of the sedimentary precursor to the arenite
Teague Granite
Correlated to Frere Formation
Fine-grained arenite -[informal_name: Correlated to Frere Formation]-
Fine-grained arenite, Teague Ring Structure

Data migrated from OZCHRON1. Original comment: Maximum age for the deposition of the sedimentary precursor to the shale
Silicified laminated shale, Interbedded with basaltic lavas near base of Killara Formation
Silicified laminated shale, Referendum Bore

Data migrated from OZCHRON1. Original comment: Maximum age for the deposition of the host clastic sediment
Fine lithic conglomerate, Unconformably overlies a siltstone unit, sample 139508 -[informal_name: Correlated to McFadden Formation]-
Savory Region
Fine lithic conglomerate, Phenoclast Hill

Stony Head Sandstone
Mathinna Supergroup
The Stony Head Sandstone is unfossiliferous, but the overlying Turquoise Bluff Slate contains a graptolite of Bendigonian to Darriwilian age (ca 485-460 Ma) (Young and Laurie 1996; VandenBerg and Laurie in Reed 2001). Taken with the age of the youngest detrital zircons, an Early Ordovician age is indicated for the Stony Head Sandstone.
Central Tasmania Region
Stony Head.
Black, L.P., Calver, C.R., Seymour, D.B., Reed, A., 2004. SHRIMP U-Pb detrital zircon ages from Proterozoic and Early Palaeozoic sandstones and their bearing on the early geological evolution of Tasmania. Australian Journal of Earth Sciences, 51(6), 885-900.

Oonah Formation
Badger Head Group
Central Tasmania Region
Badger Head Block. Badger Head

Data migrated from OZCHRON1. Original comment: interpreted age of metamorphism, based on 12 concordant analyses, error t sigma, QGNG, protolith age 1805+/-7 based on 20 concordant analyses
Deep Bore Metamorphics
gneiss
Scrimgeour, I.R., Raith, J., 2001, Some tectonothermal surprises in the Eastern Arunta Province. Annual geoscience exploration seminar (AGES) record of abstracts, 12.; Smith, J., 2001. Summary of results. Joint NTGS-AGSO age determination program 1999-2001. Northern Territory Geological Survey Record, 2001-007, 53p.

Redan Gneiss
Stevens et al. (2008, AJES) paraphrased: "A sample (2002185814) of poorly layered quartz-albite-K-feldspar-magnetite gneiss with minor sphene and secondary muscovite was taken from near Love's (1992) BH22 sample site, about 1.5 km northwest of Redan homestead. This poorly layered albitic sample contains a less complex zircon population, with essentially two age populations of zircons: protolith zircons with metamorphic zircon rims, and discrete metamorphic zircon grains."
Redan homestead area. 1 km north of Redan homestead (approx. Love's location BH-22).

Dominant 1780-1730Ma cluster. Mixture modelling suggests populations at 1748+/-4Ma (2s, 70% of analyses) & 1766+/-7Ma (2s, 30%). The younger is older but within error of the youngest individuals & is interpreted to be the max dep age
This sample from the Quilalar Formation at Jamie Copper was taken from the third cycle of this unit, at ~280 m in Section 3 of Jackson et al. (1990), where it comprises dark-grey, very fine-grained, internally laminated and hummocky cross-stratified sandstone (2003169030).
Leichhardt River Fault Trough. Jamie Creek

9 youngest individual ages form cluster separate from the dominant 1880-1840Ma cluster & weighted mean for this group (MSWD = 0.39) is 1793+/-9Ma (2s) interpreted to be the max depositional age
Mount Guide Quartzite
Grey, poorly sorted, cross bedded, coarse grained pebbly sandstone. Contains clasts of quartz, mudstone, felsic volcanic rock, and black chert.
Leichhardt River Fault Trough. Mount Isa - Cloncurry Road

The weighted mean 207Pb/206Pb age for the youngest cluster is 1779 +/- 4 Ma (2s, n = 27, MSWD = 0.77), interpreted here to be the maximum depositional age for the Lena Quartzite north-east of Lake Moondarra.
Lena Quartzite Member
The Lena Quartzite was sampled southeast of Lake Moondarra, where it crops out as fine- to medium-grained sandstone with low-angle cross-bedding (2003169036). It also contains heavy mineral bands.
Leichhardt River Fault Trough. East of Lake Moondarra

Data migrated from OZCHRON1. Original comment: Maximum age for the deposition of this sediment. 3 groups of zircon ages -other 2 groups of ages represent igneous sources
Thinly laminated quartz siltstone, Unconformably underlies conglomeratic unit -[informal_name: Correlated to Cornelia Formation]-
Savory Region
Thinly laminated quartz siltstone, Phenoclast Hill

Maximum depositional age, as measured on mount Z3671 during the 26 February 2001 analytical session.
Page et al. (2005, Econ Geol, p. 663) paraphrased: "Mount Howden section: The sample of the Plumbago Formation in the Mount Howden section was taken from a 3- to 5-m-thick, graphitic, laminated metasiltstone directly overlying carbonate units of the Bimba Formation at the Mount Howden cobalt mine. The zircons extracted from this rock (sample 98185016) are encrusted by unevenly thick, discontinuous, altered high-U rims. Some zircon rims form thick, bulbous edges that distort the grain shapes. Elsewhere in the Curnamona province, such high-U metamorphic rims have been shown to have formed at ca. 1600 Ma (e.g., Page and Laing, 1992)." This sample displays a fine-grained weakly foliated metamorphic texture, modified by sericitic overprinting. Quartz is moderately abundant, forming small clear anhedral grains that form a granoblastic mosaic throughout the rock. Sericite forms small randomly oriented flakes which are concentrated in ragged patches between the quartz grains: the sericite appears to have replaced a precursor interstitial phase (eg ?plagioclase). Opaques (?graphite) are moderately abundant, forming small randomly oriented flakes that are distributed more-or-less uniformly throughout the rock. Biotite is present as pleochroic drab brown flakes whose preferred orientation defines a weak foliation: the drab yellow-brown colour of the flakes suggests they have suffered mild modification in response to alteration. This sample is considered to have formed as a fine-grained carbonaceous pelitic sediment. It has suffered complete recrystallisation in response to a regional metamorphic event, generating the new weakly foliated assemblage of quartz + ?plagioclase + opaques (?graphite) + biotite. Subsequent retrogressive alteration generated fine-grained randomly oriented sericite after the precursor ?plagioclase.

foliated quartz-rich paragneiss
15x5m lens qtz-rich metased. w discontinuous mica-rich layers. 30m N top of small rocky hill & ~6km W-SW of Erong Springs

Cistern Formation
welded tuff, from vitric tuffaceous layer - Cistern Formation
Nelson, DR 1998, 141936: welded tuff, Red Hill; Geochronology Record 396: Geological Survey of Western Australia, 3p.

Data migrated from OZCHRON. Original comment: '37 of the analyses of these euhedral grains yield an age of 418.8+-2.6Ma, which is the youngest detrital component found in this rock (compare with the ages for anhedral, pitted grains in Records 956 and 957).'
Yellowmans Creek Formation
volcaniclastic sandstone
Lachlan Fold Belt
Black, L. P. 1998. A summary of SHRIMP zircon U/Pb isotopic data for samples from the Dubbo 1:250 000 sheet area. Geological Survey of New South Wales Report GS1998/127. & Meakin N.S. and Morgan E.J. (compilers) 1999. Dubbo 1:250 000 Geological Sheet SI/55-4, 2nd Edition. Explanatory Notes. Geological Survey of New South Wales, Sydney, xvi + 504 pp.

Data migrated from OZCHRON. Original comment: '40 of the 42 analyses yield an age of 257.3+-2.2 Ma for the formation of this rock. The two outlying analyses are a little younger than the others.'
Illawarra Coal Measures
ash tuff
Sydney Region
c-marker, Ulan open cut

The near concordant analyses range in age from about 1700 Ma to 2400 Ma. These detrital grains provide a maximum age limit for the deposition of this rock.
Daniel Creek Formation
felsic epiclastic rock
In Bernecker Creek, 52 km SW of Kidston

Using a maximum-likelihood mixture-modelling approach (Sambridge and Compston, 1994), Martin et al. (2007) determined a maximum depositional age of 1733 +/- 12 Ma from the same data.
Gooragoora Formation
Sample GSWA 148970 was taken from a unit of very thick bedded, trough cross-stratified, medium-grained quartz sandstone, approximately 1.8 km north-northwest of Carnoby Well. The sample is moderately fresh, with feldspars altered to clay minerals, and scattered heavy minerals preserved. There are no paleocurrent indicators preserved at this site, but the regional paleocurrent vector mean of the Gooragoora Formation is towards the south.
Bangemall Region
Wingate, MTD, Bodorkos, S and Sircombe, KN 2007, 148970: quartz sandstone, Carnoby Well; Geochronology Record 687: Geological Survey of Western Australia, 5p.

Using a maximum-likelihood mixture-modelling approach (Sambridge and Compston, 1994), Martin et al. (2007) determined a maximum depositional age of 1681 +/- 20 Ma from the same data.
Kiangi Creek Formation
Sample GSWA 148973 was taken from very thick bedded, silicified, fine- to medium-grained quartz sandstone at Strama Gap. The sampled horizon immediately underlies the Discovery Formation on the east bank of Irregully Creek, 0.7 km northeast of Strama Bore. This sandstone was previously considered to mark the base of the Discovery Formation in this area (Martin and Thorne, 2002), but is now considered to represent the uppermost Kiangi Creek Formation in this area. The sample has no obvious internal stratification or heavy mineral lags, but contains abundant mudstone pebble clasts locally. In thin section, the sample consists of >99% quartz, commonly with rounded detrital cores with optically continuous overgrowths.
Bangemall Region
Wingate, MTD, Bodorkos, S and Sircombe, KN 2007, 148973: silicified quartz sandstone, Strama Bore; Geochronology Record 690: Geological Survey of Western Australia, 6p.

Eighty-one analyses were made of zircon cores, which have a wide range of U contents (17-783 ppm) and Th/U (0.02-2.14). Six analyses are >10% discordant, with the remaining 75 analyses having 207Pb*/206Pb* dates ranging between c. 3579 Ma and 2830 Ma. The resulting spectrum of dates has no dominant grouping, but has maxima at c. 3550, 3265, 3230 and 3000 Ma. The two youngest analysed cores have dates of 2838 +/- 4 Ma and 2830 +/- 3 Ma (both 1sigma), which define a statistically coherent weighted mean date of 2833 +/- 5 Ma (MSWD = 3.1, probability = 0.08). Three analyses were made of the dark-CL zones mantling zircon cores, which have high U contents (627-783 ppm) and low Th/U (0.04-0.07). Two of these analyses (58.1 and 62.1) are discordant and excluded from further consideration, but the third (60.2) has a concordant 207Pb*/206Pb* date of c. 1820 Ma. Eight analyses of the moderate-CL intensity rims were attempted, with one site analysed twice (7.1 and 7.1A). One analysis (61.1) slightly overlapped a bright-CL rim and is discounted from further consideration. The moderate-intensity rims have U contents of 77-556 ppm, Th/U of 0.13-0.30 and 207Pb*/206Pb* dates of c. 1794 Ma to 1705 Ma. The two youngest dates (7.1A and 65.1) are slightly younger than the main group of five analyses, which comprise a statistically coherent group with a weighted mean date of 1790 +/- 7 Ma (MSWD = 0.55, probability of equivalence = 0.70). This date is interpreted as to reflect the timing of high-grade metamorphism, with the two younger dates interpreted to be affected by minor Pb loss. Only one late-stage, bright-CL rim was sufficiently thick to analyse. Two analyses were carried out in the same site (57.1 and 57.1A), with measured U contents of 128 and 84 ppm, and Th/U of 0.16 and 0.20. The two analyses yield 207Pb*/206Pb* dates of 1579 +/- 24 and 1580 +/- 24 Ma (both 1sigma), and have a weighted mean date of 1580 +/- 34 Ma (MSWD = 0.001, probability of equivalence = 0.97). The weighted mean date of 2833 +/- 5 Ma (95% confidence) obtained from the youngest two cores is taken as a maximum depositional age for the protolith of the quartzite, and the weighted mean date of 1790 +/- 7 Ma (95% confidence) obtained from the oldest five moderate-CL rims is interpreted as to reflect the timing of high-grade metamorphism. The two analyses of a single rim which yielded a weighted mean date of 1580 +/- 34 Ma (2sigma) is interpreted as the effect of contact metamorphism, as the date is indistinguishable from that of a nearby 1589.4 +/- 5.3 Ma granite (GA 2005670178). The geological significance of the c. 1820 Ma dark-CL zones is difficult to assess. One possibility is that this generation of zircon formation reflects metamorphism at c. 1820 Ma. Another possibility is that it is related to c. 1790 Ma metamorphism, and represents incomplete isotopic resetting or radiogenic Pb loss affecting the outer parts of zircon cores rimmed by moderate-CL overgrowths.
unnamed quartzite - Tabletop
A quartzite unit was sampled adjacent to the western margin of a large leucogranite intrusion in Tabletop Zone (MGA 513542E 7465160N). The quartzite unit strikes N, has a weak compositional layering defined by partings on bedding planes, and contains a moderately E-dipping layer-parallel foliation which is overprinted by a steeply N-dipping spaced cleavage. Further to the south, the unit contains steeply SSW-plunging mesoscopic folds, which are overprinted by a spaced cleavage dipping moderately S. Banded iron formation has been mapped immediately W of the quartzite (Bagas, 1999), but only secondary iron oxides in quartzite were observed in this study.bIn thin section the quartzite comprises >95% quartz, which forms a fine- to medium-grained recrystallized mosaic with sutured ('bulged') grain boundaries. Discontinuous folia of muscovite define the layer-parallel foliation. Rare isolated grains up to 1 mm in size consist of a recrystallized aggregate of very fine-grained muscovite and chlorite. Trace zircon, biotite and fine-grained opaque minerals are also present. A foliation defined by partial flattening of quartz grains overprints the layer-parallel foliation at a high angle and is interpreted as the east-west trending spaced cleavage seen in outcrop.
Maidment, D.W., 2017. Geochronology of the Rudall Province, Western Australia: Implications for the amalgamation of the West and North Australian Cratons. Geological Survey of Western Australia. Report, 161, 95p.

Coodardoo Formation
Sample GSWA 148975 is of medium-grained feldspathic quartz sandstone in the upper part of the Coodardoo Formation, on the northern limb of the Wanna Syncline, about 3.7 km south-southeast of Strama Bore. At this locality, the Coodardoo Formation consists of thick-bedded massive sandstone, with few laminated siltstone interbeds. In thin section, the sample consists mainly of monocrystalline quartz (~85%) with rare optically continuous overgrowths. Lithic grains are common (5-7%) and vary from cherty to microgranular and from quartz-rich to sericite-rich. Interstitial limonite-stained clays are common (5-7%) with rare anatase/rutile and rounded zircon. Paleocurrent indicators are rare in the Coodardoo Formation, but the vector mean azimuth is towards the southeast.
Wingate, MTD, Bodorkos, S and Sircombe, KN 2007, 148975: lithic quartz sandstone, Strama Bore; Geochronology Record 692: Geological Survey of Western Australia, 5p.

Timberoo Member
Grey, fine-grained sandstone, hummocky ?, interbedded with very thinly bedded siltstones

A dominant cluster between 1800 & 1675Ma was unmixed to produce a youngest age of 1681+/-10Ma which is within error of the weighted mean of the youngest 17 ages (1692+/-8ma)
Llewellyn Creek Formation
Grey, crystalline, fine-grained micaceous sandstone interbedded and graded with andalusite schists

Inserted from Geochron Delivery (Geoscience Australia; http://www.ga.gov.au/geochron-sapub-web/)
Yaya Metamorphic Complex
Papunya Quartzite
Massive crystalline quartzite outcrops at a number of localities north of Mount Larrie in HAAST BLUFF, most notably as a prominent ridge 6 km west-southwest of Papunya, which extends for 5 km along strike. These outcrops have been assigned to the Inyalinga Granulite of the Yaya Metamorphic Complex (Scrimgeour et al in press). The quartzite appears to be metasedimentary in origin, is clean, coarsely crystalline and is interpreted to have undergone structural repetition. Recessive zones occur in the quartzite ridge, with rare outcrops of calc-silicate rock. At its western end, the quartzite is intruded by the Larrie Granodiorite (1640-1630 Ma Waluwiya Suite). Large rafts of quartzite within Larrie Granodiorite at 788086mE, 7425567mN are interpreted to belong to the Inyalinga Granulite.
Massive crystalline quartzite outcrops at a number of localities north of Mount Larrie in HAAST BLUFF, most notably as a prominent ridge 6 km west-southwest of Papunya, which extends for 5 km along strike.
Cross, A., Claoue-Long, J.C., Scrimgeour, I.R., Close, D.F., Edgoose, C.J., 2005. Summary of results. Joint NTGS-GA geochronology project southern Arunta Region. Northern Territory Geological Survey Record, 2004-003, CD, 61p.

Highlands Rocks Metamorphics
-[informal_name: Highlands Rocks Metamorphics]-
NORTHERN ARUNTA (TANAMI DESERT)
Cross, A., Claoue-Long, J.C., Scrimgeour, I.R., Crispe, A., Donnellan, N., 2005. Summary of results. Joint NTGS-GA geochronology project: northern Arunta and Tanami regions, 2000-2003. Northern Territory Geological Survey Record, 2005-003, 69p.

Max depositional age. Age range 354-297 Ma. Carson et al. (Queensland Geological Record 2006/01) quoted a weighted mean 206Pb/238U age of 318.7 +/- 3.0 Ma (95% confidence) for these 74 analyses, but that date was incorrectly calculated. The analyses within the population are dispersed well beyond that expected from their analytical uncertainties, and the most representative date for this cluster is the median shown here.
Good Night beds
rare garnet, biotite quartzo-feldspathic gneiss, highly strained. Sampled for detrital U-Pb zircon geochron, meta
Proserpine Region
Carson, C.J., von Gnielinski, F.E., Bultitude, R.J., 2007. Results of the joint GSQ-GA geochronology project, New England Orogen, ROSEDALE, MOUNT PERRY and GLADSTONE 1:100 000 Sheet Areas, March 2006-December 2006. Queensland Geological Record, 2006/01, 58p.

Good Night beds
rare garnet, biotite quartzo-feldspathic gneiss, highly strained. Sampled for detrital U-Pb zircon geochron, meta
Carson, C.J., von Gnielinski, F.E., Bultitude, R.J., 2007. Results of the joint GSQ-GA geochronology project, New England Orogen, ROSEDALE, MOUNT PERRY and GLADSTONE 1:100 000 Sheet Areas, March 2006-December 2006. Queensland Geological Record, 2006/01, 58p.

Youngest individual age 1744+/-32Ma is part of 1830-1745Ma cluster. Youngest modelled age consistent with weighted mean of 1776+/-3Ma (95% conf) for youngest 65 of 67 analyses in cluster (MSWD=1.17); weighted mean age is interpreted to be Max dep age
Corella Formation
Massive, thick-bedded, clean 10-15 m thick quartzite within carbonate succession.
Neumann, N.L., Gibson, G.M., Southgate, P.N., 2009. New SHRIMP age constraints on the timing and duration of magmatism and sedimentation in the Mary Kathleen Fold Belt, Mt Isa Inlier, Australia. Australian Journal of Earth Sciences, 56(7), 965-983.

85% of ages are 1885-1740 Ma. Youngest individual age is 1742+/-58 Ma. Youngest modelled age is consistent with the weighted mean age of 1770+/-6 Ma (95% conf.) for the youngest 34 analyses (MSWD = 1.4), and is interpreted to be the maxdep age
Collected from a 40 cm-thick bed of grey-coloured, thinly bedded fine-grained sandstone in the lowermost part of the Corella Formation, about 30 m above the top of the Ballara Quartzite.
Neumann, N.L., Gibson, G.M., Southgate, P.N., 2009. New SHRIMP age constraints on the timing and duration of magmatism and sedimentation in the Mary Kathleen Fold Belt, Mt Isa Inlier, Australia. Australian Journal of Earth Sciences, 56(7), 965-983.

Martin et al. (2007) determined a maximum depositional age of 1787 +/- 4 Ma from the same data.
Blue Billy Formation
Sample GSWA 148971 was taken approximately 2 km north-northwest of Carnoby Well, within a unit of interbedded very thick bedded, medium-grained, lithic quartz sandstone and silicified siltstone at the top of the Blue Billy Formation. In hand specimen, feldspars have been altered to clay minerals, but the heavy mineral population and lithic fragments are well preserved. There are no paleocurrent indicators preserved at this site, and no paleocurrent data are available for the Blue Billy Formation, which consists mainly of planar laminated, carbonaceous siltstone.
Wingate, MTD, Bodorkos, S and Sircombe, KN 2007, 148971: lithic quartz sandstone, Bluff Bore; Geochronology Record 688: Geological Survey of Western Australia, 5p.

Martin et al. (2007) determined a maximum depositional age of 1679 +/- 3 from the same data
Mount Augustus Sandstone
Sample GSWA148972 was collected from the crest of a small isolated hill approximately 1.4 km south of Ulna Well, to the west of Mount Augustus. The sample is of coarse to very coarse grained feldspathic sandstone with well preserved trough cross stratification. The relative stratigraphic position of the sample within the Mount Augustus Sandstone is unknown because no relationships with underlying or overlying units are exposed. In thin section, the sample consists of well-rounded quartz (~60%) and alkali feldspar (35%), as well as rare rounded grains of zircon or monazite and sparse biotite and riebeckite (both < 1%). The quartz is mainly monocrystalline, with sparse grains of polycrystalline quartz. The paleocurrent vector mean at this site is towards the south, although the predominant paleocurrent direction for the Mount Augustus Sandstone is towards the southeast (Fig. 3).
Geological Survey of Western Australia geochronology dataset 689

Twenty-eight analyses were carried out, with 27 of these comprising a concordant to near-concordant grouping with moderate to high U contents (441-1777 ppm), Th/U of 0.09-0.32 and 207Pb*/206Pb* dates ranging between c. 1792 Ma and 1773 Ma. This grouping has a statistically coherent weighted mean date of 1780.4 +/- 1.5 Ma (MSWD = 1.05, probability of equivalence = 0.39). A single analysis of a near-concordant grain with the highest U content of 4153 ppm (5.1) has a significantly younger date of c. 1759 Ma and is interpreted to have undergone ancient loss of radiogenic Pb.The muscovite-rich character and compositional layering of the schist are consistent with a metasedimentary origin for this unit, but the uniform character and age of the zircons raises the question as to whether the sampled layer might instead represent a highly deformed igneous rock. It is difficult to confidently discriminate between these two alternatives, but the muscovite-rich character is perhaps more consistent with a metasedimentary protolith given the typically biotite-rich, muscovite-poor and often porphyritic character of most granitic orthogneisses in the Rudall Province, though a few muscovite-bearing units have been interpreted as orthogneisses (Hickman and Bagas, 1998). The irregular surfaces of many zircon grains and the possible rounding of crystal terminations might also be evidence of limited sedimentary transport and abrasion. The 1780.4 +/- 1.5 Ma date for this rock is thus tentatively interpreted as a maximum depositional age for a metasedimentary protolith to the schist, though a magmatic age remains a possible interpretation.
Talbot schist
Quartz-K-feldspar-muscovite schist was sampled from the northwestern part of the Talbot Zone (MGA 401083E 7507460N), where unassigned metasedimentary schist occurs adjacent to layered granite orthogneiss. Hickman and Bagas (1999) suggested that these metasedimentary rocks might pre-date layered orthogneiss and thus comprise some of the oldest rocks in the Talbot Zone. The sampled schist contains a high-grade layer-parallel foliation containing medium- to coarse-grained muscovite, which is folded about mesoscale tight, upright, northwesterly trending F4 folds. The schist forms part of a compositionally layered succession defined by differing abundances of quartz, muscovite and feldspar. In thin section, the schist consists of thin interlayered domains of granoblastic medium-grained quartz, microcline and lesser plagioclase, bound by laminae of layer-parallel muscovite, which comprises up to 15% of the rock.
Maidment, D.W., 2017. Geochronology of the Rudall Province, Western Australia: Implications for the amalgamation of the West and North Australian Cratons. Geological Survey of Western Australia. Report, 161, 95p.

Magmatic age for tuffaceous cobble within the diamictite of the Jeffreys Flat Formation. However, this only provides a maximum age for deposition of the host diamictite.
An abundance of zircon was separated from a flattened tuffaceous cobble within this diamictite, with the aim of determining the age of the source rock from which the cobble was derived. Most of the zircon is relatively equant, with aspect ratios only rarely exceeding 2:1. Both euhedral and rounded grains are present. The former, which are considerably more common, were targeted for analysis because they are considerably more likely to yield the depositional age of the tuff. Those grains are generally complexly faceted, with complementary oscillatory prismatic zonation. Although present, neither silicate cores,nor cracks, nor metamict zones are sufficiently prevalent to preclude the analysis of most grains. The array of individual ages is simple to interpret. An 1100 Ma grain fragment is considerably older than any of the other dated grains. The remaining ages are too scattered to define a single population, but this can be achieved by deleting just two of them, the first and the last of the sub-session (almost certainly just a coincidence), on the basis that they have lost a little radiogenic Pb. The remaining 16 individual ages yield a weighted mean age of 509.8 +/- 3.4 Ma (MSWD = 1.64, probability of equivalence = 0.06), which should represent the age of the tuff from which this pebble in the diamictite was derived. Unlike sub-session 1, sub-session 2 data show no evidence of post-crystallisation Pb loss. The only temporal outlier recorded in sub-session 2 is a Grenvillian age, which is about 100 million years younger than the only other previously identified example of inheritance in this rock. All 12 of the remaining ages, which are within error of each other (MSWD = 0.49, probability of equivalence = 0.91), produce a weighted mean age of 513.3 +/- 7.7 Ma. This value is statistically indistinguishable (MSWD = 0.69, probability of equivalence = 0.41) from the age derived from sub-session 1. It is therefore justifiable to combine those two estimates to obtain a preferred value of 510.4 +/- 3.0 Ma for the age of the tuff that is represented by the pebble in the diamictite.
Jeffreys Flat Formation
Felsic volcanic clast/pebble within diamictite of the Jeffreys Flat Formation (Warratta Inlier, National Parks and Wildlife Service paddock). F2 fold axis plunges 58 towards 086.
Tibooburra Region
Warratta Inlier, National Parks and Wildlife Service paddock.
Geological Survey of New South Wales (GSNSW)
Black, L.P., 2006. SHRIMP U-Pb zircon ages obtained during 2005/06 for NSW Geological Survey projects. Geological Survey of New South Wales Report GS, 2006/821, 37p.

Eighteen analyses of the zircon grains have U contents of 125-380 ppm, Th/U of 0.94-1.42 and near-concordant 207Pb*/206Pb* dates of c. 1771-1741 Ma, comprising a single statistically coherent group with a weighted mean date of 1760.1 +/- 5.1 Ma (MSWD = 0.83, probability of equivalence = 0.66). The weighted mean date of 1760.1 +/- 5.1 Ma (95% confidence) is tentatively interpreted to represent the age of a local granitic source that dominated the provenance of the sedimentary protolith of this rock and is thus interpreted as a maximum depositional age for the Larry Formation. The interpretation that the zircons in this sample have a detrital origin is consistent with the compositional layering in the sampled unit, the muscovite-rich compositions, and the lack of phenocrysts, though these features are not sufficient to demonstrate a sedimentary origin. The irregular surfaces on many zircon grains could conceivably be a result of abrasion during sedimentary transport, but modification by in-situ processes during metamorphism could conceivably also produce similar features. Given these uncertainties, it is also possible to interpret the 1760.1 +/- 5.1 Ma date as the timing of magmatic crystallization of a deformed igneous protolith, in which case this date would provide a minimum rather than maximum age for the Larry Formation.
Larry Formation
The Larry Formation was sampled from Larry Creek in the southeastern Fingoon Range (MGA 431181E 7493130N). In this area, the Larry Formation consists of quartz-feldspar-mica schist and gneiss with a centimetre- to decimetre-scale layering, and has been interpreted as a feldspar-rich metasedimentary package (Hickman and Bagas, 1998). The unit contains a pervasive layer-parallel high-grade foliation, interpreted as S2, which has been deformed by tight, NW-plunging, moderately NE-inclined to recumbent folds interpreted as F4. The unit is intruded by small quartz-K-feldspar pegmatite bodies that are sub-parallel to layering, but do not contain the layer-parallel foliation, and are tightly folded by the northwesterly trending folds. The Larry Formation rocks are generally highly weathered, with lateritic caps on hill tops indicating these rocks were proximal to an ancient weathering surface. This has resulted in the pervasive weathering of feldspars and micas to sericite and clays, though primary textures are typically preserved. In thin section, the sampled layer consists of granoblastic quartz aggregates in a clay-rich, quartz-poor groundmass. Relict muscovite within some clay pseudomorphs suggests that muscovite may have been the dominant mica in this sample. Subordinate equigranular and structureless clay-rich grains may have been derived from weathering of feldspar. Numerous thin laminae of granoblastic quartz aggregates generally <1 mm thick within the clay-rich groundmass contain fine- to medium-grained muscovite which has been armoured from weathering. The pre-weathering lithology is considered to have been a quartz-muscovite-feldspar +/- biotite schist.
Maidment, D.W., 2017. Geochronology of the Rudall Province, Western Australia: Implications for the amalgamation of the West and North Australian Cratons. Geological Survey of Western Australia. Report, 161, 95p.

Tommie Wattie Formation
upper pelitic unit, Tommie Wattie Formation
Cream coloured laminated metasedimentary rock, very quartz-rich, recrystallised, some iron staining and weathering present. This sample displays a uniformly fine-grained sutured granoblastic metamorphic texture. Albite and quartz dominate the rock: albite forms small anhedral twinned grains and quartz forms anhedral grains with slight strain shadowing. A weak foliation is defined by preferred orientation of some of the felsic grains. Biotite occurs in minor amount as small pleochroic pale tan brown flakes which also tend to be aligned in the foliation. Muscovite forms rare flakes, slightly larger than biotite. Tourmaline forms pleochroic drab green grains sparsely scattered through the rock. Rutile occurs in trace amount as small dark reddish grains. Zircon occurs as small grains. This sample may have formed as a felsic rock, possibly of psammitic sedimentary origin. It has undergone pervasive recrystallisation and alteration in response to a regional metamorphic event, generating the weakly foliated new assemblage of albite + quartz + minor biotite + tourmaline + muscovite + rutile. Small zircon grains are considered to represent a relict primary phase.

Inserted from Geochron Delivery (Geoscience Australia; http://www.ga.gov.au/geochron-sapub-web/)
Coolbro Sandstone
The Coolbro Sandstone is the basal unit of the Throssell Range Group and unconformably overlies the Rudall Province. The unit comprises a basal polymict conglomerate overlain by massive and thickly bedded sandstone with minor siltstone and shale. This sample is a grey, medium-grained, poorly sorted, thickly bedded, trough cross-stratified crystalline sandstone, collected about 50 m above the contact with Rudall Province basement, in the Kintyre region.
Near Kintyre deposit, about 50 m above contact with Rudall Province
Maidment, D.W., Huston, D.L., Maas, R., Czarnota, K., Neumann, N., Mcintyre, A., Bagas, L., 2008. The Nifty-Kintyre-Duke Cu-U-Pb-Zn mineralizing events: links to the evolution of the Yeneena Basin, northwest Paterson Orogen. Geological Survey of Western Australia. Record, 2008/2, 27-29.

Coolbro Sandstone
The Coolbro Sandstone is the basal unit of the Throssell Range Group and unconformably overlies the Rudall Province. This sample is a white, medium- to coarse-grained, pebbly and cross-bedded sandstone, collected near the stratigraphic top of the Coolbro Sandstone, in the Cottesloe Syncline about 20 km NNE of Kintyre.
West of road, mapped as Broadhurst Formation
Maidment, D.W., Huston, D.L., Maas, R., Czarnota, K., Neumann, N., Mcintyre, A., Bagas, L., 2008. The Nifty-Kintyre-Duke Cu-U-Pb-Zn mineralizing events: links to the evolution of the Yeneena Basin, northwest Paterson Orogen. Geological Survey of Western Australia. Record, 2008/2, 27-29.

Youngest modelled age of the dominant 1805-1650Ma cluster.
Mount Norna Quartzite
Fine-grained crystalline quartzite from approx 1m thick sand base with finer upper

Key Creek Gneiss
This sample of biotite paragneiss was collected from an outcrop in a creek bed ~50 m N of Normanby Road, on Sutherland station ~40 km SSE of Collinsville. The Key Creek Gneiss forms an extensive (~265 km2) metamorphic complex located in the centre of the Urannah Batholith. The rocks within the complex are mainly upper amphibolite-grade paragneisses, which have a distinctive elevated thorium response on radiometric images. The analysed sample comprises mainly quartz, feldspar, andalusite (commonly extensively altered), biotite and muscovite, with minor garnet, traces of apatite, zircon, and monazite, and scattered quartz inclusions. Previous geochronology on this sample includes SHRIMP U-Pb zircon analysis and Isotope Dilution Thermal Ionisation Mass Spectrometry (ID-TIMS) U-Pb monazite analyses (sample 1953976/RJB2913; Cross et al. 2012a). SHRIMP U-Pb zircon geochronology of two Key Creek Gneiss samples reported by Cross et al. (2012a) gave metamorphic ages of 297.0 +/- 2.7 Ma and 298.2 +/- 6.9 Ma (samples: 1980488/BB4952, 1953976/RJB2913 respectively).These SHRIMP U-Pb zircon ages, derived from analyses of low Th/U metamorphic rims, are in contrast to the ID-TIMS U-Pb monazite age determination for one of these samples (1953976/RJB2913) which gave an age of 291.0 +/- 0.9 Ma (Cross et al. 2012a). These ages led Cross et al. (2012a) to suggest that metamorphism within the metamorphic complex, was a protracted event between ~300 Ma and ~290 Ma. The IDTIMS U-Pb monazite age determination of 291.0 +/- 0.9 Ma reported for sample 1953976/RJB2913 (Cross et al., 2012a) is, however, somewhat equivocal as three of the six fractions analysed were interpreted to have possibly undergone Pb-loss, and were consequently not used in the age calculation. Therefore, an additional isotopic study of these monazites was undertaken by SHRIMP U-Pb to further examine the metamorphic crystallisation age of these grains.
Cross, A.J., Bultitude, R.J., Purdy, D.J., 2013. Summary of Results - Joint GSQ-GA Geochronology Project: Ayr, Bowen, Eulo, Mount Coolon, Proserpine and Warwick 1:250 000 sheet areas. Queensland Geological Record, 2012/19, 146p.

Youngest modelled age of 1750-1660Ma cluster; also in error of weighted mean of youngest 42 analyses
Grey crystalline medium-grained quartzite from 20cm thick sand base of turbidite package

Mitakoodi Quartzite
Grey-green v. fine-grained sandstone, thinly bedded, hummocky?, strongly cleaved

Grey-pink, crystalline massive well sorted quartzite, low angle cross beds

Youngest detrital zircon component. Age range 1774-1721 Ma.
Answer Slate
Medium bedded, medium grained calcareous sandstone, porous

Youngest individual age 1709+/-34Ma forms part of main 1795-1710Ma cluster. Youngest modelled age consistent with weighted mean age of 1748+/-3Ma for youngest 63 analyses in this cluster (MSWD=1.2), & this weighted mean age is interpreted to be Maxdep age
Deighton Quartzite
Clean, crystalline pink, cross-bedded quartzite from near the base of the unit. Interbedded with vesicular to massive basalt.

Zircon Description The sample is from outcrop of muscovite-bearing foliated meta-quartzite with a fabric dipping steeply southwest. It is metamorphosed to upper-greenschist / lower amphibolite facies and is interpreted as cover to the local granulite facies Palaeoproterozoic basement. The unit underlies flat-lying and unmetamorphosed Heavitree Quartzite. Zircons were analysed for a detrital age spectrum to assist in identifying the sediment, its associations, and maximum deposition age. Zircons in the sample have highly variable shapes, colours and internal zoning, consistent with a detrital zircon suite (Fig. 1). Internal zoning patterns are truncated, indicating breakage and abrasion of grains. There are no metamorphic zircon overgrowths. A random line of analyses was collected from grains that had been sorted as non-magnetic using the Frantz separator. U-Pb Isotopic Results A total of 66 individual analyses was collected. Of these, 4 are more than 10% discordant and are not considered further. The remaining 62 analyses provide a useful detrital zircon age spectrum (Fig. 2). All but two of the detrital ages are a continuum in the range between ca. 1230 Ma and 1850 Ma, with two outlying ages at ca 2450 Ma (Fig.3). Prominent populations are present at ca. 1700-1750 Ma and ca 1550-1600 Ma, with a subordinate grouping at ca. 1250-1350 Ma. At the youngest end of the age spectrum three individual detrital ages have a mean of 1235 ± 21 Ma (2¿, MSWD 2.6 vs a threshold value of 3.1 for 3 observations; alternatively ± 74 Ma at 95% confidence). This provides an estimate of the youngest detrital age and the maximum deposition age of the sediment. As a point of comparison, Figure 4 shows the detrital age spectrum in the Heavitree Quartzite sampled at Ruby Gap (D. Maidment, thesis). The two are similar but not the same. The spectra share prominent groupings at ca. 1700-1750 Ma and ca 1550-1600 Ma. Howeve,r the Heavitree sample, as with all sedimentary units in the Amadeus and Georgina basins, and metamorphosed equivalents in the Harts Range Group, includes Musgravian-age detritus (ca. 1150 Ma ) which has not been found in this sample. Clearly the detrital age spectrum and maximum deposition age require this meta-quartzite to be cover to the Palaeoproterozoic basement. However, the relationship to Amadeus Basin stratigraphy (Heavitree Quartzite) is not clear. On the basis of the apparent absence of Musgravian detritus, the mapped position underlying the Heavitree, and the fact that the unit is deformed and metamorphosed below flat-lying Heavitree Quartzite, the unit could be interpreted in terms of an earlier basin episode, post-ca. 1230 Ma and pre-Musgravian. Alternatively, the the apparent absence of Musgravian detritus could be interpreted as an analytical sampling artefact: in which case the unit might be regarded as a deformed and metamorphosed representative of Heavitree Quartazite now structurally juxtaposed with its unmetamorphosed equivalent. These alternatives require testing with further work.
unnamed quartzite
The sample is from an outcrop of muscovite-bearing polydeformed metaquartzite, with a dominant fabric dipping steeply southwest. The unit is metamorphosed to upper greenschist-lower amphibolite facies and is interpreted to unconformably overlie the granulite facies Palaeoproterozoic basement of the Casey Inlier. The unit is dominated by a matrix of polygonal equigranular quartz (90% modal abundance) and muscovite (5-8%). Slightly flattened quartz and stringers of aligned interstitial muscovite define the dominant foliation. Scattered unidentified opaque oxide minerals are also present (1-2%). No monazite was observed in thin section. The unit underlies flat-lying, undeformed and unmetamorphosed Heavitree Quartzite. Zircons were analysed for a detrital age spectrum to assist in identifying the rock, its associations and its maximum deposition age.

Greenish-brown mudstone in a dolomitic interval of the Quilalar Formation at 78 m in section HT 1 (Jackson et al. 2002). The sampled interval produced a distinctive spike on the gamma-ray log. Previous experience suggests that K-rich tuffaceous units often correlate with gamma-ray log spikes.
section HT 00/01 @ 52.5 i
Jackson, M.J., Southgate, P.N., Black, L.P., Blake, P.R., Domagala, J., 2005. Overcoming Proterozoic quartzite sand-body miscorrelations: integrated sequence stratigraphy and SHRIMP U-Pb dating of the Surprise Creek Formation, Torpedo Creek and Warrina Park Quartzites, Mt Isa Inlier. Australian Journal of Earth Sciences, 52(1), 1-25.

Youngest individual age 1700+/-40Ma forms part of the 1825-1700Ma cluster. Youngest modelled age consistent with weighted mean age of 1751+/-4Ma (95%conf) for the youngest 50 analyses (MSWD = 1.3).
Deighton Quartzite
Pink, cross-bedded feldspathic sandstone, with pebbles and dolomitic mud interbeds.

Deighton Quartzite
Pink-grey crystalline medium-grained quartzite

Argylla Formation
A siltstone sample (2005169045) was collected from the upper parts of a stratigraphic section comprising basal Argylla Formation, above which occurs an interval of large-clast, monomict, conglomerate (~100-150 m-thick) and a 15-20 m-thick interval of small-clast, matrix-supported, polymict conglomerate with interbedded poorly sorted sandstone and siltstone. A sharp and erosive upper contact separates sandstone of the small-clast conglomerate from white, cross-bedded quartzite of the Ballara Quartzite. The monomict conglomerate contains clasts of felsic volcanics from the underlying Argylla Formation. Sample 2005169045 was collected from a thin siltstone interbed in the small-clast, upper conglomerate unit. The siltstone occurs in a thin, poorly sorted sandstone unit which contains intraclasts of the underlying siltstone. The sample was collected to test whether the small clast conglomerate unit is temporally related to the underlying Argylla Formation, or forms the basal unit of the overlying Ballara Quartzite.
Neumann, N.L., Gibson, G.M., Southgate, P.N., 2009. New SHRIMP age constraints on the timing and duration of magmatism and sedimentation in the Mary Kathleen Fold Belt, Mt Isa Inlier, Australia. Australian Journal of Earth Sciences, 56(7), 965-983.

Chilling Sandstone
coarse grained sandstone

Martin et al. (2007) determined a maximum depositional age of 1680 +/- 8 Ma from the same data.
Curran Member
Sample GSWA 148974 was taken from a unit of interbedded fine-grained lithic sandstone and siltstone within the Curran Member of the Ullawarra Formation, below the type section of the Coodardoo Formation at Coodardo Gap. The sample site is approximately 1.2 km northeast of Coodardo Well. This fine-grained lithic sandstone has no internal stratification or grading. In thin section, the sample is rich in poorly sorted silt to medium sand-sized detrital grains (35-40%) and has a clay-rich matrix. The grains are composed of about 1% each of quartz, plagioclase, and microcline, as well as sparse quartz-rich to sericite-rich lithic grains that make up 25-75% of some layers. Accessory and trace minerals include muscovite, biotite, chlorite, leucoxene, rutile, anatase, and tourmaline. The paleocurrent vector mean for the Curran Member is towards the northwest.
Wingate, MTD, Bodorkos, S and Sircombe, KN 2007, 148974: lithic sandstone, Coodardo Well; Geochronology Record 691: Geological Survey of Western Australia, 6p.

Backdoor Formation
Sample GSWA 148977 was taken from very thick bedded, medium-grained, trough cross-stratified quartz sandstone in the upper Backdoor Formation, approximately 150 m below the contact with the Calyie Formation. The sample site is 8.4 km southeast of Bend Bore. The sample consists of moderately fresh sandstone, with feldspars partially replaced by clay minerals and locally abundant mudstone intraclasts. There is abundant quartz with well-defined rounded cores (80%) and optically continuous overgrowths in thin section, as well as rare clay-rich and quartz-rich microcrystalline clasts (2-3%). Accessory and trace minerals include greenish tourmaline, partly with pale bluish authigenic overgrowths, leucoxene, and zircon. Paleocurrent directions are hard to determine at this site, but appear to trend north to south or northwest to southeast.
Wingate, MTD, Bodorkos, S and Sircombe, KN 2007, 148977: quartz sandstone, Bend Bore; Geochronology Record 694: Geological Survey of Western Australia, 6p.

Youngest detrital zircon component. Age range 1818-1766 Ma (five analyses of two grains).
Double Crossing Metamorphics
Sampled biotite-muscovite psammite bed with minimal melt selvages. Outcrop comprises migmatitic amphibolites + biotite sillimanite schists + muscovite-biotite psammites + leucosome selvages and is strongly weathered.

Post-1810 Ma detrital zircons, incorporating the youngest detrital age component. Two-component mixture modelling of 64 analyses spanning the age range 1804-1715 Ma: younger component (1743 +/- 4 Ma) comprises ~86% of the population.
Staveley Formation
Very fine-grained sandstone from a 5-30cm thick massive bed. Outcrop comprises very fine sandstone with 1cm thick very fine-grained sandstones, with ball and pillow and convolute bedding with current-reworked ripple tops. Some calcareous component in fine

Youngest detrital zircon component. Age range 1763-1688 Ma.
Staveley Formation
Fine-grained, cross-bedded planar bedded, well-sorted poorly cemented sandstone. Beds upto 50cm thick with finer interbeds. Younging to east, stratigraphically underlies 2006169012.

Post-1770 Ma detrital zircons, incorporating the youngest detrital age component. Two-component mixture modelling of 65 analyses spanning the age range 1757-1642 Ma: younger component (1674 +/- 8 Ma) comprises ~44% of the population.
Kuridala Group
Fine-coarse-grained, poorly sorted sandstone from ~2m thick bed. Outcrop comprises ~30m thick package of fine- to coarse-grained, poorly sorted sandstones within a black siltstone-shale package (mapped as Pkrs - Kuridala slate)

Two fractions were collected from this sedimentary sample during the magnetic separator process - an initial unsorted random separate collected at the first appearance of zircon (termed magnetic fraction), and a separate that has been refined further by the separation process (termed non-magnetic fraction). Handpicking of both fractions was only undertaken to ensure purity of the zircon content. As the sample is from a sedimentary rock, more than 60 grains were analysed to generate a detrital age spectrum, and only grains with surface imperfections were avoided. All analyses were undertaken on grains of the non-magnetic fraction, which may increase the chance of bias towards selected components of the provenance distributions. Analyses with common Pb contents greater than an arbitrary threshold of 0.50% have large uncertainties and therefore have been removed from further consideration, as have analyses that are more than 10% discordant. The 207Pb/206Pb ages for grains younger than ~1300 Ma become very imprecise. Due to the wide range of ages present within this sample (Archaean to <1000 Ma) 204Pb-corrected 207Pb/206Pb ages are used to describe the provenance spectra, whereas 204Pb-corrected 206Pb/238U ages are used to describe the youngest individuals.
Malu Formation
The Malu Formation is the basal unit of the Lamil Group and outcrops north of the Parallel Range Fault. The unit comprises massive to bedded, fine- to medium-grained quartz sandstone with minor interbedded shale and dolomite. This sample was collected from near the stratigraphic top of the unit (at about the same level as 2004679008) in the Karakutikati Range, about 15 km S of the Telfer deposit on western side of Rudall Park road. It comprises buff, massive, very fine grained, quartzofeldspathic sandstone bedded at 20-50 cm scale.
About 15 km S of Telfer, west side of Rudall Park road
Maidment, D.W., Huston, D.L., Maas, R., Czarnota, K., Neumann, N., Mcintyre, A., Bagas, L., 2008. The Nifty-Kintyre-Duke Cu-U-Pb-Zn mineralizing events: links to the evolution of the Yeneena Basin, northwest Paterson Orogen. Geological Survey of Western Australia. Record, 2008/2, 27-29.

Albarta Metamorphics
high-grade metapsammite from eastern Albarta Metamorphics

Wilki Formation
The Wilki Formation conformably overlies the Puntapunta Formation and represents the uppermost unit of the Lamil Group. The unit comprises massive to bedded, fine- to medium-grained sandstone with minor shale and laminated sandstone. This sample was collected about 30 km NW of Telfer, 100 m south of Marble Bar-Telfer road, and about 50 m away from the main intrusive contact with Mount Crofton Granite. It is a grey, massive, medium- to coarse-grained quartzite with 2 m thick beds. The quartzite is locally intruded by medium-grained, sericitised monzogranite veins about 2-3 m thick, but these veins were avoided during sampling.
About 30 km NW of Telfer, and 100 m S of Marble Bar-Telfer road

Puntapunta Formation
The Puntapunta Formation is the middle unit of the Lamil Group and conformably overlies the Malu Formation. It comprises clastic carbonate rocks interbedded with siltstone and shale. This sample was collected about 16 km NW of Telfer, and comprises a grey, very fine-grained, massive to thick-bedded, crystalline sandstone. Elsewhere, the unit contains 30 cm thick beds with ball and pillow loading structures.
About 16 km NW of Telfer

Post-1800 Ma detrital zircons, incorporating the youngest detrital age component. Two-component mixture modelling of 30 analyses spanning the age range 1783-1697 Ma: younger component (1713 +/- 6 Ma) comprises ~55% of the population.
Roxmere Quartzite
Pink, poorly sorted massive feldspathic sandstone ?turbiditic

Argylla Formation
White, clean quartzite with large cross-beds and Fe-oxide spots

Youngest detrital zircon component. Age range 1786-1733 Ma.
Thinly bedded, v. fine-grained sandstone with siltstone interbeds, ?wavy bedded

Post-1800 Ma detrital zircons, including the youngest detrital age component. Two-component mixture modelling of 39 analyses spanning the age range 1777-1667 Ma: younger component (1693 +/- 9 Ma) comprises ~61% of the population.
Kuridala Group
Poorly sorted, very fine- to coarse-grained crystalline sandstone from ~2m thick massive bed, comprises quartz + K-feld+ epidote. Package comprises poorly sorted very fine- to coarse-grained massive beds upto 4m thick with finer shale/siltstone interbeds.

Post-1800 Ma detrital zircons, including the youngest age component. Two-component mixture modelling of 40 analyses spanning the age range 1788-1692 Ma: younger component (1728 +/- 8 Ma) comprises ~72% of the population.
Roxmere Quartzite
Pink, very fine- to coarse-grained, friable, very poorly sorted, cross-bedded sandstones, beds upto 10-50cm thick with some finer interbeds. outcrop youngs to east.

Youngest detrital zircon component. Age range 1685-1649 Ma. Sample from unit identified when collected as Corella Formation, but now mapped as Milo beds (Withnall 2019)
Milo beds
Grey psammite from layered calc-silicate package. Sampled ~ 40m east of 2006169021.

Youngest detrital zircon component. Single analysis only.
Grey, psammitic ~30 cm thick bed with a coarse base and a planar laminated upper, from mixed siliceous-carbonaceous unit. Carbonate beds include stromatolite mats and small domes. Uppermost Mitakoodi Quartzite sampled (mapped as Overhang Jasperlite).

Post-1800 Ma detrital zircons including youngest age component. Two-component mixture modelling of 62 analyses spanning the age range 1773-1677 Ma: younger component (1711 +/- 4 Ma) comprises ~86% of the population.
Toole Creek Volcanics
Psammite bed, at very top of the Mt Norna Quartzite/lower Toole Creek Volcanics

Malu Formation
The Malu Formation is the basal unit of the Lamil Group and outcrops north of the Parallel Range Fault. The unit comprises massive to bedded, fine- to medium-grained quartz sandstone with minor interbedded shale and dolomite. This sample was collected from near the stratigraphic top of the unit (at about the same level as 2004679003), within the Telfer Member, about 17 km NW of Telfer. It is a buff-coloured, very fine- to fine-grained, internally laminated, thick bedded sandstone.
About 17 km NW of Telfer

Pod of massive cordierite-sillimanite rock within partially melting metasediments. Interpreted as possible restite after melt extraction. Igneous zircon age consistent with Yambah Event. Inheritance conistent with Lander package metasediment protolith
A sample of massive, quartz-poor cordierite-rich rock was collected from an isolated hill of granulite-facies metasedimentary rocks, about 25 km east-northeast of Mount Singleton in southwestern MOUNT THEO. The hill comprises a metasedimentary succession mapped as high grade Lander Rock Formation. The most common rock types are metapelites (containing sillimanite-cordierite-K-feldspar +/- garnet and quartz) that locally have garnet-bearing leucosome patches interlayered with cordierite-biotite-garnet-quartz metapsammite. The metapelite and metapsammite are interlayered on a scale of 3 cm to 1 metre. These are intermingled with, and locally form xenoliths in, an S-type granite with coarse-grained K-feldspar phenocrysts up to 2 cm. The granite is garnet- and cordierite-bearing, with numerous metasedimentary xenoliths. The granite is interpreted to have formed in situ from melting of the metasedimentary rocks. Adjacent to the granite are zones of massive cordierite granulite containing variable amounts of sillimanite, biotite, spinel and garnet with apparent pseudo-xenoliths of metapsammite and locally of more typical K-feldspar-bearing metapelite. The sample selected for geochronology contains around 90% cordierite, with minor garnet, biotite and sillimanite; it appears to have little or no quartz or K-feldspar. It was interpreted in the field to be a restite from partial melting, which formed a crystal "mush" (including metapsammite xenoliths) with all melt removed. The rocks have a bedding-parallel fabric but no evidence for non-coaxial strain (Scrimgeour 2013). The sample was selected for dating to determine the age and provenance of the sedimentary precursor, and the timing of granulite-facies metamorphism.
Kositcin, N., Scrimgeour, I.R., 2020. Summary of results. Joint NTGS-GA geochronology project: central and western Aileron Province. Northern Territory Geological Survey Record, 2020-011, 32p.

Eighty-two analyses were made of zircon cores. Two analyses (28.1 and 44.1) were >10% discordant and one analysis (76.1) had high counts of 204Pb. These analyses are considered unreliable and are excluded from further evaluation. The remaining 79 analyses have a range of 207Pb*/206Pb* dates between c. 3127 Ma and 2282 Ma, with maxima at c. 2875, 2685, 2660, 2510, 2480 and 2315 Ma. The two youngest core analyses with dates of c. 2287 and 2282 Ma define a statistically coherent pair with a weighted mean date of 2284 +/- 10 Ma (2sigma, MSWD = 0.24, probability of equivalence = 0.62). This is taken as a maximum depositional age for the sandstone protolith of the quartzite. Thirteen analyses of zircon rims were completed, three of which were duplicate analyses of the same site as a previous analysis. Post-analysis examination of rim analyses showed that three of these (53.1, 57.1 and 57.1A) slightly overlapped zircon cores and are not considered further. The remaining analyses have high U contents (673-2012 ppm) and low Th/U (0.03-0.12), with 207Pb*/206Pb* dates ranging between c. 1339 Ma and 1300 Ma. Eight of these 10 analyses define a statistically coherent group with a weighted mean date of 1334.3 +/- 4.4 Ma (MSWD = 1.3, probability of equivalence = 0.22). Two analyses (51.2 and 56.1) have slightly younger ages, but form statistical outliers and are interpreted to have undergone a small degree of Pb loss. The date of 1334.3 +/- 4.4 Ma is thus interpreted to reflect the timing of high-grade metamorphism of the quartzite.The weighted mean date of 2284 +/- 10 Ma (2sigma) defined by the youngest two core analyses is taken as a maximum depositional age for the sandstone protolith of the quartzite. The weighted mean date of 1334.3 +/- 4.4 Ma is interpreted to reflect the timing of high-grade metamorphism of the quartzite.
Quartzite was sampled from a prominent strike ridge in the Harbutt Range (MGA 483024E 7465554N). The quartzite forms part of a folded and possibly structurally repeated succession comprising quartzite, amphibolite, meta-chert, banded iron formation, granitic gneiss and ultramafic rock. A poorly defined layering is visible despite extensive recrystallization. In thin section, the quartzite consists almost entirely of quartz, with trace amounts of muscovite and zircon. The quartz consists of an interlocking mosaic of elongate, medium-grained domains with prominent undulose extinction that are separated from each other by narrow zones of fine-grained, recrystallized granoblastic quartz. These textures are consistent with recrystallization during an earlier pervasive high-grade metamorphic event, followed by later discrete recrystallization along grain boundaries during lower-grade deformation.

Barossa Complex
This sample was collected from the South Para River gorge in the northernHoughton Inlier, approximately 5 km E of Williamstown. The rock is a quartz dominated, K-feldspar bearing psammite. Minor biotite is also present defining a weak foliation. This sample comes from a 1 m thick, laterally extensive psammite layer from the steeply dipping psammopelite unit which dominates the northern Houghton Inlier. The average grain size is 1-2 mm, however some coarser grained patches are enriched in K-feldspar, which occurs as crystals up to 1 cm in size, suggesting that this rock has undergone partial melting. Some surfaces within this layer show slickenlines indicating some minor faulting present, however the psammite layer is not visibly offset. The surrounding psammopelites are composed of very fine-grained biotite and retrograde sericite, as well as quartzofeldspathic material which is concentrated into fine (~5 mm) bands. This segregation defines the gneissosity in these rocks which occurs at a low angle to the sedimentary structures in most areas. The gneissosity is obliterated by an overprinting cleavage in many areas. The psammopelite unit grades into a sillimanite bearing metapelite in the central and eastern Houghton Inlier. This sample is considered to have formed as a relatively well-sorted and compositionally mature quartz sandstone. It contained a minor proportion of clastic K-feldspar and a small amount of detrital argillaceous materials. Following burial and diagenesis, regional metamorphism with accompanying ductile deformation modified the rock. Quartz and K-feldspar grains suffered elongation and partial recrystallisation, and argillaceous components recrystallised to form fine-grained small aggregates of foliated biotite and sericite. The presence of biotite in the assemblage suggests that P-T conditions reached the middle greenschist facies.
Sample R695753 was collected from the South Para River gorge in the norther Houghton Inlier, about 5 km E of Williamstown and 1 km downstream from sample R695754.
Jagodzinski, E.A., Szpunar, M., Meaney, K., Fraser, G., 2020. SHRIMP U-Pb dating of the Barossa Complex, South Australia: exploring tectonic links between the Gawler Craton and Curnamona Province. Geological Survey of South Australia. Report Book, 2020/00017, 111p.

Two fractions were collected from this sedimentary sample during the magnetic separator process - an initial unsorted random separate collected at the first appearance of zircon (termed magnetic fraction), and a separate that has been refined further by the separation process (termed non-magnetic fraction). Handpicking of both fractions was only undertaken to ensure purity of the zircon content. As the sample is from a sedimentary rock, more than 60 grains were analysed to generate a detrital age spectrum, and only grains with surface imperfections were avoided. All analyses were undertaken on grains of the non-magnetic fraction, which may increase the chance of bias towards selected components of the provenance distributions. Analyses with common Pb contents greater than an arbitrary threshold of 0.50% have large uncertainties and therefore have been removed from further consideration, as have analyses that are more than 10% discordant. The 207Pb/206Pb ages for grains younger than ~1300 Ma become very imprecise. Due to the wide range of ages present within this sample (Archaean to <1000 Ma) 204Pb-corrected 207Pb/206Pb ages are used to describe the provenance spectra, whereas 204Pb-corrected 206Pb/238U ages are used to describe the youngest individuals.
Wilki Formation
The Wilki Formation conformably overlies the Puntapunta Formation and represents the uppermost unit of the Lamil Group. The unit comprises massive to bedded, fine- to medium-grained sandstone with minor shale and laminated sandstone. This sample was collected from the top of a small prograding package in the Wilki Range, near borefields about 7 km ENE of Telfer. It comprises a grey, fine to upper-medium grained, medium bedded quartzite, with possible cross stratification.
From hill-top near borefield memorial, about 7 km ENE of Telfer

Post-1830 Ma detrital zircons, incorporating the youngest detrital age component. Three-component mixture modelling of 43 analyses spanning the age range 1822-1663 Ma: youngest component (1701 +/- 9 Ma) comprises ~35% of the population.
Rhymetically laminated very fine-grained sandstone beds upto 10cm thick interbedded with thin siltstone interbeds

Detailed data not available (age in spreadsheet compiled by Allan Parsons from pers comms from N Neumann)
Kuridala Group
Poorly sorted, coarse to fine-grained quartzofeldspathic sandstone, thick bedded and massive

Poorly sorted, coarse to fine-grained quartzofeldspathic sandstone, thick bedded and massive

The youngest ages are part of the 1810-1730Ma cluster. The mixture modelling method produces populations at 1759+/-5Ma (54% of analyses) and 1777+/-5 Ma (46% of analyses). The younger population is interpreted to be the maximum depositional age
The basal Quilalar Formation at the Jamie Copper section was sampled ~5 m above the unconformity with the underlying Leichhardt Metamorphics mapped in Section 3 of Jackson et al. (1990), where it comprises grey, massive crystalline quartzite (2004169001), above a bed with flat-rounded sandstone clast impressions.

Ballara Quartzite
Grey laminated to thinly bedded very fine- to fine-grained sandstone. Qtz-rich fine beds to 1.5cm grading up into very fine sand internally laminated. All very low angle laminations. In mapped upper Ballara Quartzite near contact with overlying Corella Formation.

Parnell Formation
Stevens et al. (2008, AJES) paraphrased: "Sample 2002182005 was taken from the Parnell Formation southeast of the Allendale mine, from the same outcrop as sample 2005 analysed by Page & Laing (1992). The rock unit is a quartz-feldspar-biotite-garnet gneiss (Potosi-type gneiss). The sample was collected to evaluate the previous result in the light of advances in technology."
About 1 km southeast of Allendale mine.

Data migrated from OZCHRON1. Original comment: Maximum age estimate for the time of deposition of the sediment
Mallina Formation
Fine-grained greywacke sandstone, This sample is poorly sorted grit
Fine-grained greywacke sandstone, May Bore
Nelson, DR 1997, 118969: fine-grained greywacke sandstone, May Bore; Geochronology Record 445: Geological Survey of Western Australia, 4p.

maximum age of deposition of the sedimentary protolith
strongly deformed fine-grained meta-psammite
Sircombe, K.N., Cassidy, K.F., Champion, D.C., Tripp, G., 2007. Compilation of SHRIMP U-Pb geochronological data Yilgarn Craton, Western Australia, 2004-2006. Geoscience Australia. Record, 2007/01, 182p.

Irregully Formation
In thin section, the sample consists of irregular quartz grains commonly with well-defined rounded detrital cores (40%), inequigranular carbonate as cement and detrital grains (35%), and abundant lithic grains (15%) predominantly of low-grade metasedimentary rock. Accessory and trace minerals include metamorphic biotite and chlorite, and detrital tourmaline.
Wingate, MTD, Bodorkos, S and Sircombe, KN 2007, 148969: dolomitic quartz sandstone, Needle Hill Bore; Geochronology Record 686: Geological Survey of Western Australia, 6p.

Backdoor Formation
Sample GSWA 148976 is of the lowermost thick-bedded sandstone (0.4 m thick) in the Backdoor Formation on the northern limb of the Wanna Syncline, on Irregully Creek. The sample site is approximately 3 km north-northwest of Dog Pool Bore. The sample consists of fine-grained, parallel stratified quartz sandstone that in thin section consists of angular to subrounded monocrystalline quartz (~65%) and cherty clasts of microcrystalline quartz (1-2%) in a matrix of interstitial carbonate (~30%). Accessory and trace minerals include muscovite and partly altered biotite, leucoxene, brown tourmaline, and zircon. The paleocurrent direction at this site, determined from sole marks, is towards the south.
Wingate, MTD, Bodorkos, S and Sircombe, KN 2007, 148976: quartz sandstone, Dog Pool Bore; Geochronology Record 693: Geological Survey of Western Australia, 5p.

Kudjumarndi Quartzite
Bedded quartzite with micaceous beds.
From a track south of Myra Exploration Camp.

Lizard Schist
The Lizard Schist is a unit of muscovite-biotite schist and metapsammite, unconformably overlain by the Neoproterozoic Heavitree Quartzite around Warren Creek. The unit is dominated by biotite-muscovite-quartz schist, with a strong schistose S1 fabric, overprinted by a variably developed high-angle crenulation. Muscovite-bearing quartz-rich psammite layers occur at the centimetre to metre scale within the schist, and locally preserve tight to isoclinal F1 folds. Pegmatite veins intrude the schist, and are accompanied by tourmalinisation, with localised development of massive tourmalinite. Garnet occurs rarely as a minor constituent of the biotite-muscovite schist. At 733030mE, 7416974mN there is an ambiguous, highly strained contact with the 1683 Ma Talipata Granite. The abundance of granitic veins in the schist near the contact with the granite leads to a tentative interpretation that the granite intrudes the schist. However, the schist also has strong lithological similarities with the Ikuntji Metamorphics of the Iwupataka Metamorphic Complex. The metamorphic grade is lower to middle amphibolite facies. The sample selected for geochronology is a 1 m-wide grey crystalline quartzite layer within the schist (Cross et al., NTGS Record 2004-003).
Mt Liebig
Cross, A., Claoue-Long, J.C., Scrimgeour, I.R., Close, D.F., Edgoose, C.J., 2005. Summary of results. Joint NTGS-GA geochronology project southern Arunta Region. Northern Territory Geological Survey Record, 2004-003, CD, 61p.

Fiery Creek Volcanics
Numerous small pieces of felsic igneous rock, broken off four separate pebbles embedded in a 20 m-thick pebbly volcanic clast breccia near the top of the Fiery Creek Volcanics, at the base of the Boomerang North section. The Fiery Creek Volcanics are disconformably to unconformably overlain by the Surprise Creek Formation at this location.
no section N Boomerang anticline

Glen Helen Metamorphics
Metasediments within Glen Helen Metamorphics
Iwupataka Metamorphics (1640-1610 Ma), possibly postdating Glen Helen Metamorphics
The sample is from drillcore from NTGS Stokes Yard DDH3, at a depth of 49.3-56.0 m. The prospect is hosted in calc-silicate and forsterite marble, interlayered with pelite, psammite, amphibolite and rare quartzite. This forms part of a relatively limited area of metasedimentary rock within regionally extensive felsic migmatite of the 1690-1660 Ma Glen Helen Metamorphics. It is unclear whether this metasedimentary rock is also a constituent of the Glen Helen Metamorphics, and this sample was dated in order to test that possibility. Igneous zircon cores from a sample of felsic migmatite from the Glen Helen Metamorphics in MOUNT LEIBIG have a SHRIMP U-Pb age of 1688 +/- 16 Ma (Kinny 2002). Metamorphic rims show evidence for isotopic disturbance, with the oldest single rim analysis of 1640 Ma. Migmatitic granite from south of Belt Range in MOUNT LIEBIG has zircon cores at 1681 +/- 3 Ma, with oscillatory zoned prismatic overgrowths at 1661 +/- 8 Ma, which may reflect 1660 Ma igneous crystallisation with an inherited 1680 Ma zircon population (this report). These ages are in agreement with SHRIMP U-Pb dates of 1660 +/- 4 Ma and 1678 +/- 6 Ma for igneous zircon from the Glen Helen Metamorphics in HERMANNSBURG (Black and Shaw 1992, 1995). The present result suggests that the dated metasedimentary rock may belong to the 1640-1610 Ma Iwupataka Metamorphic Complex. The sample for dating is migmatitic pelite and psammite, selected from drillcore to have no granitic veins other than migmatitic leucosomes. The pelite contains biotite, garnet and sillimanite, with leucosomes that have been strongly deformed and transposed into the regional fabric. Localised zones of chlorite retrogression occur.
Stokes Yard DDH3

Provenance ranges from 2810 to 1845 Ma, with main peak at 1885-1845 Ma. Youngest grain: 1847 +/- 16 Ma.
fine to coarse sandstone metamorphosed upper greenschist facies, Sample from DDH2 85.65 - 96.32 m core

Ethiudna Subgroup
Dark-grey, fine-grained quartz-feldspar rock, with calc-silicate veins (meta-felsic ?tuff). In thin section, this sample displays a fine-grained granoblastic metamorphic texture with possible relict primary phenoclastic (primary volcanic fragmental) texture. Plagioclase is abundant, forming small equant anhedral twinned grains that form an equigranular granoblastic mosaic throughout the rock. Quartz is abundant, most occurs as small anhedral grains in textural equilibrium with the plagioclase. A smaller amount of quartz occurs as large anhedral grains up to ~2 mm in size. These have suffered varied degrees of elongation in the trace of an indistinct structure (?foliation), and are interpreted to represent primary quartz crystals of probable felsic volcanic origin. Muscovite occurs in trace amount as small flakes very sparsely scattered through the rock. Similarly, small biotite flakes are also present, but most have suffered partial to severe replacement by drab yellowish clays. Chlorite occurs in trace amount as small pleochroic pale green flakes with typical anomalous greenish grey interference colours. Opaques occur in trace amount as sparsely scattered small ragged grains. Trace apatite, rare allanite and rutile. This sample possibly formed as a felsic volcanogenic deposit. It contained minor irregularly scattered quartz crystals or crystal fragments, in a fine felsic matrix with accessory zircon. A tuffaceous origin is likely.

Provenance ranges fro 2620 to 1830 Ma, with main peak 1890-1830 Ma. Youngest grain: 1822 +/- 56 Ma.
greenish-grey thin to medium ms-bt-cl quartz schist, Sample from Tin DDH5 9.00 - 17.4 m core

93 analyses yield ages between~2945 and 1650 Ma, with a dominant cluster at ~1820?1780 Ma, & a smaller cluster at ~1860. 2 grains younger than main cluster were re-analysed. Combining ages for these 2 grains gave a weighted mean of 1697?12 Ma (MSWD 0.52)
Torpedo Creek Quartzite
Green coloured, fine grained, thinly bedded siltstone, Deep marine facies within TCQ
Leichhardt River Fault Trough. Gunpowder North

Gunpowder Creek Formation
Collected from a 3-10 cm thick pinkite with vague ripple lamination in its basal part (i.e. a current-reworked tuffaceous bed). The pinkite occurs in a section of stromatolitic dolostone, dolomudstone, very fine-grained dolomitic sandstone and siltstone at 265 m in the Crocodile Waterhole section.
@256m in NABRE's Crocodile waterhole Section

Williams and Collins (1996) interpret this 1594 +/- 6 Ma, zircon overgrowth age to represent the peak of granulite facies metamorphism in the Reynolds Range. The 1812 +/- 11 Ma age is a maximum deposition age for the pelite.
Reynolds Range Group
meta pelite
Reynolds Range
Williams, I.S., Buick, I.S., Cartwright, I., 1996. An extended episode of early Mesoproterozoic metamorphic fluid flow in the Reynolds Range, central Australia . Journal of Metamorphic Geology, 14(1), 29-47.

Continuum of zircon ages in the range 2710-2495 Ma. Weighted mean age calculated from the youngest six analyses
Acacia Gap Quartzite Member
quartzite
Rum Jungle
Cross, A., Claoue-Long, J.C., Scrimgeour, I.R., Ahmad, M., Kruse, P.D., 2005. Summary of results. Joint NTGS-GA geochronology project: Rum Jungle, basement to southern Georgina Basin and eastern Arunta Region 2001-2003. Northern Territory Geological Survey Record, 2005-006, 47p.

Surprise Bay Formation
sandy turbidite
Western King Island.

Port Sorell Formation
quartz sandstone
Central Tasmania Region
Port Sorell, northern Tasmania.

The age given here of 1580 +/- 6 Ma is a weighted mean age for analyses 9.2, 10.1 and 36.1. Vry et al. (1996) interpret this ~1580 Ma age to represent the timing of a granulite facies metamorphic event in the south-east part of the Reynolds Range. The youngest detrital grains indicate a max deposition age of ~1850 Ma and the ages between ~1600 and ~1800 Ma (spots 34, 40 and 11) represent mixed ages between the ~1850 Ma cores and the ~1580 Ma rims.
Vry, J., Compston, W., Cartwright, I., 1996. SHRIMP II dating of zircons and monazites: Reassessing the timing of high-grade metamorphism and fluid flow in the Reynolds Range, northern Arunta Block, Australia. Journal of Metamorphic Geology, 14(3), 335-350.

Page et al. (2005, Econ Geol, p. 663) paraphrased: "Ameroo Hill section: At Ameroo Hill, 22 km south of Mount Howden, three psammopelites, stratigraphically within about 6 m of each other, were sampled in the overturned eastern limb of a major regional synform. A 30-cm thick, hard resistant layer (sample 99185535) represents the base of the Plumbago Formation, lying about 1 m stratigraphically above the younger of two gossanous Bimba Formation calc-silicate horizons. This layer is in the same stratigraphic position as the tuffaceous bed sampled near Mount Howden. Stratigraphically younger psammopelites are friable, gray, and fine grained and include biotite psammite lenses in psammopelite. A sample of this friable material [99185531] and a third, stratigraphically younger, contiguous 2m-composite sample [99185532] were also taken at this location. The presence of both sillimanite and andalusite in these rocks reflects the regional amphibolite facies metamorphism."
Olary Domain

the outcrop lithologies are alternating metapelites and metapsammites in which the metapelites show evidence of partial melting but the more refractory metapsammites do not contain leucosomes and retain some semblance of original gross bedding. Zircons in a sample of psammite were studied to see if there is any differences in provenance pattern and/or metamorphic zircon isotope systematics between the two lithologies. Zircons in this rock, as in the other samples, are a heterogeneous range of detrital grains and these were probed at random to obtain a detrital provenance age spectrum. There is also a distinctive new population of ovoid, multifacetted zircons of metamorphic form, not found in the metapelite, and these were analysed separately. Only 35 analyses of the detrital grains were obtained so this is only a partial provenance spectrum, but the equivalence of the spectrum to the other samples is evident. There is a sparse presence of Archaean grains, and the same increasing abundance towards younger Proterozoic ages. The youngest individual detrital grain is 1834 ± 28 Ma (2¿). Alternatively, a statistically defined grouping of the 13 youngest grains has an acceptable MSWD of 1.3 and an average age of 1855 ± 7 Ma (2¿). In detail, the young end of the provenance spectrum in the metapsammite is similar to that of the low grade Lander Rock Formation sandstone , but different from both the granite and the metapelite. The granite and the metapelite both have a significant presence of heterogeneous zircons with ages younger than ca. 1850 Ma, which is not found in the two sandstone lithologies. Instead, the metapsammite has a optically distinctive and homogeneous population of metamorphic zircons. Eleven of these were probed (Figure 9b) and they reproduce with acceptable MSWD of 1.6 a mean 207Pb/206Pb age of 1803 ± 6 Ma (2¿).
200m SE of Ngadarunga granite
Claoue-Long, J.C., Edgoose, C., 2008. The age and significance of the Ngadarunga Granite in Proterozoic central Australia. Precambrian Research, 166(1-4), 219-229.

Semaphore Sand Member
muscovite-biotite-sillimanite paragneiss
Fraser Region
outcrop along beach about 6km southwest of Point Malcolm

Saddle Creek Formation
Victoria River Region
Eastern side of Victoria River Fault.

Fifima Sandstone
graded bedded med-gr sandstone with clasts, rip-up clasts, New Holland mine sub-hz underground GSUG0072 311.00-312.30 m -[informal_name: Fifima Sandstone]-
DDH GSUG0072
Dunphy, J.M., Fletcher, I.R., Cassidy, K.F., Champion, D.C., 2003. Compilation of SHRIMP U-Pb geochronological data, Yilgarn Craton, Western Australia, 2001-2002. Geoscience Australia. Record, 2003/15, 139p.

Age based on 6 youngest analyses; other provenance at ~2720, 2550-2435, ~2350, ~2220, ~1990 and 1895-1790 (65% of grains)
greywacke
Winnecke Region
Tanami
Cross, A., Claoue-Long, J.C., Crispe, A.J., 2003. Summary of results. Joint NTGS-GA geochronology project: Tanami Region 2001-2002. Northern Territory Geological Survey Record, 2003-006, 39p.

3 interpretations of data. Prot. Synthesis age based on youngest six individuals; major provenance is at 1890-1830 Ma, with subordinate modes or individual grains at 2010-1940 Ma (26% of grains), 2205-2045 Ma (7), 2535-2445 Ma (6), ~3110 Ma and 3400 Ma.
medium grained sandstone
Tanami

3 interpretations of data. Prot. Synthesis age based on youngest six individuals; major provenance is at 1890-1830 Ma, with subordinate modes or individual grains at 2010-1940 Ma (26% of grains), 2205-2045 Ma (7), 2535-2445 Ma (6), ~3110 Ma and 3400 Ma.
medium grained sandstone
Tanami
Cross, A.J., Crispe, A.J., 2007. SHRIMP U-Pb analysis of detrital zircon: a window to understanding the Paleoproterozoic development of the Tanami Region, northern Australia. Mineralium Deposita, 42(1-2), 27-50.

Alternative age interpretation based on average age of youngest provenance population.
Mount Charles Formation
weathered volcaniclastic rock

Eighty-two analyses were collected from 81 zircon cores, with the dark rims too thin to be analysed. Four analyses (36.1, 36.2, 38.1 and 41.1) have high common Pb (>1% 206Pbc) and three (14.1, 39.1 and 50.1) are >10% discordant. These analyses are unreliable and are not considered further. The remaining analyses form an essentially unimodal distribution, dominated by dates between c. 1826 and 1753 Ma, with a few grains ranging as old as c. 2571 Ma. The youngest 56 analyses have U contents of 46-596 ppm, Th/U values of 0.21-2.03 and 207Pb*/206Pb* dates between c. 1809 and 1753 Ma, which comprise a statistically coherent grouping having a weighted mean date of 1794.0 +/- 3.3 Ma (MSWD = 1.3, probability of equivalence = 0.05). This is considered to represent a maximum age for the deposition of the sedimentary protolith. Eighteen of the remaining 19 analyses have U contents of 67-532 ppm, Th/U values of 0.10-1.74 and 207Pb*/206Pb* dates ranging between c. 2571 and 1811 Ma, and are considered to represent older provenance components. The remaining analysis (37.1; U = 828 ppm, Th/U = 0.06) has a date of 1742 +/- 9 Ma (1sigma), but has an elevated common Pb content (0.37% 206Pbc) and is 6% discordant. This high-U grain might have been affected by minor Pb loss and is not considered a reliable constraint on the maximum depositional age of the protolith.The date of 1794.0 +/- 3.3 Ma defined by the youngest 56 analyses is considered to represent a maximum age for the deposition of the sedimentary protolith. Eighteen analyses were derived from older provenance components (between c. 2571 and 1811 Ma).
Fingoon Quartzite
The Fingoon Quartzite was sampled from the Fingoon Range in the central part of the Talbot Zone (MGA 418265E 7500080N). At this location, muscovite-bearing quartzite consists of thickly layered units folded about upright NW-trending, open to close folds overprinted by a NNW-striking fracture cleavage that is evident as a foliation in more muscovite-rich layers. In thin section, the quartzite consists of a mosaic of medium-grained quartz with narrow zones of fine-grained recrystallized quartz along grain boundaries. Muscovite is fine-grained, comprising about 5-10% of the rock, and has a weak preferred orientation.

Zircons from the Upper Mount Guide Quartzite were analysed during two SHRIMP sessions. More than 60 grains were analysed during the first session (March 2004, SHRIMP II) to generate a detrital age spectrum. During this session, only grains with surface imperfections were avoided. All analyses were made on zircons from the higher-quality non-magnetic fraction. This approach would have increased the chance of not finding all components of the provenance populations. The second session in May 2004 on SHRIMP RG involved the re-analysis of the youngest grains identified in the first session. These analyses were made in approximately the same place as the original, but with a larger ion beam, longer counting times on 204Pb, 207Pb and background, and more scans, in order to test the age reproducibility of these grains and to determine a more precise maximum age of deposition.
Mount Guide Quartzite
The upper Mount Guide Quartzite was sampled from the same outcrop section as the lower Mount Guide Quartzite, ~11 km east of Mt Isa, where it comprises a medium-grained, massive sandstone with low-angle internal laminations (2003169035). The upper Mount Guide Quartzite was sampled near the top of the hill (Trig point 497).
Leichhardt River Fault Trough. Mount Isa - Cloncurry Road

Contains resorbed quartz and K-feldpsar

Mathinna Supergroup
fine grained sandstone
Northeast Tasmania Region
Head of Queen of the Earth gully.

Bimba Formation
Deformed and sericite retrogressed, muscovite-K-feldspar-quartz-biotite psammopelitic schist. This sample displays a medium-grained foliated granoblastic metamorphic texture, overprinted by further deformation and partial recrystallisation, and later weak selective weathering effects. Muscovite is abundant, forming minor large foliated plates and abundant randomly oriented small flakes in subparallel laminae that contribute to a strong foliation through the rock. K-feldspar (microcline) forms equant anhedral grains that are weakly elongated in the trace of the foliation. Quartz forms small equant anhedral grains that form microgranular mosaics in indistinct lenses or laminae subparallel to the foliation. Biotite forms well-shaped pleochroic dull tan brown to pale yellow plates, aligned in the trace of the foliation. Tourmaline is uncommon, forming large stumpy subhedral prisms pleochroic in orange-yellow colours, aligned in the trace of the structure. Rutile forms scattered large equant euhedral yellow crystals, mantled by fine-grained microgranular recrystallised rutile. Goethite is present in minor amount as cryptocrystalline dense dark red replacements of precursor small blocky crystals. It is considered that this sample has suffered two metamorphic events: initial metamorphic recrystallisation at ?amphibolite facies grade generated a medium-grained foliated granoblastic assemblage of muscovite + K-feldspar + quartz + biotite + minor tourmaline + rutile. Subsequent deformation and partial recrystallisation generated a stronger structure, emphasised by recrystallised fine-grained sericite laminae which may have formed by complete replacement of precursor ?sillimanite or ?cordierite (neither of which is preserved for confirmation). Microgranular recrystallised rutile formed as mantles on the precursor coarse rutile crystals at this time. Subsequent weathering generated minor goethite as replacements of small opaque grains of unknown type.
Ameroo Hill saddle

Provenance spans range of 3540 to 1860 Ma, with modes at 3430-3415 Ma, 1965-1860 Ma, and minor groupings at ~3540 Ma, ~3390 Ma,3315 Ma, 3230 Ma, 3160 Ma, ~3040 Ma and ~2500 Ma. Age is based on 6 youngest analyses.
Mount Charles Formation
weathered volcaniclastic rock

primary interpretation from source depositional age. igneous crystallisation also noted on figure
Stag Creek Volcanics
Sample is a dark green-coloured agglomeratic volcanic.
near Gunlom Falls, ~1km north of El Sherana homestead.. Outcrop beside road to Coronation Hill

Dead Bullock Formation
meta sandstone
Birrindudu Region

3 interpretations of data. Prot. Synthesis age based on 6 youngest analyses; spectrum dominated by continuum of ages from 1903 and 1830 Ma; other provenance at 2080-1920 Ma, 2180-2145 Ma, ~2215 Ma, ~2340 Ma, ~2555-2415 Ma, 2630-2620 Ma and ~3525 Ma.
Tanami - Mavorick Granodiorite area

Age based on 7 youngest analyses; spectrum dominated by continuum of ages from 1980 and 1735 Ma; other provenance at ~3370 Ma, ~2930 Ma, ~2910 Ma, ~2710 Ma, ~2690 Ma and 2575-2100 Ma.
Pargee Sandstone

Vaughan Springs Quartzite
End of track WNW of North Bore, Coniston Station

Narrow provenance spectra between 1765 and 1675 Ma, with two overlapping populations. Age is of younger population.
Leisler Metamorphics
The rock is an upper amphibolite-facies migmatitic metasedimentary rock comprising metapelite, interlayered with lesser metapsammite. The metapelite comprises K-feldspar-quartz leucosome and biotite-sillimanite-andalusite melanosome. The leucosome is generally randomly oriented. Metapsammite layers, 2-5 cm thick, are locally present and are not migmatitic. A previous attempt to date this unit failed due to the very small size of zircons. Therefore this sample was selected to include as much metapsammite as possible (30% of the sample). There are no clear age constraints on this unit, as it comprises isolated outcrops, but it is currently interpreted to belong to the ca 1660 Ma Yaya Metamorphic Complex and to have been metamorphosed during the ca 1640 Ma Liebig Orogeny (Worden et al., NTGS Record 2006-006).
Warumpi Province

Kiangi Creek Formation
Sample GSWA 156614 was taken from medium- to thick-bedded, fine-grained sandstone in Fords Creek, 1.2 km northeast of the confluence of Fords Creek West and Fords Creek East. The sample site is a few metres below a distinctive unit of conophyton stromatolites near the base of the Kiangi Creek Formation. No paleocurrent indicators are preserved at this site, but the paleocurrent vector mean for the Kiangi Creek Formation is towards the southwest.

The detrital zircon grains in this rock yield a complex age pattern. The main populations, all of which define maximum ages for sedimentary deposition, are at about 1770Ma, 1900-2000Ma and 2600 Ma.
Daniel Creek Formation
micaceous quartzite
Georgetown Inlier, North Queensland

Bimba Formation
Low-intensity sericite altered, foliated feldspar-biotite-quartz psammopelitic schist. The rock displays a foliated granoblastic metamorphic texture, weakly modified by selective pervasive alteration. K-feldspar is moderately abundant, forming equant anhedral grains with ‘tartan’ twinning (ie microcline). Plagioclase forms anhedral grains of comparable size, but all display partial replacement by a small amount of tiny sericite flecks. Quartz is less abundant, occurring as small anhedral to ovoid grains. Together, the felsic minerals form a granoblastic mosaic throughout the rock. Biotite flakes are pleochroic from dark tan brown to pale yellow, are distributed uniformly through the rock, and their preferred orientation defines a moderately strong foliation. Tourmaline forms small equant subhedral crystals, strongly pleochroic from dark green to very pale green. Apatite is present in trace amount as small blocky subhedral grains. This sample may have formed as a mixed psammitic and pelitic sediment. No precursor layering is observable. The rock recrystallised in response to regional metamorphism, generating the foliated granoblastic assemblage of K-feldspar + plagioclase + biotite + quartz + trace tourmaline + apatite. At a later time, partial replacement of plagioclase generated minor fine-grained sericite.
Billeroo area

Warrina Park Quartzite
White massive quartzite with no mineral bands
Leichhardt River Fault Trough. Oxide Creek

White coloured massive quartzite with mineral bands, Upper qzt below reveinment surface in TCQ
Leichhardt River Fault Trough. Gunpowder North

Youngest individuals form part of the 1810 to 1760Ma cluster, & weighted mean 207Pb/206Pb age for this entire group (n = 22, MSWD = 1.09) is 1783+/-5Ma (2s). This is interpreted to be the Maximum depositional age
At 74m in Crocodile Waterhole section 95AW-09: Bigie Formation sample, where the unit outcrops as fine-grained, planar-laminated quartzo-feldspathic sandstone (2003169021). It is overlain by trough cross bedded pebbly sandstone (not sampled).
Leichhardt River Fault Trough. Crocodile Waterhole

Youngest individual 207Pb/206Pb ages form part of dominant 1810-1760Ma cluster, & weighted mean age for entire group (n = 42, MSWD = 0.95) is 1779+/-5Ma (2s). This is interpreted to be the Maximum depositional age
Alsace Quartzite
Grey coloured, medium-coarse grained massive sandstone.

Weighted mean age of youngest 3 grains of 64 analyses with range from ~2585 to 1670Ma; clusters at 1810-1760 & 1870-1840Ma
Grey coloured, fined grained, thinly bedded siltstone, Sampled thicker bed (approx. 40cm thick)
Leichhardt River Fault Trough. Bull Creek Syncline

Age based on six youngest grains from dominant continuum at 1825-1655 Ma. Other provenance at ~1865 Ma, ~2150 Ma and ~2525 Ma. Five concordant grains at 1580-1520 Ma, and one at ~1350 Ma were considered isotopically mixed and discarded.
Chewings Range Quartzite
MacDonnell Ranges
Cross, A.J., Claoue-Long, J.C., Scrimgeour, I.R., Close, D.F., Edgoose, C.J., 2005. Summary of results. Joint NTGS-GA geochronology project: southern Arunta Region. Northern Territory Geological Survey Record, 2004-003, 61p.

Page et al. (2005, Econ Geol, p. 663) paraphrased: "Dead Horse section: A graded, laminated psammopelite from this site [99185533] was sampled 2.5 km southwest of the Walparuta Creek section, on the upright western limb of the same Dead Horse synform. Good agreement is evident between the ages of the zircons from the Dead Horse and Walparuta Creek sections, at 1693 +/- 5 Ma and 1693 +/- 4 Ma, respectively. The underlying gossanous Bimba Formation thus has a minimum age of 1693 +/- 4 Ma."
Olary Domain

Berinka Volcanics
altered volcanic rock
Outcrop near hillcrest above a creek.

sheared granule/pebble-sized quartzite/chert-rich conglom, GC sample
outcrop on S. side of track
Dunphy, J.M., Fletcher, I.R., Cassidy, K.F., Champion, D.C., 2003. Compilation of SHRIMP U-Pb geochronological data, Yilgarn Craton, Western Australia, 2001-2002. Geoscience Australia. Record, 2003/15, 139p.

coarse-sand to grit sandst, minor shaley clasts, GC sample
Binduli deposits (Croesus), Navajo prospect, ND14 84.00-88.00 m
Fletcher, I.R., Dunphy, J.M., Cassidy, K.F., Champion, D.C., 2001. Compilation of SHRIMP U-Pb geochronological data, Yilgarn Craton, Western Australia, 2000-2001. Geoscience Australia. Record, 2001/47, 111p.

Data migrated from OZCHRON1. Original comment: This maximum depositional age is based on 13 euhedral grains of higher Th/U than the remainder. Other provenance ages in this tuffaceous siltstone are 1780-1830 Ma, 1880-1900 Ma, and ~2500 Ma. Other single grains 1700, 2030, 2200, 2320 Ma.
Yarrawirrie Formation
Core of south plunging syncline. Irregular dips
Pietsch, B.A., Plumb, K.A., Page, R.W., Haines, P.W., Rawlings, D.J., Sweet, I.P., 1994. A revised stratigraphic framework for the McArthur Basin, NT. In: Australian Mining Looks North - The Challenges and Choices (ed. Hallenstein, C.P.). 1994 AusIMM Annual Conference, Darwin, 5-9 August 1994. AusIMM. Publications, 5/94, 135-138.

The generally concordant or slightly discordant analyses is the maximum time of deposition of the volcaniclastic sediment.
Cooya Pooya Dolerite
rhyolite from Kialrah Rhyolite. plagioclase, abundant qtz,
~3km southwest of Warambie Homestead
Nelson, DR 1998, 144261: rhyolite, Bradley Well; Geochronology Record 272: Geological Survey of Western Australia, 4p.

Data migrated from OZCHRON1. Original comment: Maximum age for the deposition of the quartzite
Rudall Complex
Muscovite quartzite
Muscovite quartzite, Fingoon Quartzite
Nelson, DR 1995, 104989: muscovite quartzite, Fingoon Quartzite; Geochronology Record 5: Geological Survey of Western Australia, 4p.

Estimate of maximum deposition calculated from 'Unmix' function in ISOPLOT
quartz -rich metasediment lens within sillimanite-garnet-biotite migmatite metapelites.

Wings Sandstone
Tyennan Region
Road cut on Clear Hill road.

Strathgordon Metamorphic Complex
Strathgordon Tyennan
Small quarry adjacent to Gordon River Road.

Major provenance continuum at 1845-1640 Ma with other analyses at 1940 Ma, ~2369 Ma and 2555-2440 Ma (7). Age is based on six youngest individuals. Youngest individual: 1638 +/- 40.
Chewings Range Quartzite
ARUNTA
Cross, A.J., Claoue-Long, J.C., Scrimgeour, I.R., Close, D.F., Edgoose, C.J., 2005. Summary of results. Joint NTGS-GA geochronology project: southern Arunta Region. Northern Territory Geological Survey Record, 2004-003, 61p.

The mass fractionation correction of 0.204% was applied to Batch 2 to duplicate the 207Pb/206Pb ratio of QGNG for Batch 1, so that unknowns from both batches could be combined.
Chilling Sandstone
Chilling Sandstone Volcanics
Sample not necessarily representative of these mapped volcanics.
Sampled from boulders in a valley below a hill.

Mount Basedow Gneiss
Eastern side of Mt Basedow.. Quartzite from outcrop along Jim Jim Rd.

Within pelite-dominated lithologies assigned as metamorphosed equivalents to the Reynolds Range Group, a psammite layer was sampled at a location dominated by partially melted pelite lithologies. Bedding is preserved within the psammite even though it adjoins large melt bodies formed in the surrounding pelites. The lithological association is similar to the presence of rare thin sandstone horizons within the Reynolds Range Group Pelite Unit. The detrital zircon age pattern comprises ages distributed across a series of populations in the age range ca. 1840-2700 Ma, with prominent groupings at ca. 1860 Ma, ca. 2200 Ma, and ca. 2500 Ma. The 1840-1880 Ma age population, while prominent, does not dominate the spectrum as is found in regional samples of Lander Rock Formation. Instead, the distribution of ages across the 1840-2700 Ma range is similar to that described above in the unmetamorphosed Mount Thomas Quartzite, and in the unassigned sandstones immediately underlying the unconformity in the Reynolds Range. Discrimination on the basis of the youngest measured ages is inherently uncertain, because the possibility that metamorphism has generated misleading young ages in some grains cannot be ruled out. However in this case the youngest measured ages ¿ three grains with a mean age of 1799 ± 8 Ma - are consistent with post-Stafford Event deposition, and this constraint equates with the youngest detrital zircons found in unmetamorphosed equivalent with the same provenance spectrum.

Putardi Quartzite
The Putardi Quartzite occurs as prominent ridges that include Mount Udor, Mount Putardi and Mount Peculiar, over a discontinuous strike length of 100 km. The unit is dominated by crystalline metasedimentary quartzite, often containing kyanite and/or muscovite, interlayered with quartz-muscovite and muscovite-biotite phyllite and schist. Most commonly, the Putardi Quartzite occurs within a broad zone of high non-coaxial strain (Udor Deformed Zone), in which it is structurally repeated and interleaved with granite. This high strain typically obscures the original relationship between the Putardi Quartzite and adjacent granites. However, at Mount Putardi, the Putardi Quartzite forms a large basinal structure that is relatively unaffected by non-coaxial strain, and it is interpreted to overlie the 1663 Ma Udor Granite. Strain that is associated with the Udor Deformed Zone is attributed to the 1590 Ma Chewings Orogeny, and the quartzite is truncated by undeformed dykes of Stuart Pass Dolerite. The sample is a clean, crystalline, muscovite-bearing quartzite from immediately adjacent to the Browns Bore-Mount Liebig track.
Immediately adjacent to the Browns Bore-Mount Liebig track.

quartz metasedimentary rock
Vry, J., Compston, W., Cartwright, I., 1996. SHRIMP II dating of zircons and monazites: Reassessing the timing of high-grade metamorphism and fluid flow in the Reynolds Range, northern Arunta Block, Australia. Journal of Metamorphic Geology, 14(3), 335-350.

Youngest detrital zircon age component. Unmixing of the 13 post-1700Ma analyses using a 2-component model yielded ages of 1633 ? 16 Ma (2s, fraction = 0.69, i.e. about 9 analyses), and 1679 ? 25 Ma (2s, fraction = 0.31, i.e. about 4 analyses). In Queensland Geological Record 2011/03, the weighted mean of the youngest 9 analyses is preferred as the maximum age for deposition.
Doomadgee Formation
poosible tuff within Doomagee Formation
Carson, C.J., Hutton, L.J., Withnall, I.W., Perkins, W.G., Donchak, P.J.T., Parsons, A., Blake, P.R., Sweet, I.P., Neumann, N.L., Lambeck, A., 2011. Joint GSQ-GA NGA geochronology project Mount Isa region, 2009-2010. Queensland Geological Record, 2011/03, 211p.

Youngest detrital zircon age component. Age range: 1612-1520 Ma.
Burangoo Sandstone
Collexted by Ian Sweet (GSQ)
Carson, C.J., Hutton, L.J., Withnall, I.W., Perkins, W.G., Donchak, P.J.T., Parsons, A., Blake, P.R., Sweet, I.P., Neumann, N.L., Lambeck, A., 2011. Joint GSQ-GA NGA geochronology project Mount Isa region, 2009-2010. Queensland Geological Record, 2011/03, 211p.

Youngest detrital zircon age component. Age range: 1666-1630 Ma.
Starcross Formation
Sampled by Allan Parsons (GSQ) for detrital U-Pb zircon SHRIMP geochronology
Carson, C.J., Hutton, L.J., Withnall, I.W., Perkins, W.G., Donchak, P.J.T., Parsons, A., Blake, P.R., Sweet, I.P., Neumann, N.L., Lambeck, A., 2011. Joint GSQ-GA NGA geochronology project Mount Isa region, 2009-2010. Queensland Geological Record, 2011/03, 211p.

Pandurra Formation
Pandurra Formation - Red Rock Hill
Gawler Region
Fraser, G.L., Neumann, N.L., 2010. New SHRIMP U-Pb zircon ages from the Gawler Craton and Curnamona Province, South Australia, 2008-2010. Geoscience Australia. Record, 2010/16, 256p.

Moonabie Formation
Moonabie Fm - SE Mt Whyalla
Gawler Region
Fraser, G.L., Neumann, N.L., 2010. New SHRIMP U-Pb zircon ages from the Gawler Craton and Curnamona Province, South Australia, 2008-2010. Geoscience Australia. Record, 2010/16, 256p.; Szpunar, M., Fraser, G., 2010. Age of deposition and provenance of Palaeoproterozoic basins on north-eastern Eyre Peninsula. Geological Survey of South Australia. Report Book, 2010/00008, 26p.

Youngest detrital zircon age component. Age range: 1584-1560 Ma.
Schultz Sandstone Member
Collected by Ian Sweet (GSQ) for detrital zircon geochronology

Pandurra Formation
Pandurra Formation - Mt Laura
Gawler Region
Fraser, G.L., Neumann, N.L., 2010. New SHRIMP U-Pb zircon ages from the Gawler Craton and Curnamona Province, South Australia, 2008-2010. Geoscience Australia. Record, 2010/16, 256p.

Corunna Conglomerate
Corunna - lower green Sst, Baxter Hills
Fraser, G.L., Neumann, N.L., 2010. New SHRIMP U-Pb zircon ages from the Gawler Craton and Curnamona Province, South Australia, 2008-2010. Geoscience Australia. Record, 2010/16, 256p.

Corunna Conglomerate
volcanic clast in Corunna

Corunna Conglomerate
Corunna - upper green Sst, Baxter Hills

felsic volcaniclastic rock

Granite

Bleechmore Metamorphics
Coarse-grained, garnet-rich leucogneiss/migmatite that lies within mostly high-grade metasediments and mafic granulites of the Bleechmore Granulite. The sample was taken well within the unit to distinguish it from the previously dated sample of Maidment et al (2005) which was sampled just below the contact with the Mendip Metamorphics to the north of the main Bleechmore Granulite.
Bodorkos, S., Beyer, E.E., Edgoose, C.J., Whelan, J.A., Webb, G., Vandenberg, L.C., Hallett, L., 2013. Summary of results. Joint NTGS-GA geochronology project: Central and eastern Arunta Region, January 2008-June 2011. Northern Territory Geological Survey Record, 2013-003, 66p.

Aileron Metamorphics
Qtz-Felds-Bio-Garnet-sillimanite migmatitic metapelite. The Aileron Metamorphics are interpreted to be a granulite facies equivalent of the 1860-1830 Ma Lander Rock Formation. This sample is from the easternmost extension of the Reynolds Range. The Aileron Metamorphics themselves have not been dated, but SHRIMP U-Pb dating of high grade Lander Rock Formation metasediments further to the west in the Reynolds Range (NAPPERBY) shows high grade metamorphism occurred during the 1600-1580 Ma Chewings Orogeny. It is expected that the rims on this sample will give the same metamorphic history.
Bodorkos, S., Beyer, E.E., Edgoose, C.J., Whelan, J.A., Webb, G., Vandenberg, L.C., Hallett, L., 2013. Summary of results. Joint NTGS-GA geochronology project: Central and eastern Arunta Region, January 2008-June 2011. Northern Territory Geological Survey Record, 2013-003, 66p.

Inverway Metamorphics
Basement to the Birrindudu Basin in the Victoria River region, the Inverway Metamorphics, is exposed as two small inliers (<3 km2 in total) on LIMBUNYA and comprise steeply dipping, cross-bedded to massive arkosic quartz-muscovite schist with minor metasiltstone and felsic volcanics (Sweet et al., 1974a, b; Cutovinos et al., 2002; Carson, 2013). The thickness of the unit is unknown. Metamorphic grade is sub-greenschist to greenschist facies (Sweet et al., 1974a, b; Cutovinos et al., 2002). The absolute age of these rocks has not been determined; however they likely correlate with rocks of the Halls Creek or Pine Creek Orogens (Cutovinos et al., 2002). The sample was collected near #19 Bore, Limbunya Station, and is a steeply dipping, cross-bedded to massive arkosic quartz-muscovite schist with minor interbedded metasiltstone and felsic volcanics (Carson, 2013; Cutovinos et al., 2002).
Victoria River Region
Kositcin, N., Carson, C.J., 2017. New SHRIMP U-Pb zircon ages from the Birrindudu and Victoria Basins, Northern Territory. Geoscience Australia. Record, 2017/16, 84p.

Provenance clusters spanning 1899-1846 Ma; mixture modelled for maximum depositional age Youngest of two-component mixture modelling of 42 analyses; fraction = 0.83 (i.e. about 35 analyses), misfit = 0.979. Interpreted as best (conservative) maximum age for deposition of sedimentary precursor.
Inverway Metamorphics
collected for U-Pb determination of Inverway Metamorphics.
Victoria River Region
Carson, C.J., 2013. The Victoria and Birrindudu Basins, Victoria River region, Northern Territory, Australia: a SHRIMP U-Pb detrital zircon and Sm-Nd study. Australian Journal of Earth Sciences, 60(2), 175-196.

Provenance clusters spanning 2015-1801 Ma; mixture modelled for maximum depositional age Youngest of six-component mixture modelling of 101 analyses; fraction = 0.08 (i.e. about 8 analyses), misfit = 0.519. Interpreted as best (conservative) maximum age for deposition of sedimentary precursor.
Stirling Sandstone
Collected for detrital zircon U-Pb study
Carson, C.J., 2013. The Victoria and Birrindudu Basins, Victoria River region, Northern Territory, Australia: a SHRIMP U-Pb detrital zircon and Sm-Nd study. Australian Journal of Earth Sciences, 60(2), 175-196.

Maximum age for deposition of sedimentary rock Age range 1647-1623 Ma.
Wickham Formation
Collected for detrital zircon U-Pb SHRIMP study
Wiso Region
Carson, C.J., 2013. The Victoria and Birrindudu Basins, Victoria River region, Northern Territory, Australia: a SHRIMP U-Pb detrital zircon and Sm-Nd study. Australian Journal of Earth Sciences, 60(2), 175-196.

Gilberton Formation
The most extensive outcrop area of Gilberton Formation is one of about 120 km2 near Gilberton. Other occurrences are scattered through the central part of the Georgetown Region mainly preserved beneath areas of Carboniferous volcanic rocks. All outcrops lie within the Georgetown Region (Withnall et al., 1997). This sample was collected from drillcore (DDH 9025; 32.68-32.70 m). The Late Devonian to Early Carboniferous Gilberton Formation predominantly consists of quartzose to feldspathic fluvial sandstones and conglomerates, with sparse tuffs and volcaniclastic sedimentary rocks the latter occurring locally in the Maureen area (Withnall et al., 1997a, b). Macroflora indicate deposition of the Gilberton Formation between the late Famennian and Visean (Withnall et al., 1997a). The sample was collected in order to determine the depositional age of the unit (on the premise that the sample may represent a volcanic tuff).
Neumann, N.L., Kositcin, N., 2011. New SHRIMP U-Pb zircon ages from North Queensland 2007-2010. Geoscience Australia. Record, 2011/38, 82p.

Lady Clayre Formation
Collected by Lex Lambeck for detrital U-Pb geochronology

Harts Range Metamorphic Complex
Locally migmatitic sillimanite-biotite-feldspar-quartz ± garnet ± muscovite metapelite, purportedly Harts Range Metamorphic Complex but kyanite previously unknown from there. Detrital spectrum and rim ages; possibly two rim events.
Bodorkos, S., Beyer, E.E., Edgoose, C.J., Whelan, J.A., Webb, G., Vandenberg, L.C., Hallett, L., 2013. Summary of results. Joint NTGS-GA geochronology project: Central and eastern Arunta Region, January 2008-June 2011. Northern Territory Geological Survey Record, 2013-003, 66p.

Kanandra Metamorphics
Pervasively-melted Kanandra metapelite with coarse sillimanite (to 30 mm) and garnet, well-developed 'stringer' melanosomes. Psammite forms minor coherent layers 1-10 cm thick - pelite dominant, with abundant melt invading adjacent, volumetrically dominant mafics.

alt. conservative estimate of the maximum age of deposition: 1625 +/- 36 Ma. MSWD = 1.3. N=4 youngest
The 62 analyses in combined groups indicate dates that define significant age components at c. 1625, 1774, 1837, and 1884 Ma and several minor components in the range 3173-1198 Ma. These are interpreted as the ages of zircon-crystallizing rocks in the detrital source region of the sandstone, or the ages of detrital components within sediments which have been reworked.
pebbly sandstone
Kirkland, CL, Wingate, MTD, Spaggiari, CV and Tyler, IM 2009, 184339: sandstone, Pollock Hills; Geochronology Record 817: Geological Survey of Western Australia, 5p.

alt. conservative estimate of the maximum age of deposition: 1775 +/- 7 Ma. MSWD = 1.21. N=15 youngest
The 52 analyses in combined Groups indicate dates at c. 1849, 1964, and 2307 Ma, and several minor components spanning the range 2695-1750 Ma. These are interpreted as the ages of zircon-crystallizing rocks in the detrital source region of the sandstone, or the ages of detrital components within sediments which have been reworked.
Kirkland, CL, Wingate, MTD, Spaggiari CV and Tyler, IM 2009, 184341: quartzite, Lake Mackay; Geochronology Record 818: Geological Survey of Western Australia, 5p.

Birrindudu Region
Kirkland, CL, Wingate, MTD, Spaggiari CV and Tyler, IM 2009, 184342: sandstone, Alec Ross Range; Geochronology Record 819: Geological Survey of Western Australia, 5p.

Entia Metamorphics
Sillimanite-bearing migmatitic gneiss overprinted by coarse, randomly-oriented kyanite of probable Alice Springs age. Sampled in low-strain area of Entia dome, near Huckitta Granodiorite. Sill defines shallow SW-plunging lineation, which may be either Strangways or Larapinta age.

. Range of individual ages: 1659-1589 Ma.
Milo beds
Collected to further assess the age of the Tommy Creek Block.

Population encompassing the youngest detrital zircon age component. Fraction of 3-component mixture model of 64 analyses = 0.08 (i.e. about 5 analyses).
possible Torpedo Creek Formation??
Magee, C.W., Withnall, I.W., Hutton, L.J., Perkins, W.G., Donchak, P.J.T., Parsons, A., Blake, P.R., Sweet, I.P., Carson, C.J., 2012. Joint GSQ-GA geochronology project, Mount Isa Region, 2008-2009. Queensland Geological Record, 2012/07, 134p.

Population encompassing the youngest detrital zircon age component. Fraction of 3-component mixture model for 8 analyses = 0.36 (i.e. about 3 analyses).
Boodjamulla Formation
Collected for SHRIMP detrital zircon U-Pb study. Sampled by Ian Sweet.
Magee, C.W., Withnall, I.W., Hutton, L.J., Perkins, W.G., Donchak, P.J.T., Parsons, A., Blake, P.R., Sweet, I.P., Carson, C.J., 2012. Joint GSQ-GA geochronology project, Mount Isa Region, 2008-2009. Queensland Geological Record, 2012/07, 134p.

Population encompassing the youngest detrital zircon age component. Fraction of 3-component mixture model of 52 analyses = 0.23 (i.e. about 12 analyses). Called Surprise Creek Formation in GA Geochron Delivery.
Sampled by Paul Blake (GSQ), site not visited by Carson

Population encompassing the youngest detrital zircon age component. Fraction of the 11 analyses in the 2-component mixture model = 0.66 (i.e. about 7 analyses).
Doherty Formation
biotite metasedimentary rock

Youngest detrital component Age range 1607-1589 Ma.
Weaner Sandstone
collected for U-Pb zircon detrital SHRIMP study and Sm-Nd isotopic study

sandstone + siltstone

pebbly sandstone

felsic volcaniclastic sandstone

Corunna - upper green Sst, Uno Range

Corunna - white Sst, Uno Range

The sample was collected from drillhole GSQ Georgetown 4, by Ian Withnall (GSQ), and comprises material from two depth intervals (153.39-158.13 m and 160.20-161.64 m) which were combined prior to processing for zircon. The sample is a volcanic rock within the Candlow Formation, Etheridge Province of the Georgetown Inlier. The Candlow Formation lies stratigraphically above the Lane Creek Formation and is therefore potentially younger than the ca. 1655 Ma leucogabbro sill in that unit (Withnall et al., 1988; Black et al., 1998; Baker et al., 2010). Black and McCulloch (1984) completed Sm-Nd analysis on the volcanic rock within the Candlow Formation which indicates a juvenile magmatic input. This juvenile magmatic input was dismissed by Black and McCulloch (1984) as alteration effects. However more detailed isotopic work by Lambeck (2011) and Lambeck et al. (2012) suggests the juvenile input is part of a larger juvenile volcanic suite that is represented throughout Proterozoic Australia. The volcanic unit was interpreted by A. Lambeck and I.Withnall to have basal peperitic textures. Dating the volcanic rock was thought to be able to provide direct timing of felsic magmatism and sedimentation in the Georgetown Inlier.
GSQ Georgetown 4
Lambeck, A., 2011, Basin analysis and the geochemical signature of Paleoproterozoic sedimentary successions in northern Australia: Constraints on basin development in respect to mineralisation and paleoreconstruction models. PhD. thesis, 157p.

This sample was collected by A. Lambeck from the A2 Prospect near Croydon, Georgetown Inlier, to assess if the Phanerozoic input in sample 1977975 was possible zircon contamination.
Lambeck, A., 2011, Basin analysis and the geochemical signature of Paleoproterozoic sedimentary successions in northern Australia: Constraints on basin development in respect to mineralisation and paleoreconstruction models. PhD. thesis, 157p.

Probable youngest detrital zircon age component. Age range: 1645-1592 Ma.
Tidna Sandstone
Collected by Ian Sweet (for GSQ) for detrital zircon geochronology
Georgina Region

Double Crossing Metamorphics
Sampled by Allan Parsons for detrital geochronology (GSQ)

unnamed pelitic schist
The sample is a pelitic schist characterised by large quartz augen in a fine-grained muscovite-rich matrix. The sample is from an unnamed unit on the 2nd edition NAPPERBY mapsheet, which appears to be part of the metasedimentary rocks surrounding the Wangala Granite. The unit may be related to the nearby Wickstead Creek Beds which are interpreted as a calcareous equivalent of the Lander Rock Formation.
Kositcin, N., Beyer, E.E., Whelan, J.A., Close, D.F., Hallett, L., Dunkley, D.J., 2013. Summary of results. Joint NTGS-GA geochronology project: Arunta Region, Ngalia Basin,Tanami Region and Murphy Province July 2011-June 2012. Northern Territory Geological Survey Record, 2013-004, 39p.

alt. conservative estimate of the maximum depositional age: 974 +/- 25 Ma. MSWD=0.79. N=2 youngest
The data for combined groups age components at c. 1612, 1421, 1152, and 1061 Ma are interpreted as the ages of zircon crystallizing rocks in the detrital source region(s), or as the ages of detrital components within sediments that have been reworked into this rock.
Wingate, MTD, Kirkland, CL and Haines, PW 2013, 143741: sandstone, Angas Hills; Geochronology Record 1106: Geological Survey of Western Australia, 5p.

British Empire Granite
Broadview Schist, collected by Mike Szpunar, PIRSA
Fraser, G.L., Neumann, N.L., 2010. New SHRIMP U-Pb zircon ages from the Gawler Craton and Curnamona Province, South Australia, 2008-2010. Geoscience Australia. Record, 2010/16, 256p.; Szpunar, M., Fraser, G., 2010. Age of deposition and provenance of Palaeoproterozoic basins on north-eastern Eyre Peninsula. Geological Survey of South Australia. Report Book, 2010/00008, 26p.

Qtz-felds-bio metapsammitic gneiss, with occasional narrow leucosomes, interpreted to be an amphibolite facies equivalent of the 1860-1830 Ma Lander Rock Formation. The sample is from the easternmost exposures of this unit, and sporadic outcrop trends NW into mapped Lander Rock Formation (MOUNT PEAKE). Metamorphic age should correspond with the 1810-1800 Stafford Event. It is separated from the Aileron Metamorphics sample (CJE222) by the NW trending Woolanga Lineament, interpreted as the northern and western boundary of rocks affected by the Chewings Orogeny.

Provenance clusters spanning 1681-1611 Ma; mixture modelled for maximum depositional age Youngest of two-component mixture modelling of 8 analyses; fraction = 0.20 (i.e. about 2 analyses), misfit = 0.969. Interpreted as best (conservative) maximum age for deposition.
Neave Sandstone
Collected for zircon U-Pb SHRIMP study
Wiso Region

Hughie Sandstone
The Hughie Sandstone (Wattie Group, Sweet et al., 1974 a, b) forms low, weakly terraced hills adjacent to Wattie Creek in central–eastern LIMBUNYA (Cutovinos et al., 2002). It is composed of cross-bedded and ripple marked, fine- to medium-grained, immature quartz sandstone up to 90 m thick probably deposited in transgressive, shallow marine and near marine conditions that included minor subaerial exposure. The unit is apparently conformable on the Burtawurta Formation in LIMBUNYA (Cutovinos et al., 2002; Dunster and Ahmad, 2013a). The Hughie Sandstone was sampled at the top of the unit, near the inferred contact with the overlying Mount Sanford Formation on Riveren Station (near Neave Creek bore, Carson, 2013). At this location the Hughie Sandstone is a mature, ferruginous (with reduction spots), fine-grained quartz sandstone with rounded quartz grains. Asymmetrical ripples are preserved on bedding surfaces, and there are rip-up clasts associated with cross-bedding.
Wiso Region
Kositcin, N., Carson, C.J., 2017. New SHRIMP U-Pb zircon ages from the Birrindudu and Victoria Basins, Northern Territory. Geoscience Australia. Record, 2017/16, 84p.

Seale Sandstone
The Seale Sandstone (Wattie Group; Sweet et al., 1974a, b; Beier et al., 2002; Dunster and Ahmad, 2013a) conformably overlies the Gibbie Formation and has a gradational contact with the conformably overlying Timber Creek Formation of the Bullita Group (Dunster and Cutovinos, 2002). The unit consists predominantly of medium-grained quartz sandstone deposited under high energy, shallow marine transgressive conditions. It is 111 m thick in WAVE HILL and known to contain live oil (Dunster and Ahmad, 2013a). The Seale Sandstone contains up to 10–15% feldspar, clay and chert fragments, and is strongly cross-stratified (Sweet et al., 1974a, b; Beier et al., 2002; Cutovinos et al., 2002). The unit is poorly exposed and was sampled from locally derived rubbly debris adjacent to the Buntine Highway. At this location the Seale Sandstone is a reddish, ferruginous, medium- to fine-grained lithic sandstone, with symmetrical ripples preserved on bedding surfaces.
Kositcin, N., Carson, C.J., 2017. New SHRIMP U-Pb zircon ages from the Birrindudu and Victoria Basins, Northern Territory. Geoscience Australia. Record, 2017/16, 84p.

Cross, A., Jaireth, S., Hore, S., Michaelsen, B.H., Schofield, A., 2010. SHRIMP U-Pb detrital zircon results, Lake Frome region, South Australia. Geoscience Australia. Record, 2010/46, 28p.

unnamed quartzite (west Lake Gilles)
quartzite west of Lake Gilles

metasandstone
Musgrave Region
Kirkland, CL, Wingate, MTD and Evins, PM 2010, 190292: metasandstone, Mount Finlayson; Geochronology Record 935: Geological Survey of Western Australia, 5p.

A package of north-northwesterly trending, southwesterly dipping metasedimentary rocks, belonging to the Biranup Zone, are exposed along Ponton Creek, about 15-20km north of Zanthus and the transcontinental railway. These rocks, of which sample 194731 is representative, are mostly psammitic gneisses with sparse garnet and, locally, thin leucosomes. Fine bedding laminations and cross-bedding are preserved and indicate younging to the west-southwest. The foliation, defined by biotite and quartz, is sub-parallel to bedding, and contains a mineral lineation that plunges shallowly to the southwest. Locally, the psammitic gneiss has been intruded by metagranite and coarse pegmatite (neither of which is present in the sample), and is flanked by migmatitic granite gneiss and foliated metagranodiorite that exhibit the same foliation and lineation.

conservative alternate max depositional age 207Pb/206Pb: 1862 +/- 5Ma. MSWD = 1.4. N=20
Kimberley Region
Kirkland, CL, Wingate, MTD, Tyler, IM and Sheppard, S 2010, 182101: quartz sandstone, Pentecost River; Geochronology Record 883: Geological Survey of Western Australia, 5p.

conservative alternate maximum depositional age 207Pb/206Pb: 1864 +/- 4 Ma. MSWD = 1.01. N = 28 youngest
pebbly sandstone
Kimberley Region
Kirkland, CL, Wingate, MTD and Tyler, IM 2010, 182107: quartz sandstone, Inglis Gap; Geochronology Record 888: Geological Survey of Western Australia, 5p.

conservative alternate maximum depositional age 207Pb/206Pb: 1869 +/- 7 Ma. MSWD = 1.4. N = 15 youngest
Kimberley Region
Kirkland, CL, Wingate, MTD and Tyler, IM 2010, 182105: quartz sandstone, The Bench; Geochronology Record 886: Geological Survey of Western Australia, 5p.

the ages of detrital components within sediments that have been reworked into this rock
Kirkland, CL, Wingate, MTD and Tyler, IM 2010, 182104: quartz sandstone, Saddler Spring; Geochronology Record 885: Geological Survey of Western Australia, 5p.

This sample was collected from a turbidite sequence at the base of Mount Oxley, approximately 30 km east-south-east from the town of Bourke. The in-situ outcrop is in a drainage gutter adjacent to, and east of, the access road to Mount Oxley summit. The sample comes from a ~20 cm thick coherent sandy bed within strongly cleaved and folded phyllites. Bedding dips moderately to the southeast and a slaty cleavage is parallel to bedding. The slaty cleavage is overprinted by a weak crenulation cleavage in metamudstones immediately to the east. The presence of the bedding-parallel and crenulation cleavages draws comparison to structures observed in Girilambone Group rocks to the south, where these fabrics are attributed to the Late Ordovician-Early Silurian Benambran Orogeny (Burton et al., 2012). The sample site is on the northeastern flank of Mount Oxley, and rocks here have been correlated with other exposures on the flanks of Mount Oxley, including sample OXCOSJT0861.01A (GA 2135490). This sample was analysed to collect a detrital zircon age spectrum for comparison with, for example, turbiditic rocks of the Girilambone Group of the northern Lachlan Orogen.
Fraser, G.L., Gilmore, P.J., Fitzherbert, J.A., Trigg, S.J., Campbell, L.M., Deyssing, L., Thomas, O.D., Burton, G.R., Greenfield, J.E., Blevin, P.L., Simpson, C.J., 2014. New SHRIMP U-Pb zircon ages from the Lachlan, southern Thomson and New England orogens, New South Wales: February 2011-June 2013. Geoscience Australia. Record, 2014/53, 217p.

Provenance clusters spanning 1888-1794 Ma; mixture modelled for maximum depositional age. Youngest of two-component mixture modelling of 37 analyses; fraction = 0.64 (i.e. about 24 analyses), misfit = 0.928. Interpreted as best (conservative) maximum age for deposition of sedimentary precursor.
Westmoreland Conglomerate
tuff within Westmoreland Conglomerate Immediately overliying unconformity with mm basement
Murphy Region
Carson, C.J., Hollis, J.A., Glass, L.M., Close, D.F., Whelan, J.A., Wygralak, A., 2011. Summary of results. Joint NTGS-GA geochronology project: East Arunta Region, Pine Creek Orogen and Murphy Inlier, July 2007-June 2009. Northern Territory Geological Survey Record, 2010-004, 84p.

Weaner Sandstone
The Weaner Sandstone (Sweet et al., 1974a, b) is only exposed in VICTORIA RIVER DOWNS, where it forms a crescent shaped belt of subcrop and small scarps around the northern and western margin of the Fitzgerald Range and adjacent to Gordon Creek. The Weaner Sandstone comprises thinly to thickly cross-bedded sandstone and minor polymictic pebble conglomerate with clasts of volcanic rock, typically 3-15 m thick and deposited under shoaling, shallow marine conditions (Dunster and Ahmad, 2013a). Stratigraphic drilling by the NTGS (Dunster and Cutovinos, 2002) showed that the unit rests unconformably on the underlying dolomitic siltstone and sandstone of the Bynoe Formation (Beier et al., 2002); the upper contact is conformable with the overlying Battle Creek Formation (Carson, 2013). The sampled unit is a medium- to coarse-grained (up to 5 mm grain size) poorly-sorted, texturally immature sandstone, comprised of angular to sub-angular quartz grains and lithic fragments, with weakly defined bedding and internal cross-bedding.

Youngest zircon age components. Fraction of 2-component population ~ 0.75 (i.e. about 15 analyses).
Oroopo Metabasalt
Collected by Laurie Hutton (GSQ) for SHRIMP zircon U-Pb geochronology to obtain an extrusive or magmatic age. FPXRF results indicate ca. 292 ppm Zr.

unnamed paragneiss
A sample of upper-amphibolite facies metamorphic rocks that outcrop in the remote northwestern corner of the Limbla map area was collected for U‑Pb SHRIMP geochronology. The outcrops are dominated by pelitic to psammitic stromatic metatexite. Veins of leucocratic melt permeate the more pelitic outcrops, crosscutting the stromatic layering. It is not certain whether these veins represent in-source melt or allochthonous melt injected into the metamorphic pile from a remote magmatic/anatectic source. The rocks appear to contain at least two fabrics, with an early (S1) sillimanite-bearing fabric isoclinally folded within an overprinting S2 fabric. Strain is variably expressed across the outcrops but grades up to ultra-mylonite in a few locations. The paragneiss is in contact with a porphyroclastic (protomylonitic) felsic gneiss (GA 2109985, NTGS IC10JAW1551), and field relationships are unclear as to whether the felsic gneiss is younger or older than the paragneiss. These metamorphic rocks are migmatitic and contain a high strain fabric. It is likely that they are older than nearby low-grade, relatively unstrained outcrops of Heavitree Quartzite of Neoproterozoic age (which may in fact be separated from these outcrops by an unconformity).
Kositcin, N., Carson, C.J., Hollis, J.A., Close, D.F., Whelan, J.A., Webb, G., Donnellan, N., 2013. Summary of results. Joint NTGS-GA geochronology project: Arunta Region, Davenport Province and Pine Creek Orogen July 2009-June 2011. Northern Territory Geological Survey Record, 2012-008, 49p.

Bluebush Metamorphics
The Bluebush Metamorphics are an association of upper amphibolite- to granulite facies metamorphic rocks within the Limbla map area. The rocks are dominated by net-textured and schollen (raft) diatexite of mostly pelitic composition. The outcrops frequently contain isolated rafts of calc-silicate composition intermingled with pelitic rafts. The diatexite does not contain a pervasive fabric; however, some of the rafts that make up the diatexite do preserve a relict gneissosity/foliation. The diatexite is locally intruded by a medium-grained biotite granite of unknown age.
Kositcin, N., Carson, C.J., Hollis, J.A., Close, D.F., Whelan, J.A., Webb, G., Donnellan, N., 2013. Summary of results. Joint NTGS-GA geochronology project: Arunta Region, Davenport Province and Pine Creek Orogen July 2009-June 2011. Northern Territory Geological Survey Record, 2012-008, 49p.

Chiripee Metamorphics
Granulite-grade gt-bt-sill-qtz-fspr gneiss. This unit comprises interbedded pelite-psammopelite and minor quartzite sequences with numerous gt-bearing qtz-fspr leucogranitic melt veins. It is interlayered with subordinate gt-bearing mafic granulite. There is no previous dating for this unit so we're interested in obtaining a detrital age spectrum from zircon cores and metamorphic age/s from rims to compare with the Bleechmore, Kanandra and Aileron granulites.

Skull Creek Formation
The Skull Creek Formation (Bullita Group) is a widely distributed clastic dolostone and siltstone unit defined by Sweet et al. (1974a, b) and best exposed in central and western VICTORIA RIVER DOWNS (Beier et al., 2002; Dunster and Ahmad, 2013a). The 160–230 m thick Skull Creek Formation comprises interbedded, fine- to medium-grained sandstone and dolarenite, biostromal dolostone and minor dolomitic siltstone, oolitic grainstone, dolorudite and chert (Dunster and Cutovinos, 2002; Beier et al., 2002), likely deposited mostly in high-energy marine conditions but with intermittent evaporitic depositional conditions that included subaerial exposure and minor open-water settings (Dunster and Ahmad, 2013a). The sample collected is a buff-coloured, medium- to fine-grained dolomitic sandstone/dolostone, comprised of well-sorted, well-rounded quartz and lithic grains, with minor feldspar and accessory opaques. The locally flat-lying bedding is massive, 10–50 cm thick, and defined by compositional variations in dolomitic and sandy components.

Youngest detrital component Age range 1345-1310 Ma.
Jasper Gorge Sandstone
Collected for detrital zircon U-Pb SHRIMP study

Angalarri Siltstone
The Angalarri Siltstone was sampled on the south side of a road cutting, immediately (~40 m) to the east of the East Baines River on the Victoria Highway. The road cutting locally exposes a 30 m high flat-lying sequence of purplish to red siltstone-mudstone, characterised by 2-10 mm thick discontinuous lenticular laminations. Interbedded within the laminated siltstone-mudstone unit are discontinuous lenticular cream quartz sandstones which display internal cross-bedding. The sampled unit is taken from one of the lenticular sandstones.

Willyama Supergroup
f-gr, qz-feld-bi gneiss
Jagodzinski, E.A., Fricke, C.E., 2010. Compilation of new SHRIMP U-Pb geochronological data for the Southern Curnamona Province, South Australia, 2010. Geological Survey of South Australia. Report Book, 2010/00014, 50p.

Chiripee Metamorphics
Unmelted amphibolite-facies psammitic gneiss: aim to get good max dep age (and hopefully c. 1590 Ma metamorphic age) to link Delny Gneiss (to north) with high-grade Chiripee (with younger apparent max dep age) to the south.

alt. maximum age of deposition: single analysis: 1570 +/- 22 Ma.
Kirkland, CL, Wingate, MTD, Spaggiari, CV and Tyler, IM 2009, 184336: sandstone, Pollock Hills; Geochronology Record 816: Geological Survey of Western Australia, 5p.

chloritic metasandstone and metasiltstone with sericitic alteration of feldspars. Collected from depth range: 1320'6'' to 1325'6''
Bellfield 1A
Fraser, G.L., Gilmore, P.J., Fitzherbert, J.A., Trigg, S.J., Campbell, L.M., Deyssing, L., Thomas, O.D., Burton, G.R., Greenfield, J.E., Blevin, P.L., Simpson, C.J., 2014. New SHRIMP U-Pb zircon ages from the Lachlan, southern Thomson and New England orogens, New South Wales: February 2011-June 2013. Geoscience Australia. Record, 2014/53, 217p.

This sample was collected near Florida homestead from outcrop of bioturbated quartzite containing worm burrow casts up to ~3 cm in diameter oriented with long axis normal to bedding. The presence of worm burrows suggests a shallow marine facies. The quartzite has a weak tectonic foliation that penetrates the worm burrow casts. There are currently no direct age constraints on this quartzite, although it has been interpreted to be part of the Late Silurian to Early Devonian Cobar Supergroup (Burton et al., 2012). The sample was analysed to collect a detrital zircon age spectrum for comparison with other sedimentary rocks of the region, particularly other quartzite units
Fraser, G.L., Gilmore, P.J., Fitzherbert, J.A., Trigg, S.J., Campbell, L.M., Deyssing, L., Thomas, O.D., Burton, G.R., Greenfield, J.E., Blevin, P.L., Simpson, C.J., 2014. New SHRIMP U-Pb zircon ages from the Lachlan, southern Thomson and New England orogens, New South Wales: February 2011-June 2013. Geoscience Australia. Record, 2014/53, 217p.

A more conservative estimate of the maximum depositional age is given by the weighted mean 207Pb*/206Pb* date of 1361 +/- 15 Ma (MSWD = 0.46) for the youngest four analyses in Group S.
Musgrave Region
Kirkland, CL, Wingate, MTD and Smithies, RH 2011, 187289: metasandstone, Prostanthera Hill; Geochronology Record 934: Geological Survey of Western Australia, 5p.

1106 +/- 39 Ma. 1sigma. N= single analysis
It is possible that all of the analyses are of unmodified detrital zircons, in which case the date of 1106 +/- 39 Ma (1 sigma) for the single analysis represents a maximum depositional age for the sedimentary precursor.
phyllite
Kirkland, CL, Wingate, MTD, Smithies RH and Howard, HM 2012, 190233: phyllite, Prostanthera Hill; Geochronology Record 1065: Geological Survey of Western Australia, 5p.

Budgery Sandstone Member
This sample was collected ~20 metres east of the Poplins trigonometric station at the top of one of two prominent steep conical hills known as The Brothers, on The Brothers property, approximately 50 km northeast of the town of Nyngan. The sample is a quartzite that represents partially recrystallised quartz-rich sandstone. The quartzite dips to the north-east and has a weak tectonic foliation, and contains numerous quartz veins along cleavage planes and occurring in en-echelon sets. No direct age constraints exist for the quartzite. It is included in the Budgery Sandstone Member of the Narrama Formation (Girilambone Group) and is, therefore, interpreted to be Early Ordovician in age. Other nearby quartzites (e.g. Trig Hill at Girilambone, north of Tritton) are likewise assigned to the Budgery Sandstone Member. These quartzites are interpreted to be lenses of quartz-rich sandstones within the turbidite sequence that have been more resistive to tectonic fabric development and subsequent weathering. No worm burrows or other fossils have been noted in the unit. The sample was analysed to produce a detrital zircon age spectrum, for comparison with zircon age spectra from other local sedimentary rocks, particularly other quartzite units in the region.

Coronga Peak Quartzite
This sample was collected from outcrop in a road cutting approximately 200 metres north of the summit of Coronga Peak. The sample is a massive quartzite with occasional laminations, and represents partially recrystallised quartz-rich sandstone. The quartzite at Coronga Peak is included in the Coronga Peak Quartzite, a unit that elsewhere demonstrably interfingers with the Drouin Conglomerate Member of the latest Silurian to Early Devonian Meryula Formation (Burton et al., 2012). There remains a degree of uncertainty, however, regarding the correlation between the quartzite at Coronga Peak, as sampled here, and this Siluro-Devonian unit elsewhere. This sample was collected and analysed to produce a detrital zircon age spectrum for comparison with zircon age spectra from other samples of Coronga Peak Quartzite of certain latest Silurian-Early Devonian age, and also with other quartzites in the region.

Saddle Creek Formation
The Saddle Creek Formation was sampled 5 m up sequence above the low angle unconformity with the underlying Angalarri Siltstone exposed on the road to Bullo River Station. The Saddle Creek Formation at this location is a medium-grained, well-sorted, quartzo-feldspathic sandstone with thin discontinuous layers of siltstone and layer parallel traces of opaque minerals (ilmenite and magnetite). The sandstone is medium-bedded (10-50 cm thick) and exhibits well-defined cross-bedding. Upper bedding surfaces show well-developed asymmetrical ripple sets, with wavelengths around 8-10 cm. Opaques are concentrated on ripple crests.

Bungitina metamorphics
Fine-grained garnet-sillimanite-biotite schistose gneiss, containing garnet porphyroclasts 0.3 cm across, migmatitic in places. Approximately 40 m true thickness; interlayered with kyanite-sillimanite-muscovite feldspar schistose gneiss. Kyanite grew during cooling: crystal growth is randomly oriented and cross cuts the sillimanite lineation. Meta-sedimentary units overlie fine-grained laminated quartzofeldspathic gneiss, and are intruded by coarse-grained intermediate to mafic igneous rocks. Although the contact was not observed here, the Bruna Granitic Gneiss sits structurally above these meta-sediments, which were previously mapped as part of Bungitina Metamorphics.

Key Creek Gneiss
biotite gneiss
Cross, A.J., Bultitude, R.J., Purdy, D.J., 2013. Summary of Results - Joint GSQ-GA Geochronology Project: Ayr, Bowen, Eulo, Mount Coolon, Proserpine and Warwick 1:250 000 sheet areas. Queensland Geological Record, 2012/19, 146p.

Pinkerton Sandstone
The Pinkerton Sandstone was sampled adjacent to the road to Bullo River Station, where it is comprised of fine-grained, well-sorted and well-rounded, ferruginous, feldspathic quartz sandstone. Bedding is massive and up to 1 m thick. In contrast to other units in the Auvergne Group, high-energy depositional features such as cross-bedding and ripple marks were observed at the sample location.

Spencer Sandstone
The sample was collected from exposure located along Bullo River Road. The Spencer Sandstone at this location is a thin- to medium-bedded (5-50 cm), fine-grained quartz sandstone characterised by moderately- to well-rounded quartz grains hosted within feldspathic matrix with rare large rounded grains of milky quartz. Iron staining on weathered surfaces is common, and bedding surfaces exhibit symmetrical ripples of 3–5 cm wavelength.

Provenance clusters spanning 1118-949 Ma; mixture modelled for maximum depositional age Youngest of two-component mixture modelling of 40 analyses; fraction = 0.66 (i.e. about 26 analyses), misfit = 0.983. Interpreted as best (conservative) maximum age for deposition of sedimentary precursor.
Black Point Sandstone Member
Collected for detrital zircon U-Pb SHRIMP study

Stubb Formation
Collected for detrital zircon U-Pb SHRIMP study, sampled unit is a 5-50cm wide lense of discontinous quartz sandstone within the Formation

Christie Gneiss
Sample R1562986 is a coarse grained, migmatised, quartz-plagioclase-microcline-cordierite-garnet gneiss from drillhole CD-1. At the hand specimen scale, layering is defined by alignment of biotite in melanocratic microlithons. Garnet porphyroblasts are coarse grained, up to 4 cm wide, and are typically elongate parallel to the main gneissic foliation. Quartz-feldspar is developed as leucocratic segregations adjacent many of the garnets, most likely indicating the garnet has grown via biotite breakdown reaction with the production of quartz-feldspar melt associated with this reaction. In thin section, quartz shows both polygonal-textured, coarse-grained forms, and also some zones of medium- to fine-grained recrystallisation. Quartz grain boundaries are typically lobate, indicative of high temperature recrystallisation. Feldspar occurs as both plagioclase and microcline, with the former the dominant species and the latter being perthitic in nature. Numerous examples of myrmekite are observed, also indicative of high temperature metamorphic conditions. Garnet occurs as coarse grained, anhedral porphyroblasts that show quartz +/- biotite inclusions and are typically rimmed by light brown biotite that is most likely a product of retrograde breakdown of garnet. Cordierite is also seen in thin section as coarse grains intergrown with quartz and in some instances with fine-grained biotite (+/- sillimanite?) rims. Opaque species, possibly ilmenite, are common as irregular shaped grains within the quartz-feldspar matrix. Zircon and monazite is abundant within the rock, with the former occurring as large euhedral to subhedral grains, often with prominent radiation damage halos within biotite.
Mt Christie CD-1
Jagodzinski, E.A., Reid, A.J., Fraser, G., 2009. Compilation of SHRIMP U-Pb geochronological data for the Mulgathing Complex, Gawler Craton, South Australia, 2007-09. Geological Survey of South Australia. Report Book, 2009/00016, 119p.; Reid, A.J., Jagodzinski, E.A., Fraser, G.L., Pawley, M.J., 2014. SHRIMP U-Pb zircon age constraints on the tectonics of the Neoarchean to early Paleoproterozoic transition within the Mulgathing Complex, Gawler Craton, South Australia. Precambrian Research, 250, 27-49.

This sample was collected from the Eastern Succession of the Mount Isa Inlier. SHRIMP U-Pb dating was undertaken to establish the maximum depositional age of the Answer Slate in the Kuridala region. The Answer Slate sample was sampled to directly compare with the maximum timing of deposition of the Toole Creek Volcanics (sandstone unit) in the Mount Isa Eastern Succession (Carson et al., 2009). The Answer Slate was thought to be a direct stratigraphic equivalent to the Toole Creek Formation as indicated by mapping completed by Parsons et al. (2008) as part of the GSQ Mt Isa Mapping Project. The sample collected for analysis is a black sandy siltstone collected by A. Lambeck (GA) and A. Parsons (GSQ).
Lambeck, A., 2011, Basin analysis and the geochemical signature of Paleoproterozoic sedimentary successions in northern Australia: Constraints on basin development in respect to mineralisation and paleoreconstruction models. PhD. thesis, 157p.

Fraction of 2-component group ~ 0.46 (i.e. about 8 analyses).
Hedleys Sandstone
Collected by Ian Sweet (on behalf of the GSQ)

Collected by Paul Blake (on behalf of GSQ)

Doherty Formation
Collected by Allan Parsons (GSQ)

Officer Region
Wingate, MTD, Lu, Y, Kirkland, CL, Haines, PW and Smithies, RH 2017, 189557: quartz sandstone, Mount Blyth; Geochronology Record 1371: Geological Survey of Western Australia, 6p.

Bleechmore Metamorphics
Coarse-grained, garnet-rich leucogneiss/migmatite that lies within mostly high-grade metasediments and mafic granulites of the Bleechmore Granulite. The sample was taken well within the unit to distinguish it from the previously dated sample of Maidment et al (2005) which was sampled just below the contact with the Mendip Metamorphics to the north of the main Bleechmore Granulite.

Granulite facies metasediment S of Andrew Young Hills Gabbro. Detrital zircon age spectrum consistent with Lander package. No clearly defined metamorphic age although some grains clearly affected by metamorphism.
A sample of migmatitic metapsammite was collected from an isolated hill 7 km south of the Andrew Young Hills and 3.5 km south of Black Hill Bore on southwestern MOUNT DOREEN. Overall, the hill comprises metapsammite interlayered with garnet-cordierite-sillimanite-biotite metapelitic rocks, and is surrounded by unconsolidated Quaternary sediments. Metapelite shows evidence for extensive partial melting (garnet-bearing leucosomes), leaving a cordierite-rich melanosome. Psammite is the dominant lithology and forms layers up to 2-3 m thick. The psammitic rocks are interpreted to have undergone biotite dehydration melting, forming cordierite-bearing leucosomes, and locally cordierite-garnet-bearing granite, possibly representing areas of pooled in situ melt. The hill also includes minor mafic granulite interpreted to be metamorphosed sill-like intrusive bodies (see MD03IRS29). The nearest outcrop of undeformed layered mafic igneous rock is of the ca 1635 Ma Andrew Young Igneous Complex, 4.5 km to the north. Lithologically, the dated sample is a granulite-facies, biotite-bearing metapsammite (quartz-rich metasedimentary rock) with K-feldspar-rich leucosome (locally garnet-bearing) enclosing aggregates of cordierite and quartz. Nearby, areas of coalesced leucosome form a diatexite containing rafts of metapsammite. The metapsammitic rock is variably foliated but not strongly deformed. The sample was selected for geochronology to determine a maximum age for deposition of the sedimentary protolith and the age of overprinting metamorphism.
Kositcin, N., Scrimgeour, I.R., 2020. Summary of results. Joint NTGS-GA geochronology project: central and western Aileron Province. Northern Territory Geological Survey Record, 2020-011, 32p.

Cahill Formation
Silicified tuff? hosted in upper Cahill Frm, Myra Falls Inlier, Arnhem Land
Carson, C.J., Hollis, J.A., Glass, L.M., Close, D.F., Whelan, J.A., Wygralak, A., 2011. Summary of results. Joint NTGS-GA geochronology project: East Arunta Region, Pine Creek Orogen and Murphy Inlier, July 2007-June 2009. Northern Territory Geological Survey Record, 2010-004, 84p.

Radium Creek Group
Quartzofeldspathic gneiss with feldspathic banding
Mount Painter Region

Birksgate Complex
This sample was selected for geochronology based on field relationships and petrographic interpretation that suggested this was a comparatively rare layered meta-sediment or volcaniclastic unit of the Birksgate Complex within the Tieyon 100k mapsheet. It is a uniformly fine- to medium-grained felsic rock dominated by pale grey felsic grains, and containing small uniformly distributed small black flakes (biotite) with weak preferred orientation defining a weak foliation. The sample responds weakly to the hand magnet, suggesting magnetite occurs pervasively in minor amount. The protolith for this sample is uncertain: it may have formed as a quartzo-feldspathic sediment, possibly of silty to sandy type, dominated by feldspar and quartz clastic grains, accompanied by trace clastic zircon and minor detrital clays. However, an alternative origin as a micro-granitoid remains possible. Recrystallisation occurred in response to regional metamorphism at elevated P-T conditions (amphibolite facies). This produced the medium-grained foliated granoblastic metamorphic assemblage of K-feldspar + quartz + plagioclase + minor biotite + opaques (including magnetite). Trace clastic zircon appears to have survived this event. At a later time, after uplift and erosion had elevated the rock body into a shallower crustal environment at greenschist facies P-T conditions, a very small amount of fluid circulated through the rock and produced minor new replacement sericite + biotite + chlorite. The presence of biotite in this assemblage suggests that the P-T conditions were in the middle greenschist facies (ie biotite grade). Note that this fine-grained biotite occurs in only trace amount, only in the sericitic clouds after plagioclase, and is much less abundant than the prograde biotite which formed larger well-shaped plates.
Eromanga Region
Jagodzinski, E.A., Dutch, R., 2013. SHRIMP U-Pb geochronology of the Tieyon (5645) 1:100 000 mapsheet. Geological Survey of South Australia. Report Book, 2013/00006, 222p.

Youngest detrital component. Age range 1568-1521 Ma.
purple, cross-bedded, coarse-grained sandstone with heavy mineral banding
Carpentaria Lowlands Region

Youngest detrital component. Age range 1845-1843 Ma.
Bernecker Creek Formation
This sample of the Bernecker Creek Formation was collected from along the Percy River ~2 km north of Ortona Station, in the Ortona Anticline of the Etheridge Province, Queensland. Here, the formation is characterised by packages of turbiditic sandstones which have very thick, massive-graded bases, with reworked upper layers. The sample was collected from the lower part of one of these packages, and is a grey, recrystallised, fine-grained sandstone with grits.
Neumann, N.L., Kositcin, N., 2011. New SHRIMP U-Pb zircon ages from North Queensland 2007-2010. Geoscience Australia. Record, 2011/38, 82p.

Youngest detrital component. Age range 1703-1686 Ma.
Daniel Creek Formation
The Daniel Creek Formation was sampled from along the Percy River ~4 km north of Ortona Station, in the Ortona Anticline of the Etheridge Province, Queensland. The sample (2007169003) was collected from the upper part of this formation, ~50 m below the contact with the overlying Dead Horse Metabasalt, and is a grey, fine-grained sandstone from a thick bed interbedded with thinly-bedded siltstones.
Neumann, N.L., Kositcin, N., 2011. New SHRIMP U-Pb zircon ages from North Queensland 2007-2010. Geoscience Australia. Record, 2011/38, 82p.

Barossa Complex
Sample R1009272 was collected from a large road cutting on Gorge Road in the River Torrens gorge, about 0.5 km W of Cudlee Creek, in the southern Houghton Inlier. This lithology is dominated by quartz, biotite, and a fine grained retrograde mineral that is most likely sericite. Coarse quartz and K-feldspar occurs in leucosomes throughout the rock, indicating partial melting has occurred. A subtle layering of quartz rich and quartz poor domains is present and may reflect a primary sedimentary feature. Retrogression of the primary mineral assemblage obscures many of the structures within this rock. Similar quartz-biotite-sericite gneisses occur throughout the southern Houghton Inlier, and structurally overlie (younging uncertain) calcsilicate and quartofeldspathic gneisses. Retrogression is much more extensive in the southern Houghton Inlier than the north, and minor faults and hydrous alteration around quartz veins is common, which often obscures lithological boundaries and sedimentary or metamorphic structures.
Sample R1009272 was collected from a large road cutting on Gorge Road in the River Torrens gorge, about 0.5 km W of Cudlee Creek, in the southern Houghton Inlier.
Jagodzinski, E.A., Szpunar, M., Meaney, K., Fraser, G., 2020. SHRIMP U-Pb dating of the Barossa Complex, South Australia: exploring tectonic links between the Gawler Craton and Curnamona Province. Geological Survey of South Australia. Report Book, 2020/00017, 111p.

Knapdale Quartzite
cross bedded pinkish quartzo-feldspathic sandstone, bedding on 5-15m scale, younging to west.
Carson, C.J., Hutton, L.J., Withnall, I.W., Perkins, W.G., 2009. Joint GSQ-GA NGA geochronology project Mount Isa region, 2007-2008. Queensland Geological Record, 2008/05, 88p.

Youngest detrital age component. Age range 1799-1688 Ma.
Quamby Conglomerate
collected at Quamby Gold Mine by Ian Withnall GSQ, for SHRIMP U-Pb zircon detrital study
Carson, C.J., Hutton, L.J., Withnall, I.W., Perkins, W.G., 2009. Joint GSQ-GA NGA geochronology project Mount Isa region, 2007-2008. Queensland Geological Record, 2008/05, 88p.

high grade metamorphic rocks 72653
raft of migmatic metasediment enclosed within 1640 Ma Warumpi granites in western Casey Inlier
Carson, C.J., Hollis, J.A., Glass, L.M., Close, D.F., Whelan, J.A., Wygralak, A., 2011. Summary of results. Joint NTGS-GA geochronology project: East Arunta Region, Pine Creek Orogen and Murphy Inlier, July 2007-June 2009. Northern Territory Geological Survey Record, 2010-004, 84p.

Entia Metamorphics
This is a migmatised garnet, silliminite, biotite schist, containing garnet porphyroclasts c. 2 cm across. The sample sent (IC07JAW232) is taken from the more quartz-rich component of the rock. In the field outcrop is intermittent and quite weathered covering an area of approximately 4 x 15 m, no direct contact with other lithologies was observed. This unit crops out in the western Entia Dome (Figure 1) as a metasedimentary package within the orthogneiss dominated Palaeoproterozoic Entia Gneiss Complex (EGC).

Restite fragment of psammite a few metres across within partially melting metasediments. Detrital spectrum (N=31) incomplete, but consistent with Lander Package.
A sample of metapsammite was collected from a low hill of granulite-facies migmatitic metasedimentary rocks on the eastern side of Cockatoo Creek, 10 km north-northwest of Mount Denison homestead in northwestern NAPPERBY. It is a cordierite-bearing, quartz-rich metasedimentary rock, with minor garnet. The metasedimentary rocks in the area include: (1) K-feldspar-sillimanite-cordierite schlieren and layers, which may be residue from melting of metapelite; (2) cordierite-quartz metapsammite, locally with garnet; and (3) cordierite-K-feldspar-quartz rock (with or without garnet), interpreted to be leucosome. These are spatially associated, and have a transitional relationship, with a cordierite-bearing S-type granite (NP03IRS011), which is considered to be an in situ melt. There are no exposed relationships with any other rock types, and no other rocks have been dated in the area. The sample was selected for geochronology to determine the age and provenance of the sedimentary precursor and the timing of granulite-facies metamorphism.
Kositcin, N., Scrimgeour, I.R., 2020. Summary of results. Joint NTGS-GA geochronology project: central and western Aileron Province. Northern Territory Geological Survey Record, 2020-011, 32p.

1380 +/- 10 Ma. MSWD = 1.8. N = 14: A more conservative estimate of the maximum depositional age
The date of 1298 +/- 26 Ma for the single analysis could alternatively reflect growth of new zircon, associated with melting during the 1345-1293 Ma Mount West Orogeny (Smithies et al., 2009).
metagranitic rock
Kirkland, CL, Wingate, MTD and Smithies, RH 2010, 187195: leucogranitic gneiss, Mount Scott; Geochronology Record 912: Geological Survey of Western Australia, 5p.

Barossa Complex
Sample R1588241 is a muscovite-biotite psammopelite with a strong gneissic fabric segregating quartzofeldspathic and micaceous minerals, forming 0.5-1.0 cm bands. Quartz-rich layers up to 5 cm thick, possibly a relict sedimentary feature, closely follow the gneissic layering. Thin leucosomes, several centimetres thick, parallel the gneissic foliation, and in some places are boudinaged. Larger pegmatites which cross the foliation are common in the surrounding area. The gneissosity of this rock has been multiply deformed. Larger wavelength folds commonly overprint older crenulations, indicating at least 2 folding events. The sampled psammopelite grades into a structurally overlying muscovite sillimanite schist to the south. The Warren Inlier lies within the sillimanite isograd of the Delamerian Orogen, and is positioned in an area of intense deformation as mapped by Mills (1973). In thin section, this sample displays a foliated granoblastic metamorphic texture with spaced phyllosilicate laminae. Abundant plagioclase forms anhedral unzoned grains from c. 0.2 mm to 2 mm with a range of grain shapes, suggesting that varied degrees of equilibration of primary plagioclase occurred during metamorphism. Muscovite forms colourless well-shaped plates c. 1.0-1.5 mm long, mostly concentrated in muscovite-rich laminae c. 0.5-2.0 mm thick which are spaced through the rock c. 1-2 mm apart. A strong foliation is defined by preferred orientation of the muscovite laminae and the muscovite flakes within the laminae. Biotite forms well-shaped plates similar in size to muscovite, mostly within the plagioclase-rich laminae. Minor chlorite forms pleochroic pale green flakes interleaved with biotite and muscovite. Minor quartz forms anhedral equant grains in equilibrium with adjacent plagioclase. Accessory minerals include rutile (as euhedral c. 100-200 um crystals), monazite (c. 100 um), and zircon as tiny rounded inclusions in biotite, enclosed in radiation haloes.
Sample R1588241 was collected from the South Para River in the Warren Inlier, about 3.5 km SE of Williamstown and 400 m downstream from the Warren Reservoir dam.
Jagodzinski, E.A., Szpunar, M., Meaney, K., Fraser, G., 2020. SHRIMP U-Pb dating of the Barossa Complex, South Australia: exploring tectonic links between the Gawler Craton and Curnamona Province. Geological Survey of South Australia. Report Book, 2020/00017, 111p.

Corbett Formation
The Corbett Formation was sampled from the Percy River, north-northwest of Ortona Station, in the Etheridge Province, Queensland. The sample was located a few hundred metres above the Dead Horse Metabasalt, from a package containing occasional thick beds associated with fine-grained, thinly-bedded, laminated siltstones. The sample was collected from one of the thick beds, and is a calcareous fine- to coarse-grained sandstone.

Townley Formation
The Townley Formation was collected southwest of Green Hills, in the Etheridge Province, Queensland. The sample (2007169005) was collected ~400 m below the contact with the overlying Heliman Formation from a thick bed within a siltstone-sandstone package, and is a fine-grained sandstone.

Heliman Formation
The sample from the Heliman Formation comes from Black Gin Creek, southwest of Green Hills, in the Etheridge Province, Queensland. A fine-grained sandstone with mud clasts (2007169006) was sampled from a thick bed approximately 50 m from the top of the (mapped) formation.

Langdon River Mudstone
The Langdon River Mudstone was collected from the Candlow Creek, ~2 km north of West Candlow Dam, in the Etheridge Province, Queensland. The sample (2007169007) comprises dark grey, fine-grained sandstone-mudstone, with planar laminations.

Malacura Sandstone
The Malacura Sandstone, part of the Langlovale Group, was sampled ~3.5 km southwest of Red Bull Bore, in the Etheridge Province, Queensland. The sample (2007169009) was collected ~500 m above the Langdon River Mudstone, from a ~2 m thick bed overlain by a reworked, thinly-bedded siltstone, and is a poorly sorted, gritty, coarse- to fine-grained sandstone.

Youngest detrital component. Weighted mean 207/206 RATIO before IMF correction = 0.10201 +/- 0.61% (95% conf). Divide by IMF factor (1.00354) to get the IMF-corrected 207/206 = 0.10165. Add the IMF uncertainty (0.17% at 95% confidence) in quadrature to the population mean [i.e. sqrt(0.61^2 + 0.17^2)] to get an expanded uncertainty of 0.63%. Converting the IMF-corrected 207/206 ratio and its expanded uncertainty into IMF-corrected 207/206 date and uncertainty = 1654 +/- 11 Ma (95% confidence).
possible felsic tuff with probable clastic detritus
Carson, C.J., Hutton, L.J., Withnall, I.W., Perkins, W.G., 2009. Joint GSQ-GA NGA geochronology project Mount Isa region, 2007-2008. Queensland Geological Record, 2008/05, 88p.

Collected for possible SHRIMP U-Pb zircon detrital analysis by Alexis Lambeck for PhD studies.

This sample was collected from the Lane Creek Formation which sits stratigraphically at the top of the Robertson River Subgroup in the Etheridge Province of the Georgetown Inlier. SHRIMP U-Pb dating was undertaken to establish the maximum depositional age of the Lane Creek Formation. The Lane Creek Formation is constrained by the 1655.9 +/- 2.2 Ma leucogabbro sill which intrudes this unit and is thought to approximate the depositional age of the Lane Creek Formation (Black et al., 1998). The sample was collected to test if the maximum timing of deposition of the Lane Creek Formation could potentially be correlated with the ca. 1658 Ma maximum depositional age of the Toole Creek Volcanics (sandstone unit) in the Mount Isa Eastern Succession (Carson et al., 2009). The sample collected for analysis is a poorly sorted fine-grained sandstone collected by Ian Withnall (GSQ).

Cahill Formation
Sample of psammitic Cahill Formation from hanging wall of Ranger mine, from drill core just SE of the pit (checked for radiation - background). Drill hole number GT07-PZ10. Sample interval 54.3-55.8 m. Drilled by ERA. Collected by J Hollis NTGS for detrital zircon U-Pb SHRIMP analysis.

This rock is a garnet-bearing felsic gneiss, consisting of polygonal-textured quartz-plagioclase-garnet-biotite, with a foliation defined by oriented biotite. Garnet contains needle-like inclusions of sillimanite forming inclusion trails, but not consistent in orientation throughout a thin-section. No sillimanite is observed outside garnet, in the matrix. Abundant zircon is visible in thin-section.
Fraser, G., Reid, A., Stern, R., 2012. Timing of deformation and exhumation across the Karari Shear Zone, north-western Gawler Craton, South Australia. Australian Journal of Earth Sciences, 59(4), 547-570.

Moonabie Formation
Fraser, G.L., Neumann, N.L., 2010. New SHRIMP U-Pb zircon ages from the Gawler Craton and Curnamona Province, South Australia, 2008-2010. Geoscience Australia. Record, 2010/16, 256p.; Szpunar, M., Fraser, G., 2010. Age of deposition and provenance of Palaeoproterozoic basins on north-eastern Eyre Peninsula. Geological Survey of South Australia. Report Book, 2010/00008, 26p.

metasedimentary raft contained within regional 1640 Ma Warumpi granites of the western Casey Inlier, east Arunta

Delmore Metamorphics
Cordierite-bearing metapsammite associated with cordierite-anthophyllite metapelite. Delmore Metm underlie (with structural discontinuity) the <1760 Ma Ledan Schist, and may have been affected by 1775 Ma Yambah event as well as 1730 Ma Strangways event. Targeting max dep age and rim ages.
Central Arunta

Sample R1588242 was collected from a large ridge of quartzite 4 km S of Normanville, in the southernmost exposure of the Myponga inlier, and about 1.5 km NW of sample R695754. The rock collected for analysis is a medium-grained (up to 1 mm), impure quartzite to psammite which varies from 95% to 60% quartz. K-feldspar and biotite make up the remainder, with biotite < 5% of the rock. A weak foliation is observed where biotite is present. The quartzite is one of two quartzite beds which bound a NW-SE trending unit of calc-silicate. The SE extent of this package is bounded by a shear zone displaying extensional kinematics (Morrissey et al. 2013), against which a migmatised garnet-sillimanite gneiss is juxtaposed. This area is intruded by coarse K-feldspar dominated granite and pegmatite intrusions similar to that of sample R695754. In thin section, this sample displays a foliated sutured granoblastic metamorphic texture. Quartz dominates, as large anhedral grains 1-4 mm in size. All are elongated in ductile manner in the trace of a metamorphic foliation, with aspect ratios c. 2:1. All grains display a significant degree of shadowy strain effects, and suturing around grain margins represents incipient recrystallisation of the larger grains. K-feldspar forms small anhedral grains, mostly concentrated around margins of the larger grains. All display the typical "tartan" twinning of microcline. Rare biotite forms small flakes c. 100-300 um long, concentrated in small wispy aggregates, with preferred orientation contributing to the metamorphic foliation. Small colourless muscovite/sericite flakes are intergrown with biotite. Opaque oxide minerals form small grains scattered through the rock. Zircon occurs as uncommon small rounded grains < 50 um in size.
Kanmantoo Region
Sample R1588242 was collected from a large ridge of quartzite 4 km S of Normanville, in the southernmost exposure of the Myponga inlier, and about 1.5 km NW of sample R695754.

This sample was collected from a small outcrop in a drainage depression near Downers Road, approximately 2 km east of the Oakbank township, on the eastern limit of the Oakbank inlier. It is a biotite-rich schist, with a fine-grained quartz and K-feldspar groundmass. Biotite defines a well-developed foliation which is deformed into open folds at the outcrop scale. The groundmass of quartz and feldspars is fine grained, averaging 0.5 mm grain sizes, with some coarse K-feldspar crystals up to 5 mm which are wrapped by the biotite foliation. This sample site is weathered and friable which casts some uncertainty on the identification of the fine grained groundmass minerals in hand specimen. The metasediments of the Oakbank Inlier are poorly exposed and have not been mapped or described in any detail previously. This inlier is intruded by the 856 +/- 20 Ma granite of Preiss et al. (2008), as well as a large pegmatite dykes of an unknown age. The Oakbank Inlier lies within the andalusite-staurolite isograd of the Delamerian Orogen which makes a potential Cambrian overprint or retrogression likely. In thin section, this sample displays a foliated granoblastic metamorphic texture with indistinct mineralogical banding. Plagioclase is abundant, forming equant anhedral grains mostly c. 0.4 mm in size, with sharp grain contacts and triple-grain junctions approaching 120 degrees. The resulting granoblastic mosaic suggests more-or-less equilibrium recrystallisation at elevated P-T conditions. Biotite is the other principal mineral. It forms well-shaped plates mostly c. 0.5-1.0 mm long. Their strong preferred orientation contributes to a strong penetrative foliation. Chlorite occurs in minor amount as small pleochroic green flakes, interleaved with some of the biotite plates. Opaques occur in minor amount as bladed crystals c. 0.2-0.5 mm long. A feldspathic siltstone is considered a likely protolith.
Sample R1588240 was collected from a small outcrop in a drainage depression near Downers Road, about 2 km E of Oakbank township, on the E limit of the Oakbank Inlier.

Christie Gneiss
R1565736 is from 97-98 m and is a medium to fine-grained quartz-biotite-plagioclase gneiss that includes a zone of interpreted syn-metamorphic partial melt. Quartz has been extensively dynamically recrystallised, being predominantly equant, polygonal grains. Undulose extinction and subgrain development are also common features within quartz grains. Biotite occurs as elongate light brown laths that define a foliation within the rock, that appear to post-date and earlier generation of darker brown, irregular shaped biotite. Radiation damage halos, most likely due to monazite inclusions, are common within biotite. Plagioclase is typically clouded, most likely due to fine grained sericitisation. Muscovite occurs as fine-grained laths interstitial to other phases and also as inclusions within the plagioclase. Subhedral to round zircon grains are common and opaque minerals are irregularly shaped and occur within quartz and plagioclase. The rock is probably best described as a microgneiss, due to the fine-grained nature of the minerals and the granoblastic texture. The precursor is likely to have been a psammitic metasediment.
Jagodzinski, E.A., Reid, A.J., Fraser, G., 2009. Compilation of SHRIMP U-Pb geochronological data for the Mulgathing Complex, Gawler Craton, South Australia, 2007-09. Geological Survey of South Australia. Report Book, 2009/00016, 119p.; Reid, A.J., Jagodzinski, E.A., Fraser, G.L., Pawley, M.J., 2014. SHRIMP U-Pb zircon age constraints on the tectonics of the Neoarchean to early Paleoproterozoic transition within the Mulgathing Complex, Gawler Craton, South Australia. Precambrian Research, 250, 27-49.

Population encompassing the youngest detrital zircon age component. Fraction of 2-component mixture model of 49 analyses = 0.10 (i.e. about 5 analyses).
Westmoreland Conglomerate
Possible peperite intruded into Westmorland Conglomerate, Sampled by LJH (GSQ)

Constance Sandstone
cliff forming sandstone in South Nicholson Group, sampled by I Sweet GSQ

Myra Falls Metamorphics
Small sample of cd-bearing leucosome from migmatitic pelitic gneiss from drill core, Caramal Inlier. Drill hole number TCSHD0030. Interval 278.95-279.13 and 229.8-230 m (two samples of cd-bearing leucosome combined from continuous section of metasediments). Drilled by Cameco. Sampled by J. Hollis NTGS for SHRIMP geochronology

Provenance clusters spanning 1800-1675 Ma; mixture modelled for maximum depositional age. Youngest of four-component mixture modelling of 21 analyses; fraction = 0.33 (i.e. about 7 analyses), misfit = 0.281. Interpreted as best (conservative) maximum age for deposition of sedimentary precursor.
collected for U-Pb SHRIMP geochron

Christie Gneiss
In outcrop, the lithologies are very clearly metasedimentary, occurring as metapsammitic to metapelitic units with garnet and biotite being common metamorphic minerals developed within the predominantly quartzofeldspathic lithologies. This mineral assemblage is typical for metapelitic Christie Gneiss and suggests Sleafordian metamorphism reached at least mid-amphibolite facies conditions in this area. In places primary sedimentary layering is well preserved, despite the inferred metamorphic overprint, with gradations between interlayered psammite and pelite observed within vertically dipping layers indicating the original sedimentary units varied from sandstone to muddy sandstone and probably represent shallow water clastic material. Sample R1562450 is a garnet-bearing quartz-feldspar gneiss. Quartz is the dominant mineral in the sample and occurs as large to medium grains, all with irregular, recrystallised boundaries along which subgrains are extensively developed. Plagioclase is subordinate and occurs are recrystallised perthitic grains to 2 mm in diameter. The quartz and plagioclase together show a strong preferred orientation and define a tectonic fabric. Plagioclase is weakly altered to sericite. Garnet, although not present within the thin section cut for this sample, is present in the hand sample as 2-4 cm diameter euhedral crystals randomly occurring throughout the rock. Field descriptions noted that the garnet was concentrated into layers parallel to the bulk lithological layering, suggesting the original variation in bulk composition has permitted the growth of garnet in more pelitic horizons. The sample is interpreted to be metasedimentary, with a quartz-rich, clastic source.
Jagodzinski, E.A., Reid, A.J., Fraser, G., 2009. Compilation of SHRIMP U-Pb geochronological data for the Mulgathing Complex, Gawler Craton, South Australia, 2007-09. Geological Survey of South Australia. Report Book, 2009/00016, 119p.; Reid, A.J., Jagodzinski, E.A., Fraser, G.L., Pawley, M.J., 2014. SHRIMP U-Pb zircon age constraints on the tectonics of the Neoarchean to early Paleoproterozoic transition within the Mulgathing Complex, Gawler Craton, South Australia. Precambrian Research, 250, 27-49.

Population encompassing youngest detrital age component. Fraction of 2-component mixture model of 64 analyses = 0.84 (i.e. about 54 analyses).
sampled by Allan Parsons (GSQ). Crappy sample.

Provenance clusters spanning 1882-1829 Ma; mixture modelled for maximum depositional age Youngest of three-component mixture modelling of 18 analyses; fraction = 0.25 (i.e. about 4-5 analyses), misfit = 0.933. Interpreted as best (conservative) maximum age for deposition of sedimentary precursor.
Depot Creek Sandstone
silty sandstone

Magmatic crystallisation of the ignimbrite bomb, but only a maximum age for deposition of the Gnalta group succession which hosts it
These zircons are relatively uniform in size, and average about 100 um in length. Most grains are approximately equant; only very rarely do aspect ratios exceed 2:1. Except for occasional embayments, probably caused by growth adjacent to a previously crystallised mineral, euhedral faces are almost universally preserved. Those faces include both simple and more complex prisms and pyramids, which are commonly developed on the same grain. The grains are essentially free of cracks and metamict zircon. Those features together with a low incidence of inclusions have provided essentially no impedance to the analysis of any grain. Oscillatory prismatic and sector zoning are about equally abundant, and commonly occur together. Only about 10% of the grains contain obviously discordant cores. Most of those cores have relatively restrained cathodoluminescence compared with that of the enclosing zircon. The abundant, high quality, zircon was ideal for establishing the crystallisation age of this ignimbrite bomb, which definies a maximum age for deposition of the host Gnalta Group. The 40 dated zircon grains yield an almost perfect isotopic grouping, with only one yielding an age that is statistically distinguishable from the others. With an age of 635 Ma, that grain is considerably older than the others, even though it is morphologically similar to them and is not particularly distinctive in its U and Th contents. The remaining 39 individual ages produce a weighted mean age of 510.5 +/- 2.9 Ma (MSWD = 1.07, probability of equivalence = 0.36). This should date the crystallisation of the ignimbrite bomb, and defines a maximum age for deposition of the Gnalta Group succession hosting the bomb.
Gnalta Group
This ignimbrite is a bomb/clast within the Gnalta Group, and defines a maximum age for the host unit. It was sampled in Cymbric Vale paddock, just North of Mutawintji National Park.
Wonominta Region
Cymbric Vale paddock, just N of Mutawintji National Park. Field site PG29 (also KM29A).
Geological Survey of New South Wales (GSNSW)
Black, L.P., 2007. SHRIMP U-Pb zircon ages obtained during 2006/07 for NSW Geological Survey projects. Geological Survey of New South Wales Report GS, 2007/298, 84p.

Sample R1588243 was collected from the NE Aldgate Inlier, adjacent to Greenhill Road about 5 km N of Bridgewater and is a psammite layer within a weathered sillimanite-bearing gneiss. The psammite is coarse grained (up to 2 mm) and dominated by quartz with minor weathered feldspar. The surrounding pelites clearly preserve a sillimanite- and mica-dominated assemblage. The mica species are difficult to identify due to weathering, however biotite is a likely constituent due to iron oxide staining, with finer-grained muscovite which may be related to retrogression. Leucosomes are uncommon but are observed on a 2-5 cm scale, and parallel a weak gneissosity defined by segregation of quartzofeldspathic and pelitic minerals. The basement rock at the sample location is directly overlain 50 m away by the basal units of the Neoproterozoic Aldgate Sandstone, which in this location feature a strong cleavage, which is also observed in the basement lithology. In thin section, sample R1588243 displays a partly preserved foliated and mineralogically banded texture, severely modified by subsequent pervasive alteration. Quartz occurs in significant amount as anhedral grains which range from c. 0.4 mm up to 4 mm. Smaller grains and larger grains tend to be concentrated in indistinct subparallel bands many millimetres thick, which defines mineralogical and grain size banding. White mica is abundant and occurs as aligned plates scattered throughout through the rock, and their preferred orientation defines a foliation subparallel to the mineralogical banding defined by quartz grains. However most white mica occurs as tiny anhedral grains with random orientation, forming a fine-grained pervasive mat throughout the rock. It is readily interpreted as a pervasive alteration phase. Opaque oxide minerals occur in significant amount as grains c. 0.4-1.0 mm in size. Tourmaline and zircon occur in trace amounts.
Sample R1588243 was collected from the NE Aldgate Inlier, adjacent to Greenhill Road about 5 km N of Bridgewater.

Lewis Range Sandstone
Birrindudu Region
Wingate, MTD, Bodorkos, S and Kirkland, CL 2008, 178851: sandstone, Bald Hill; Geochronology Record 743: Geological Survey of Western Australia, 5p.

Euhedral 'Igneous' grains spanning 1890-1795 Ma; mixture modelled for maximum depositional age. Centre of three-component mixture modelling of 27 analyses; fraction = 0.59 (i.e. about 16 analyses), misfit = 0.838. Interpreted as the best (conservative) maximum age for deposition of volcaniclastic precursor. IMF correction has been applied to this value, which is the preferred maximum depositional age.
Saint Ronans Metamorphics
Collected from map unit Psa (ARDMORE 100K), mapped as top of St Ronans Metamorphics complex

Granulite facies metasediments N of Mt Hay attributed as Lander Package. Detrital zircon age spectrum consistent with Lander Package. No obvious metamorphic rims but a few analysed areas have high-U, low-Th and track to undefined metamorphic age
A sample of fresh, quartz-rich metapsammitic rock containing garnet and biotite was collected from one of a group of low isolated hills located 30 km north-northwest of Mount Chapple in HERMANNSBURG. These rocks were included in the Narwietooma Metamorphic Complex (as unit Pnx) by Warren and Shaw (1995). The Narwietooma Metamorphic Complex of Warren and Shaw (1995) comprises the Mount Hay Granulite (dominated by mafic granulite), Mount Chapple Metamorphics (dominated by quartzofeldspathic gneiss and felsic granulite) and the Bunghara Metamorphics (dominated by mafic to intermediate granulite and lesser felsic migmatite). Unlike the remainder of the Narwietooma Metamorphic Complex, the rocks north-northwest of Mount Chapple are composed primarily of metasedimentary rocks and gneissic garnet-bearing granite, and therefore, may belong to the Lander Rock Formation. The metasedimentary rocks are dominated by garnet-cordierite-biotite-sillimanite migmatitic metapelites with garnet-bearing leucosomes, interlayered with metapsammite. The garnet-bearing porphyritic granite may be locally derived from partial melting of the metasedimentary rocks. Mafic granulite is mainly restricted to layers and pods within the metasedimentary rocks. This sample was selected for geochronology to help constrain the timing of deposition of the metasedimentary rocks in northern HERMANNSBURG, and determine potential correlations with the Lander Rock Formation (maximum depositional ages of ca 1860-1830 Ma) or Strangways Metamorphic Complex (ca 1820-1790 Ma; Scrimgeour 2013). The results would also assist in constraining the timing of high-grade metamorphism in this part of the Aileron Province, which is also poorly understood. There is no previous dating from this area.

Eyre Formation
weathered sandstone
Eromanga Region
Cross, A., Jaireth, S., Hore, S., Michaelsen, B.H., Schofield, A., 2010. SHRIMP U-Pb detrital zircon results, Lake Frome region, South Australia. Geoscience Australia. Record, 2010/46, 28p.

Kenella Gneiss
The sample of the Kenella Gneiss is from the central Mulgathing Complex, east of the township of Tarcoola. In this region the Kenella Gneiss varies from quartz-feldspar-biotite gneiss to quartz-feldspar gneiss, and occurs together with layer-parallel and discordant amphibolite units. The sample, R1562453, is a quartz-plagioclase gneiss that contains minor muscovite and around 5% opaque minerals. The opaque species, possibly ilmenite or magnetite, occurs as anhedral to subhedral grains that are interstitial to the quartz-feldspar matrix, but may also occur as inclusions within either of the silicate minerals. The relative abundance of the opaque mineral species suggest the sample may be derived from a siliceous volcanic or volcaniclastic protolith. The data from the Kenella Gneiss sample complements U-Pb zircon data from two samples reported by Swain et al. (2005).

Blue Range beds
Blue Range Beds, Ningana Homestead

Blue Range beds
Blue Range Beds, Mt Wedge

Radium Creek Group
Quartzofeldspathic gneiss with heavy mineral banding + ?magnetite
Mount Painter Region

Heavitree Formation
A sample of the Heavitree Quartzite was collected from southeastern Limbla for U-Pb SHRIMP geochronology. In Limbla, along the northeastern margin of the Amadeus Basin, the basal Neoproterozoic units, the Heavitree Quartzite and the Bitter Springs Formation are structurally interleaved with the Palaeoproterozoic Aileron Province of the Arunta Region. At this location the Heavitree Quartzite and the Bitter Springs Formation are isoclinally folded with intrusive rocks of the ca 1745 Ma Atneequa Suite and ca 1770 Ma Moonlight Gneiss occurring north and south (respectively), both of which are strongly foliated to locally mylonitic. Weakly preserved trough crossbedding in the Heavitree Quartzite indicates younging to the north on the northern limb of the fold. In hand specimen the quartzite is purple, relatively well-sorted, fine- to medium-grained and contains rare feldspar clasts. Locally the quartzite grades into granule to pebble conglomerate. At this location the quartzite is approximately 20 metres thick.
Kositcin, N., Whelan, J.A., Hallett, L., Beyer, E.E., 2014. Summary of results. Joint NTGS-GA geochronology project: Amadeus Basin, Arunta Region and Murphy Province July 2012-June 2013. Northern Territory Geological Survey Record, 2014-005, 24p.

rhyolite

A sample of strongly-foliated to mylonitic, hematite-bearing quartzite was collected from north central Limbla for U-Pb SHRIMP geochronology. At this location the Bitter Springs Formation and Heavitree Quartzite are structurally repeated in a series of thrust slices. North and South of the sample location, granulite-facies metasedimentary rocks of the Bluebush Metamorphics and intrusive rocks of the Atneequa Suite (Whelan et al 2011) unconformably underlie the quartzite. In Limbla, along the northeastern margin of the Amadeus Basin, the basal Neoproterozoic units, the Heavitree Quartzite and the Bitter Springs Formation, are structurally interleaved with the Palaeoproterozoic Aileron Province. No sedimentary structures were observed in outcrop at and along strike of the sample location. Given its location along strike from known exposures of Heavitree Quartzite, this sample was collected in order to try and constrain the nature of the protolith (deformed quartz vein or deformed Heavitree Quartzite?). At this location the quartzite contains abundant hematite, secondary copper minerals and box work after sulfide.
Kositcin, N., Whelan, J.A., Hallett, L., Beyer, E.E., 2014. Summary of results. Joint NTGS-GA geochronology project: Amadeus Basin, Arunta Region and Murphy Province July 2012-June 2013. Northern Territory Geological Survey Record, 2014-005, 24p.

Age range from 2647-1839 Ma, dominant peak at 1864 plus a scattering of individual ages
Murphy Metamorphics
The sample was collected from a section of the Murphy Metamorphics consisting predominantly of lithic greywacke interlayered with minor banded shale and quartzwacke. The sample is a poorly sorted, framework supported, fine- to medium-grained lithic greywacke dominated by sub-rounded to rather angular lithic fragments and lesser quartz grains. Other phases include former magnetite grains largely replaced by hematite and secondary iron oxides and accessory zircon and tourmaline grains. The matrix of this greywacke consists almost entirely of heavily limonite or hematite-altered clayey silt. The red colour reflects abundant hematite and iron hydroxides both in many of the lithic clasts and throughout the matrix. Metamorphic textures are generally absent and grade is interpreted to be sub-greenschist-facies. The Murphy Metamorphics are intruded by the1846 ± 6 Ma Nicholson Granite, which provides a minimum age for deposition of the sedimentary protoliths (Kositcin et al 2012).
Murphy Region
Kositcin, N., Whelan, J.A., Hallett, L., Beyer, E.E., 2014. Summary of results. Joint NTGS-GA geochronology project: Amadeus Basin, Arunta Region and Murphy Province July 2012-June 2013. Northern Territory Geological Survey Record, 2014-005, 24p.

Max depositional age. The youngest concordant analysis at 520 +/- 10 Ma (2sigma) can be considered as a maximum depositional age for this sample.
GSQ Mitchell 1 was drilled in 1972 by the Geological Survey of Queensland. It intersected high-grade metasedimentary rocks of the Nebine Ridge at 717.9 metres after penetrating sediments of the Surat Basin (Wallin, 1974). The metasedimentary units in Mitchell 1 consist of interbedded metasiltstone, metasandstone and quartzite. The basement lithologies are phyllitic to schistose and generally steeply dipping with s0 parallel to s1. Sample 2130080/TH438 from 767.49-770.53 metres consists of laminated quartz-mica phyllite. In thin section the rock is characterised by alternating quartz-rich and phyllosilicate-rich layers. Quartz is highly strained and recrystallised. Phyllosilicate-rich layers include varying proportions of quartz and exhibit anastomosing shear zones. Detrital grains include quartz, muscovite (identified as larger grains within phyllosilicate-rich layers) and rare feldspar.
GSQ Mitchell 1
Kositcin, N., Purdy, D.J., Brown, D.D., Bultitude, R.J., Carr, P., 2015. Summary of results. Joint GSQ-GA geochronology project: Thomson Orogen and Hodgkinson Province, 2012-2013. Queensland Geological Record, 2015/02, 68p.; Purdy, D.J., Cross, A.J., Brown, D.D., Carr, P.A., Armstrong, R.A., 2016. New constraints on the origin and evolution of the Thomson Orogen and links with central Australia from isotopic studies of detrital zircons. Gondwana Research, 39, 41-56.

DIO NARYILCO 1 was drilled by Delhi Petroleum Pty Ltd in 1963. It was drilled to a depth of 1477.4 m and recovered basement core from 1389.5 m (Brown et al., 2012). It is located approximately 25 km northwest of Naryilco in southwestern Queensland. The sample analysed is a grey fine- to medium-grained quartzite. Murray (1994) describes the unit sampled as a poorly sorted quartzose sandstone with an average grain size of about 0.1 mm. The dominant clastic components are quartz (up to 1 mm and comprising 40% of the rock), feldspar (mostly plagioclase and comprising ~20% of the rock) as well as 10% metasedimentary lithics, ~5% calcite, minor muscovite flakes and accessory apatite, tourmaline and zircon. Brown et al. (2012) assigned this unit to the Thomson Orogen, which at this location is overlain by sedimentary rocks of the Jurassic to Cretaceous Eromanga Basin. This sample was analysed to obtain provenance age information and a maximum age of deposition.
Naryilco 1
Cross, A.J., Purdy, D.J., Bultitude, R.J., Brown, D.D., Carr, P.A., 2016. Summary of results - Joint GSQ-GA geochronology project: Thomson Orogen, New England Orogen, Mossman Orogen and Mount Isa region, 2011-2013. Queensland Geological Record, 2016/03, 142p.; Purdy, D.J., Cross, A.J., Brown, D.D., Carr, P.A., Armstrong, R.A., 2016. New constraints on the origin and evolution of the Thomson Orogen and links with central Australia from isotopic studies of detrital zircons. Gondwana Research, 39, 41-56.

Cook Gap Schist
metasedimentary non-carbonate chemical or biochemical rock
Sample R2023011 (depth 54.1-54.3 m) is a siliceous iron formation from within the Wilgerup Deposit, from a unit considered to be either Upper or Lower Middleback Jaspilite. The ages of zircon in this sample will enable us to place the Wilgerup schist into the context of the recent work that has subdivided the Hutchison Group into three occurrences of dolomite-BIF-schist successions; differing in their ages and schist protolith provenances (Szpunar et al. 2011a; Szpunar et al. 2011b). This sample is a finely laminated hematite-dominated iron formation. Layering is defined by greater or lesser abundances of hematite, which occurs as small, <50-micron angular crystals. The hematite can be seen to be replacing magnetite as in many instances, the core of the hematite grains is composed of magnetite. Hematite also occurs in the matrix as red masses, intergrown with the very fine grained quartz-dominated matrix. Minor chlorite occurs along small fractures. Some small, <100-micron zircons are observed within the quartz-rich matrix. Sample R2023012 (depth 57.2-57.5 m) is more siliceous metasediment than sample R2023011 within the same iron formation. Both samples are from close intervals of the same drillhole, and their SHRIMP zircon results have been combined for the purpose of interpretation.
Jagodzinski, E.A., Farrell, F., Reid, A., 2017. Project PGC03-06: Centrex Metals Ltd: Maximum depositional age of the Wilgerup Schist, Eyre Peninsula. IN Jagodzinski, E.A. and Reid, A.J. (eds) PACE Geochronology: Results of collaborative geochronology projects 2013-15. Geological Survey of South Australia. Report Book, 2015/00003, 79-87.

Price Metasediments
The so-called Price Metasediments occupy a narrow, c. 3 km wide magnetic high zone that trends to the north along the western edge of lower Eyre Peninsula. The magnetic high within this zone is mostly the result of iron-rich rocks that occur within a predominantly clastic sedimentary sequence. The Price Metasediments are phyllitic a result of low grade deformation. The metasedimentary rocks show a pronounced spaced cleavage and a well defined intersection lineation between the schistosity and the bedding surface. The Price Metasediments are described as having small garnets in samples from exploration drilling on Coffin Bay Peninsula (Oliver and Fanning, 1997), however, the sample taken for geochronology has no garnet visible at the hand specimen scale. Compositional layering expressed as variations in quartz content appear to define the original sedimentary layering, although it is possible that this could be a transposed foliation. The Price Metasediments have been quoted as having a depositional age of 1766 +/- 14 Ma (Oliver and Fanning, 1997). However, this age is derived from unpublished data, as the original reference contains no data tables. In thin section, compositional banding is present, defined by greater or lesser abundances of quartz versus fine-grained clays, which likely derive from micas present originally within the rock. The darker bands are dominated by these fine-grained clays plus quartz. The rock has a spaced cleavage developed due to the alignment of mica and the partial reorientation of the compositional layering. Coarse- to medium grained opaque phase is abundant throughout the rock. This is likely a combination of both pyrite and magnetite, since the hand specimen responds to a hand magnet indicating magnetite is present within the rock. The thin section is however cover-slipped and reflected light microscopy is not possible to confirm this.
Jagodzinski, E.A., Reid, A.J., Hand, M., 2012. SHRIMP U-Pb geochronology of Archaean to Palaeoproterozoic rocks from the southern Eyre Peninsula. Geological Survey of South Australia. Report Book, 2012/00015, 78p.

Geochronology for Geol Survey of Queensland
Kajabbi Formation
Kajabbi Formation southeast of Kajabbi, and is a very thick-bedded, laminated and rarely cross-bedded, medium- to coarse-grained feldspathic sandstone.

Geochronology for Geol Survey of Queensland
Kajabbi Formation
Base of the Kajabbi Formation southwest of the Mt Roseby Homestead, and is a medium- to thick-bedded, fine- to very coarse-grained, locally pebbly quartzose sandstone.

arkose
Canary 1

basaltic andesite

pelitic gneiss

Geochronology for Geol Survey of Queensland
arkose
Canary 1

Sandstone which occurs between tillitic intervals.
Marduroo 1

GSQ Julia Creek 1

Max depositional age. Age range 516-506 Ma.
Charters Towers Metamorphics
The Charters Towers Metamorphics are a belt of low-pressure-high temperature metamorphic rocks which crop out in a discontinuous, broadly east-west belt over 150 km long. The rocks consist of quartz-biotite-plagioclase schist, cordierite-quartz-biotite-schist, quartzite, and minor calc-silicate rocks. Peak amphibolite-grade metamorphic conditions are indicated by the presence of sillimanite and migmatite. The absence of garnet has been used to infer low pressure relative to temperature. The unit shows a well-developed foliation, which trends north-west and dips steeply to the north-east, and includes localised isoclinal folding. The age of the unit is constrained by the intrusion of the Bucklands Hill Diorite which was dated at 508 +/- 7 Ma (Hutton and others, 1997). The sample site is a railway cutting to the east of town near the intrusive contact with the Columbia Creek Complex. The sample (2128016/DPTH009) is a dark grey, fine-grained plagioclase-muscovite-biotite-quartz-?cordierite schist with minor banding, which resembles cross bedding. It contains abundant sericitically altered grains, some of which have hexagonal habits (cordierite?).
Charters Towers Region
Cross, A.J., Dunkley, D.J., Bultitude, R.J., Brown, D.D., Purdy, D.J., Withnall, I.W., von Gnielinski, F.E., Blake, P.R., 2015. Summary of results Joint GSQ-GA geochronology project: Thomson Orogen, New England Orogen and Mount Isa region, 2010-2012. Queensland Geological Record, 2015/01, 138p.; Purdy, D.J., Cross, A.J., Brown, D.D., Carr, P.A., Armstrong, R.A., 2016. New constraints on the origin and evolution of the Thomson Orogen and links with central Australia from isotopic studies of detrital zircons. Gondwana Research, 39, 41-56.

The Sequoia Prospect is a magnetite iron ore prospect located in the central-eastern Christie Domain. Drilling by the South Australian Department of Mines and Energy in 1997 defined an inferred resource of 22 Mt grading 28.4% Fe, comprising several steeply dipping, laterally discontinuous 2–50 m wide layers of quartz-actinolite-magnetite, actinolite-magnetite, and biotite-quartz-magnetite gneiss (Davies, 2000). The magnetite gneiss is structurally concordant with a banded quartz-magnetite-diopside-hypersthene-amphibole gneiss with-interlayered quartz–microcline–plagioclase gneiss and plagioclase-rich granitoid. This sample is dominated by K-feldspar, which is weakly sericitised and intergrown with plagioclase in a perthitic texture. Minor biotite is light brown. The texture of the rock is granoblastic, however, there is a weak foliation defined by the alignment of recrystallised quartz grains and the minor biotite crystal aggregates. The rock is extensively recrystallised and variably sericite altered.
SE DD 1
Reid, A., Jagodzinski, E.A., 2017. Project PGC03-11: Geochronology of granite and granite gneiss from Apollo Minerals tenements, Commonwealth Hill. IN Jagodzinski, E.A. and Reid, A.J. (eds) PACE Geochronology: Results of collaborative geochronology projects 2013-15. Geological Survey of South Australia. Report Book, 2015/00003, 141-167.

psammitic granofels/hornfels

DDH T17 was drilled in 1981 by Pressuag Australia, who were targeting linear magnetic anomalies. The unit sampled is a mauve to grey, cleaved metamudstone from the depth interval 163.28-166.9 m. In thin section the sample has diffuse sedimentary lamination defined by minor darker layers and trails of quartz disrupted by folding and an axial planar cleavage. No rocks are exposed locally, and lithological information is known only from drilling. DDH T17 targeted a magnetic trend interpreted as a southerly extension of the Warraweena Volcanics (Hegarty, 2010), which are calc-alkaline basaltic andesites (Burton et al., 2008) intersected by drilling about 20 km to the NE. DDH T17 intersected: (1) hematitic altered metamudstones, metasiltstones and phyllitic units interpreted as Girilambone Group (Byrnes 1993). At ~185.3 m an overall sandier sequence was noted with massive quartzite, black shale, and metamudstone with two cleavages at low angles; (2) felsic volcanic tuffs (Vickery, 2008), interpreted by Simpson (2013) as coherent, weakly porphyritic rhyolitic sills with quartz phenocrysts and a sericite altered quartz-feldspar groundmass. These sills contain cassiterite, and may relate to the nearby Mooculta Granite. The interpreted gravity low and contact aureole associated with this granite extends to just south of T17 (Hegarty 2010); and (3) mafic dykes with alkali geochemistry (Vickery, 2008), which intrude the metasedimentary units with disconformable contacts (e.g. ~194 m). They have been described as olivine- and pyroxene-phyric basalts by Simpson (2013). This package of rocks is interpreted to be within the southern Thomson Orogen (Glen et al., 2010; 2013). The sample was collected to obtain a detrital zircon age spectrum for comparison with other local and regional sedimentary rocks. A maximum depositional age from this sample will also provide a maximum age constraint on the intruding felsic sill and mafic dykes.

Max depositional age. Age range 389-378 Ma.
Theresa Creek Volcanics
The Theresa Creek Volcanics crop out in the Theresa Creek Dam area, south of Clermont. They dominantly comprise mafic volcanics (basalt to andesite), lesser breccia, conglomerate, rare tuff and volcaniclastic arenite (Withnall and others, 1995). No previous geochronological studies have been carried out on this unit, and geological relationships loosely constrain its deposition to between ~380 Ma and ~360 Ma (Withnall and others, 1995). The Theresa Creek Volcanics unconformably overlie the Anakie Metamorphic Group which was deformed and metamorphosed at ~510 Ma. The volcanic rocks are intruded and contact-metamorphosed by the Iron Hut Quartz Monzonite, to which Withnall and others (1995) assigned a Devonian age, based on similarities with the Stevenson Quartz Monzodiorite for which existing K-Ar and Rb-Sr biotite ages span the range ~382 Ma to ~379 Ma. The Theresa Creek Volcanics are unconformably overlain by felsic volcanic rocks and sedimentary rocks correlated with the Silver Hills Volcanics, for which Cross and others (2009) determined a SHRIMP U-Pb zircon age of 362.8 +/- 2.7 Ma in the Mount Coolon region. Anderson and others (2004) determined a paleomagnetic paleopole position that is inconsistent with the suggested Middle Devonian age, and more indicative of an Ordovician age. On that basis, it was considered that mafic volcanics in the Fork Lagoons beds could be correlative with these rocks. An Ordovician age might also suggest that the volcanics were correlatives of the Macquarie Arc in NSW that host significant gold-copper mineralisation at Cadia-Ridgeway. The sample was therefore collected for SHRIMP U-Pb zircon analysis to resolve the age. The sample (2128094/DPTH049) is a dacitic ignimbrite, crystal-rich and strongly welded, comprising fine feldspar fragments (<1 mm) in a dark blue-grey, formerly glassy siliceous groundmass. Small pumice fragments are observed on some surfaces and the ignimbrite also contains small, dark coloured lithic fragments.
Anakie Region
Cross, A.J., Dunkley, D.J., Bultitude, R.J., Brown, D.D., Purdy, D.J., Withnall, I.W., von Gnielinski, F.E., Blake, P.R., 2015. Summary of results Joint GSQ-GA geochronology project: Thomson Orogen, New England Orogen and Mount Isa region, 2010-2012. Queensland Geological Record, 2015/01, 138p.

This sample was collected ~50 m south of a small gully near the eastern flank of Mount Oxley. The sample comes from a ~5 m long exposure of a ~30 cm thick, quartz-rich, coarse-grained, moderately east-dipping metasandstone bed. The sandstone is heavily quartz-veined and iron-stained along fractures and contains small vughs. The age of the metasandstone is unknown. The sandstone is correlated with a turbidite sequence, the Booda Formation, exposed around the base of Mount Oxley, including sample GSNSW OXCOPJG0014, and is unconformably overlain by a sequence interpreted to be an outlier of middle- to late-Devonian Mulga Downs Group. The Booda Formation is interpreted to predate the Benambran Orogeny based on the presence of tectonic fabrics, and is assigned an Ordovician-age based on tentative correlation with the Girilambone or Bendoc groups.

Max depositional age. Age range 406-388 Ma.
DIO TARTULLA 1 was drilled by Delhi Petroleum Pty Ltd in 1981 and reached a depth of 2591.7 m before termination. It is located approximately 5 km northeast of Woomanooka Station, in southwestern Queensland. The sample submitted for analysis is a light to medium grey metasiltstone to fine-grained metasandstone locally with dark coloured shale laminations and scattered, round siliceous pebbles. Murray (1994) also noted the presence of pyrite nodules up to 1 cm across. Murray (1994) and Brown et al. (2012) classified the basement metasedimentary rocks from DIO TARTULLA 1 as a part of the Thomson Orogen. This sample was analysed to obtain provenance age information and a maximum age of deposition in order to better understand its stratigraphic context.
TARTULLA 1
Cross, A.J., Purdy, D.J., Bultitude, R.J., Brown, D.D., Carr, P.A., 2016. Summary of results - Joint GSQ-GA geochronology project: Thomson Orogen, New England Orogen, Mossman Orogen and Mount Isa region, 2011-2013. Queensland Geological Record, 2016/03, 142p.

Timbury Hills Formation
HPP BENDIBOI 1 was drilled to a depth of 1668.5 m by Hematite Petroleum Pty Ltd in 1979. It is located in the southern part of the Roma Shelf approximately 5 km south-east of the junction of Noona and Bendiboi Creeks and about 75 km north-east of St George, Queensland. Murray (1994) described basement core between 1656.59-1661.86 m as coarse-grained garnet-muscovite-biotite schist or gneiss, which he considered a high grade (probable amphibolite facies) part of the Timbury Hills Formation, a unit typified by lower greenschist facies metamorphism in the northern part of the Roma Shelf. The age of the Timbury Hills Formation is loosely constrained by plant fossils from drill hole AAO PICKANJINNIE 2 (which indicate a Devonian age) and intrusions of Devonian to Carboniferous granites that provide a minimum age (Murray 1994). Additionally, a SHRIMP U-Pb detrital zircon maximum deposition age of 419.8 +/- 4.1 Ma was interpreted for a sandstone from the Timbury Hills Formation, recovered from drill hole AAO TIMBURY HILLS 2 (2130082/TH679; Kositcin et al. 2015a). The sample submitted for geochronology is a garnet-muscovite-biotite paragneiss and comprised 59.33 cm of half core. It was analysed to determine the age of metamorphism and the maximum deposition age of the protolith.
BENDIBOI 1
Cross, A.J., Purdy, D.J., Bultitude, R.J., Brown, D.D., Carr, P.A., 2016. Summary of results - Joint GSQ-GA geochronology project: Thomson Orogen, New England Orogen, Mossman Orogen and Mount Isa region, 2011-2013. Queensland Geological Record, 2016/03, 142p.

Cleve Group
Sample R1832106 is a quartz-feldspar-sillimanite gneiss that represents the principal host lithology within the Mawson Prospect drillholes. The gneiss is leucocratic, and has undergone migmatisation as evident by the differentiated metamorphic layering defined by leucosomes of quartz and feldspar and melanosomes that are rich in biotite. The sample is dominated by a granoblastic quartz-feldspar texture which is dissected by through-going zones of sillimanite (fibrolite) associated with biotite. Quartz shows significant subgrain development, including lobate grain boundaries indicative of high temperature metamorphism, which is likewise indicated by the presence of sillimanite as an aluminosilicate phase. K-feldspar is present as coarse crystals with generally subhedral habit, which preserve cross-hatch twinning. Plagioclase is subordinate, ~20%, although an important component to the gneiss. This gneissic rock has undergone significant secondary alteration. Feldspars, both plagioclase and orthoclase, are clouded by a sericite +/- hematite alteration. Biotite crystals are strongly altered and in places are replaced by chlorite-sericite-leucoxene aggregates.
Reid, A., Jagodzinski, E.A., Greene, D., Maas, R., Selby, D., Gregory, C., 2012. Project PGC02-04 and PGC02-05: Geochronology from the Mawson prospect, Weednana Skarn magnetite deposit and the Telephone Dam prospect, South Australia. IN Reid, A. and Jagodzinski, L. (eds) PACE Geochronology: Results of collaborative geochronology projects 2011-12. Geological Survey of South Australia. Report Book, 2012/00012, 101-135.

Provenance clusters spanning 1621-1533 Ma; mixture modelled for maximum depositional age. Youngest of two-component mixture modelling of 26 analyses; fraction = 0.62 (i.e. about 16 analyses), misfit = 0.910. Interpreted as best (conservative) maximum age for deposition of sedimentary precursor.
Birksgate Complex
This sample occurs in close proximity to other potentially metasedimentary rocks (represented by SampleIDs R1842269 and R1039159). The sample is a finely layered tight to isoclinally folded quartzofeldspathic migmatitic gneiss with minor compositional variation from garnet absent, to garnet present, going west to east across the outcrop. This sample is also adjacent to a 4m wide microgranite dyke which crosscuts the foliation and was also sampled (SampleID R1842263) for geochronology. It is a medium-grained crystalline rock in which banding on the centimetre scale is well-defined by bands rich in dark ferromagnesian grains (biotite) and bands rich in felsic grains (white feldspar, translucent grey quartz). Preferred orientation of the biotite flakes defines foliation subparallel to mineralogical banding. This sample is considered to have formed as a layered sediment, in which layering was defined by varied abundances of clastic grains (plagioclase, quartz, K-feldspar, trace zircon), detrital clays, and calc-silicate chemical sedimentary components. The inferred presence of calc-silicate chemical sedimentary components implies a marine environment of deposition. Recrystallisation in response to regional metamorphism in the amphibolite facies generated new granoblastic assemblages of plagioclase, quartz, K-feldspar, biotite, hornblende, clinopyroxene (diopside), minor opaques and trace apatite. Particular sedimentary protoliths produced different mineral assemblages: i) Mixed clastic-pelitic-calc-silicate layers produced plagioclase + quartz + biotite + minor hornblende + clinopyroxene + opaques (including magnetite) + apatite. These are the darker band and paler grey band in the hand sample. ii) Some felsic clastic layers produced K-feldspar + quartz + plagioclase + minor biotite. This the pale cream band in the hand sample.
Eromanga Region
Primary Industries and Resources South Australia (PIRSA)
Jagodzinski, E.A., Dutch, R., 2013. SHRIMP U-Pb geochronology of the Tieyon (5645) 1:100 000 mapsheet. Geological Survey of South Australia. Report Book, 2013/00006, 222p.

GSQ Dobbyn 2

siltstone
GSQ Julia Creek 1

Hodgkinson Formation
This outcrop forms part of a belt of rocks (informal subunit Dhr9 of the Hodgkinson Formation) up to 20 km wide, characterised by mottled pale purplish pink tones on ternary radiometric images in contrast to the overall darker tones shown by adjacent rock packages in the Hodgkinson Formation. This outcrop is about 31 km NNW of 2153450/BB4542 (this record) and was selected for dating to compare the detrital zircon age spectrum with spectra yielded by sandstones elsewhere the Hodgkinson Formation, most with different radiometric signatures. The sample was collected from an outcrop in Hells Gate Creek downstream of the bridge on the main Lakeland Downs-Laura road. Outcrops in this area comprise brown, thin to medium-bedded (5-50 cm thick), medium to coarse-grained sandstone (0.1-2 mm, average 0.7 mm) containing relatively coarse detrital muscovite flakes and rip-up mudstone clasts. The sandstone is poorly sorted, with 20% matrix. Most grains are angular to subangular, with a few subrounded-rounded fragments. Quartz (65%), mainly as monocrystalline grains, is the dominant framework mineral. Sparse polycrystalline quartz grains up to 2 mm are also present. The sandstone also contains minor, little-altered plagioclase, detrital muscovite and biotite flakes (up to 0.6 mm long; muscovite > biotite), K-feldspar, traces of calcite, and accessory zircon and tourmaline. The detrital mica flakes are characterised by undulose extinction and curved or bent cleavage planes. Sericite/muscovite and fine biotite are common in the matrix. Sparse (5%) clasts of mudstone (angular; up to 3 mm), siltstone, chert, and quartzite (rounded; up to 2 mm), and subangular-rounded fragments consisting of sericite/muscovite were also detected in thin section. This sample is finer grained, much more matrix rich, poorer in detrital muscovite, K-feldspar and lithic fragments (which are also smaller), and richer in detrital biotite than sample 2153450/BB4542. Bedding is also much better developed.
Cairns Region
Cross, A.J., Purdy, D.J., Bultitude, R.J., Brown, D.D., Carr, P.A., 2016. Summary of results - Joint GSQ-GA geochronology project: Thomson Orogen, New England Orogen, Mossman Orogen and Mount Isa region, 2011-2013. Queensland Geological Record, 2016/03, 142p.

Max depositional age. The weighted mean 206Pb/238U age of 419.8 +/- 4.1 Ma recorded by the youngest group of 16 zircons (age range 437-412 Ma) is interpreted to record a maximum depositional age of this sandstone of the Timbury Hills formation.
AAO Timbury Hills 2 was drilled by Associated Australian Petroleum in 1960 in the Roma Shelf area to a depth of 1341 metres. Basement (beneath the Surat and Bowen Basins) comprises greenschist facies metasedimentary rocks intersected at 1171 metres (Derrington, 1960). Sixteen metres of core were collected from a variety of intervals. Core interval 8 was chosen for geochronology. Despite variation in metamorphic grade, all metasedimentary basement rocks in the Roma Shelf area are informally referred to as the Timbury Hills formation (Murray, 1994). The presence of plant fossils in a single drill core (AAO Pickanjinnie 2) suggests a Devonian age, but it is unclear whether the formation comprises sequences of different age (Murray, 1994). We sampled the Timbury Hills formation from AAO Timbury Hills 2 to provide the first U-Pb SHRIMP geochronology constraints on the unit. The sample selected is a fine-grained, dark grey, quartz sandstone and represents a relatively low grade variety of the Timbury Hills formation.
TIMBURY HILLS 2
Kositcin, N., Purdy, D.J., Brown, D.D., Bultitude, R.J., Carr, P., 2015. Summary of results. Joint GSQ-GA geochronology project: Thomson Orogen and Hodgkinson Province, 2012-2013. Queensland Geological Record, 2015/02, 68p.

AAO BERYL 1 was drilled to a depth of 1266.1 m by Associated Australian Oilfields NL in 1964. It is located approximately 65 km northwest of Muttaburra, central Queensland and 5 km southwest of Beryl Farm. The sample submitted for SHRIMP U-Pb detrital zircon geochronology is a fine-grained, grey quartz sandstone (Murray, 1994). Basement rocks in AAO BERYL 1 were assigned by Brown et al. (2012) as belonging to the Thomson Orogen package and/or the suggested time equivalent, Warburton Basin. These rocks are overlain by sedimentary rocks of the mid Carboniferous-Middle Triassic Galilee Basin, and Jurassic to Cretaceous Eromanga Basin. The aim of this study was to obtain provenance age information and a maximum age of deposition for this sample.
Beryl 1
Cross, A.J., Purdy, D.J., Bultitude, R.J., Brown, D.D., Carr, P.A., 2016. Summary of results - Joint GSQ-GA geochronology project: Thomson Orogen, New England Orogen, Mossman Orogen and Mount Isa region, 2011-2013. Queensland Geological Record, 2016/03, 142p.; Purdy, D.J., Cross, A.J., Brown, D.D., Carr, P.A., Armstrong, R.A., 2016. New constraints on the origin and evolution of the Thomson Orogen and links with central Australia from isotopic studies of detrital zircons. Gondwana Research, 39, 41-56.

The sample was collected from a low rise on the southern side of the Booroomugga Road, about 1.9 km east of the Johnsons Road intersection, approximately 50 km northwest of Nyngan. The sample is a very hard, dark grey, medium grained, poorly sorted, feldspathic sandstone. Weathered surfaces exhibit a stripy cleavage. The sample was collected to obtain a detrital zircon age spectrum for comparison with other local and regional sedimentary rocks. Turbidites of the Narrama Formation are generally quartz-mica rich rather than feldspathic. The Narrama Formation includes mafic rocks of both ocean island basalt (OIB) and mid-ocean ridge basalt (MORB) affinity so a proximal zircon source and the high feldspar content may indicate active volcanism nearby. The Narrama Formation is late Lancefieldian to Chewtonian in age based on conodont biozonation, although the ages of the top and base of the unit are unconstrained (Burton et al., 2012).

Youngest detrital component, Age range 687-663 Ma.
Waldo Pedlar Member
The Pertatataka Formation consists mainly of grey-green and purple-brown laminated micaceous siltstone and shale with thin interbeds of sandstone and limestone. Two members are restricted to the northeast of the basin: the lower Waldo Pedlar Member and the upper Cyclops Member (Wells et al 1967). The Waldo Pedlar Member consists of thinly bedded, fine-grained, flaggy sandstone with ripple and current flow markings. The Cyclops Member contains flaggy sandstone and rhythmically thinly-bedded sandstone (Wells et al 1970). Preiss et al (1978) and Field (1991) considered the Waldo Pedlar and Cyclops members to be correlatives, although Freeman et al (1991) disagreed on the basis of their lithological differences. Sandstone of the Waldo Pedlar Member rests unconformably on the Olympic Formation. A sample from the Waldo Pedlar Member, comprising fine-grained, finely laminated sandstone with some soft sediment deformation, was collected from an isolated ridge southwest of Olympic Bore.
Kositcin, N., Normington, V.J., Edgoose, C.J., 2015. Summary of results. Joint NTGS-GA geochronology project: Amadeus Basin, July 2013-June 2014. Northern Territory Geological Survey Record, 2015-001, 56p.

DIO BETOOTA 1 was drilled to a depth of 2994.4 m by Delhi Petroleum Pty Ltd in 1959. It is located in central western Queensland approximately 9 km east-southeast of Betoota and is near a present day artesian bore. The sample submitted for analysis is a red, medium- to coarse-grained lithic sandstone. Basement rocks in DIO BETOOTA 1 were assigned by Brown et al. (2012) to the Thomson Orogen package and/or the suggested time equivalent, Warburton Basin. They are overlain by sedimentary rocks of the early Permian- Middle Triassic Cooper Basin and Jurassic to Cretaceous Eromanga Basin (Brown et al., 2012). This sample was submitted for SHRIMP U-Pb analysis to obtain zircon provenance age information and a maximum deposition age.
Betoota 1
Cross, A.J., Purdy, D.J., Bultitude, R.J., Brown, D.D., Carr, P.A., 2016. Summary of results - Joint GSQ-GA geochronology project: Thomson Orogen, New England Orogen, Mossman Orogen and Mount Isa region, 2011-2013. Queensland Geological Record, 2016/03, 142p.; Purdy, D.J., Cross, A.J., Brown, D.D., Carr, P.A., Armstrong, R.A., 2016. New constraints on the origin and evolution of the Thomson Orogen and links with central Australia from isotopic studies of detrital zircons. Gondwana Research, 39, 41-56.

This sample of foliated and laminated metasiltstone was collected from DDH DR20 (Aberfoyle), depth interval 268.05-269.60 m, at the W. B. Clarke Geoscience Centre at Londonderry. In thin section, the sample contains quartz, fine-grained white mica, minor biotite, and andalusite. A continuous cleavage and minor development of shear bands were also noted. Hole DDH DR20 was drilled towards the northwest, from hangingwall to footwall of the so-called DMK line in the Doradilla area, which contains the Doradilla, Midway and 3KEL tin deposits, and was designed to intersect steep southeast dipping mineralisation and structures. The top of the hole intersected contorted quartz-mica metasedimentary rocks interpreted as Girilambone Group. The hole then intersected calc-silicate schists and porphyritic dykes associated with the Midway Granite, before intersecting the sampled laminated metasiltstone and metasandstone sequence towards the end of hole. This latter sequence lacks the deformation seen in rocks at the top of the hole, and is interpreted to be north of the DMK line. Sn-skarn mineralisation along the DMK line in the Doradilla area consists of a linear, mineralised calc-silicate horizon, with alteration intensity increasing with proximity to the Middle Triassic Midway Granite (Burton et al., 2007). The protolith of the calc-silicate horizon is enigmatic, with a calcareous sediment or limestone horizon proposed by previous workers, with this horizon interpreted to be younger (possibly equivalent to the Late Silurian-Early Devonian Cobar Supergroup) than the surrounding Girilambone Group (Burton et al. 2007). An ~11 m intersection of marble in drillhole Midway MW2 along the DMK line to the northeast supports a limestone protolith. The only age constraint currently comes from Glen et al. (2010) who sampled a quartz-rich metasandstone from the surface near the historical Doradilla headframe north of the DMK line and determined a maximum depositional age of ~ 420 Ma.

Areyonga Formation
The fluvial to glaciogene Areyonga Formation predominantly consists of diamictite but includes interbeds of sandstone, conglomerate, shale, siltstone and dolostone (Preiss et al 1978; Walter et al 1995; Edgoose 2013). The Areyonga Formation rests disconformably on the Bitter Springs Formation (Wells et al 1970) and in turn is conformably overlain by siliciclastics and carbonates of the Aralka Formation. The sample was collected west-southwest of Dead Horse Waterhole where the Areyonga Formation is expressed as topographic highs and ridges. The outcrop is locally steeply dipping and is variably micaceous and silicified. The sample is a well-bedded and laminated, immature, medium- to coarse-grained quartz sandstone with occasional gravel beds up to 1 cm wide. The sandstone overlies ~50 m of diamictite. Proximal to the sample location is an outcrop of cap carbonate, which in other areas is observed directly overlying the diamictite. These cap carbonates, which occur in association with the glacial sediments of the Areyonga Formation across the Amadeus Basin, have been correlated with 700-690 Ma Sturtian glaciation successions across Australia and globally. In thin section, interlocking quartz grains are subangular to rounded and range between 100 um and 500 um in length. Rounded, 500 um rock fragments, comprised of chert or micro-quartz make up 5-10% of the sample, with micro-quartz and clay minerals infilling the matrix.
Kositcin, N., Normington, V.J., Edgoose, C.J., 2015. Summary of results. Joint NTGS-GA geochronology project: Amadeus Basin, July 2013-June 2014. Northern Territory Geological Survey Record, 2015-001, 56p.

Sefton Metamorphics
PHP4/D3 was a mineral exploration hole drilled to a depth of 95 m by Newmont Holdings Pty Ltd in 1985, in the Iron Range Province of the eastern Cape York Peninsula. Based on similarities of rock types and ages, Purdy et al. (2013) suggested that the Iron Range Province could be a northerly extension of the Thomson Orogen. The only formal unit identified is the Sefton Metamorphics (Willmott et al., 1973), which comprise compositionally diverse siliciclastic and calc-silicate rocks typically metamorphosed to greenschist facies (Trail et al., 1969; Teluk, 1984; Blewett and Knutson, 1997), and intruded by Paleozoic (Silurian-Permian) granites of the Pama Igneous Association and Kennedy Igneous Association (Purdy et al., 2013). SHRIMP U-Pb detrital zircon data from a metaconglomerate (Blewett et al., 1998) yielded five grains between ~1240 Ma and ~1060 Ma, which defined a loose maximum deposition age. More recently, Kositcin et al. (2015b) reported SHRIMP U-Pb detrital zircon data from two Sefton Metamorphics samples: one (2165207/PCTH013) contained a single grain at 992 +/- 29 Ma (2sigma), interpreted as a maximum deposition age; the other (2165082/PCTH010) gave an age of 1648.6 +/- 4.5 Ma defined by the youngest 39 grains. A sample of strongly deformed quartz mica schist was submitted for SHRIMP U-Pb detrital zircon analysis to obtain provenance age information and a maximum age of deposition. The sample comprises quartz as fine crystals with chess board texture along with patches of fine calcite and chlorite, and rarely as larger, twinned rhombohedral crystals. Large albite grains occur within strongly foliated mica-rich domains and contain sigmoidal inclusion trails comprising abundant, fine-grained acicular crystals. The sample overall comprises quartz (45%), calcite (30%), chlorite (10%), biotite (10%), and feldspar (5%). Approximately 10 m deeper in the hole, the schist is intruded by a quartz diorite (sample 2152167/SEF_b) which failed to yield zircons.

Olympic Formation
The Olympic Formation, formally the Olympic Member of the Pertatataka Formation (Wells et al 1967), disconformably overlies the Aralka Formation, and is restricted to the northeastern portion of the Amadeus Basin. The Pioneer Sandstone, a lateral equivalent to the Olympic Formation, extends across to the north-central part of the basin. Both these formations have been correlated with Elatina glacial successions within the Adelaide Fold Belt and the Georgina, Ngalia and Officer basins (Lindsay 1993; Walter et al 1995). However, significant uncertainty is associated with the age of the Elatina Glaciation; no direct age determination is available, and only maximum and minimum age limits of ~640 Ma and ~580 Ma can presently be applied (see Williams et al 2008; Grey et al 2011). The Olympic Formation comprises lenticular units of sandstone, siltstone, conglomerate, diamictite, shale and dolostone (Edgoose 2013). Coarse-grained, faintly laminated and well bedded, feldspathic sandstone from the lowermost unit exposed on a steep cliff approximately 9 km southwest of Mt Capitor was collected for geochronology. The sandstone is overlain by diamictite and siltstone units, with interlayered carbonates near the top of the succession. In thin section, the sample consists predominantly of interlocking, subangular to subrounded quartz grains mostly between 100 um and 200 um in size but up to 500 um. K-feldspar crystals are typically angular and approximately 300 um in length. Subrounded to rounded rock fragments, mostly micro-quartz, make up ~2% of the sample. The matrix consists of very fine-grained quartz.
Kositcin, N., Normington, V.J., Edgoose, C.J., 2015. Summary of results. Joint NTGS-GA geochronology project: Amadeus Basin, July 2013-June 2014. Northern Territory Geological Survey Record, 2015-001, 56p.

Julie Formation
The Julie Formation was originally a member of the Pertatataka Formation (Wells et al 1967), subsequently upgraded to Formation status by Preiss et al (1978) due to the wide distribution of the unit and its importance as a marker bed. The formation conformably overlies the Pertatataka Formation (Kennard et al 1986) and is comprised of predominantly carbonate rocks such as dolostone and limestone, with lenses and beds of sandstone and occasional siltstone (Wells et al 1970). The formation also contains thickly-bedded ooid grainstones of shallow marine origin representing an upward-shallowing cycle, following deposition of the deeper water Pertatataka Formation. The sample was collected from the base of the Allabarinja Range where the Julie Formation comprises interbedded dolostone and sandstone. The dolostone is platy with calcrete crusts formed on erosional surfaces and the sandstone beds are gritty and calcareous. The sample collected for geochronology was a gritty, calcareous medium-grained sandstone interlayered with dolostone and dolomitic siltstone as beds ~10-20 cm thick.

Birksgate Complex
This sample was selected for geochronology based on field relationships and petrographic interpretation that suggested this was a comparatively rare layered meta-sediment or volcaniclastic unit of the Birksgate complex within the Tieyon 100k mapsheet. It is a mesocratic crystalline rock composed of subequal abundances of grey felsic grains (feldspar, quartz) and ferromagnesian grains (hornblende, biotite). Antipathetic abundances of felsic and ferromagnesian grains defines indistinct mineralogical banding, and preferred orientation of ferromagnesian grains defines a foliation subparallel to the banding. The sample responds weakly to the hand magnet, suggesting minor magnetite is present. This sample is considered to have initially formed as a sedimentary deposit composed of mixed sedimentary components including clastic grains (plagioclase >> zircon), detrital clays, and calc-silicate chemical sedimentary components. Slight variations in the components may have been responsible for primary layering in the sediment. Recrystallisation occurred in response to regional metamorphism in the amphibolite facies, producing the granoblastic assemblage of plagioclase + quartz + hornblende + biotite + diopside + opaques (including magnetite) + apatite. Weak mineralogical banding may reflect primary sedimentary layering. A directed stress regime during this event produced preferred orientation of biotite and hornblende grains which defines a foliation subparallel to mineralogical banding. The relatively high abundance of quartz for the mesocratic nature of this metamorphic rock discounts an intermediate or basic igneous protolith, and provides mineralogical support for a sedimentary protolith.
Primary Industries and Resources South Australia (PIRSA)
Jagodzinski, E.A., Dutch, R., 2013. SHRIMP U-Pb geochronology of the Tieyon (5645) 1:100 000 mapsheet. Geological Survey of South Australia. Report Book, 2013/00006, 222p.

IOL BRAIDWOOD 1 was drilled to a depth of 2365.5 m by International Oil Proprietary in 1985. It is located in central western Queensland approximately 17 km northwest of Jundah, 500 m west of the Winton-Jundah Road and approximately 8 km northwest of its junction with the Thomson Development Road. The sample submitted for SHRIMP U-Pb analysis is a red, fine-grained calcareous sandstone. It is moderately sorted, silicified and contains subangular to subrounded lithic fragments that are occasionally mottled very pale grey green (Brown et al., 2012). It was classified as a Thomson Orogen unit by Brown et al. (2012) and is located in the northern part of the Devonian Warrabin Trough that in this area is concealed below sedimentary rocks of the Jurassic to Cretaceous Eromanga Basin. SHRIMP U-Pb detrital zircon geochronology was undertaken on this sample to obtain provenance age information and a maximum age of deposition in order to better understand its stratigraphic context.
BRAIDWOOD 1

AFO Comet 1 was drilled in 1965 by Associated Freney Oil Field. Basement was intersected at 717 metres and the hole terminated at 917 metres. The hole penetrates the Bowen Basin to the east of the outcropping Anakie Province and terminates in tuffaceous sandstone. Five cores, totalling 12.14 metres, were recovered from Comet 1 (Mines Administration Ltd, 1965; QDEX:1731). Core 2 is the most coarse-grained and was selected for geochronology to test correlation with the Combarngo Volcanics, identified in the Roma Shelf area (Murray, 1994) as a Late Carboniferous to Early Permian volcanic succession at the base of the Bowen Basin. The sample selected is a shallow-dipping, pale grey/green, silicified tuffaceous sandstone.
Comet 1
Kositcin, N., Purdy, D.J., Brown, D.D., Bultitude, R.J., Carr, P., 2015. Summary of results. Joint GSQ-GA geochronology project: Thomson Orogen and Hodgkinson Province, 2012-2013. Queensland Geological Record, 2015/02, 68p.

Gillen Member
The Bitter Springs Formation comprises three members (Gillen, Loves Creek and Johnnys Creek members) consisting of dolostone, limestone, siltstone, sandstone, halite, evaporites, and a basaltic unit. Its depositional age is currently constrained to approximately 820 Ma based on geochemical correlation of the basalt with the Amata Dolerite in the Musgrave Province. The Amata Dolerite forms part of a continental flood basalt province and has been dated at ca 800 Ma (Sm-Nd whole rock + clinopyroxene + plagioclase, Zhao and McCulloch 1993; Zhao et al 1994), and 824 +/- 4 Ma (U-Pb baddeleyite; unpublished data quoted in Glikson et al 1996). The Gillen Member is the lowermost unit of the Bitter Springs Formation and consists of dolomite, green siltstone, sandstone, shale and evaporites, and sits paraconformably on the Heavitree Quartzite. The sample was collected in an area where five depositional cycles of the Gillen Member have been identified (units 1 to 5 of Lindsay 1993) from outcrop of steeply dipping and tightly folded interbedded limestone and fine-grained micaceous quartz sandstone, and is interpreted to belong to Unit 2 of the Gillen Member. The sandstone consists of quartz and muscovite within an Fe-oxide matrix. In thin section, pore space >500 um is infilled with carbonate. The outcrop is weathered, and the limestone beds have surficial solution weathering patterns on exposed bedding planes.

Poorly sorted, immature, medium-grained sandstone composed of subhedral quartz grains and subsidiary K-feldspar and plagioclase, with small lithic clasts dominated by quartz and mica.
Explorer 28
Maidment, D.W., Huston, D.L., Donnellan, N., Lambeck, A., 2013. Constraints on the timing of the Tennant Event and associated Au-Cu-Bi mineralisation in the Tennant Region, Northern Territory. Precambrian Research, 237, 51-63.

HPP GOLEBURRA 1 was drilled to a depth of 1581.3 m by Hematite Petroleum Pty Ltd in 1972. It is located approximately 44 km east of Winton, central Queensland and ~1.4 km north-northeast of Colane No. 2 Bore adjacent to Scarlet Creek. The sample analysed is a fine grained quartzite. Murray (1994) describe it as is a metamorphosed quartzofeldspathic sandstone with larger clasts of quartz and feldspar (up to 0.5 mm) as well as smaller clasts and matrix that have been recrystallised to a mosaic of quartz, plagioclase, muscovite, green biotite, calcite and chlorite (Murray, 1994). Basement core in HPP GOLEBURRA 1 has been assigned as Thomson Orogen by Brown et al. (2012) and is overlain by sediments of the mid Carboniferous-Middle Triassic Galilee Basin, and Jurassic to Cretaceous Eromanga Basin.
Goleburra 1

This sample (comprising fine-grained 'red-bed' sandstone and feldspathic coarse-grained sandstone to granule conglomerate) was collected from a steep gully below the sandstone cliffs of the Mount Oxley Formation (informal) on the southeast flank of Mount Oxley. Excellent, near continuous exposure of poorly sorted conglomerates of the Moira Formation (informal) red beds are found within the steep, upper part of this gully. The Moira Formation unconformably overlies the Booda Formation (informal), with the unconformity mapped at several locations around the base of Mount Oxley and the Oxley Range. A transitional contact between the Moira Formation and the overlying Mount Oxley Formation has been observed throughout the area. There are currently no age constraints on either the Moira Formation or Mount Oxley Formation at Mount Oxley or the Oxley Range due to a lack of fossils. The units are openly folded with a north-south trending syncline interpreted at Mount Oxley. No tectonic foliations have been observed, and the unit is interpreted to post-date Cobar deformation at ~400 Ma. The Moira and Mount Oxley formations are considered to be part of the Mulga Downs Group. Elsewhere in the Mulga Downs Group fish fossils have been used to constrain a Middle to Late Devonian age. The sample was collected to obtain a detrital zircon age spectrum for comparison with other local and regional sedimentary rocks.

Hodgkinson Formation
The sample was collected east of Thornborough, 650 m SE of the road to Kingsborough, on the SW side of a station track. It is from a NNW- trending, lenticular package of rocks (informal subunit Dhr9) 80 km long and up to 5 km wide in the southern-central part of the Hodgkinson Formation. This belt is distinguished from adjacent packages by reddish pink to maroon tones on ternary radiometric images (reflecting relatively high potassium counts) which contrast with the much paler tones of adjacent subunits Dham and Dhm, but are similar to those shown by rocks mapped as part of the same subunit 120 km to the north (WSW of Lakeland Downs on Bonney Glen station; sample 2153450/BB4542, this record). Zircons were analysed to compare their provenance age spectrum with spectra defined by other samples from the Hodgkinson Formation. At this site, bouldery outcrops comprise brownish grey, poorly sorted sandstone and conglomeratic sandstone containing detrital muscovite as a conspicuous minor component, and minor cobble conglomerate. Clasts in the sandstones are granule- to pebble-sized, and consist mainly of quartz (up to 2 cm), but also include angular intraformational fragments (up to 3 cm, of black carbonaceous mudstone and scarcer fine-grained sandstone and siltstone), and a range of basement clasts (including fine-grained granitoid). Framework grains are mainly subangular and 0.2-2 mm (average ~0.8 mm). They consist mainly of quartz (70%; mostly monocrystalline, rarely polycrystalline), fresh to slightly altered plagioclase and K-feldspar in roughly equal amounts (6% each), and minor (3%) detrital muscovite as slender flakes up to 2 mm. Most muscovite grains show undulose extinction and some have curved cleavage planes. Fine-grained matrix components (<10%) encompass biotite, chlorite, sericite, calcite, and accessory zircon and garnet. Lithic fragments are scarce (<5%), and comprise mudstone, siltstone, chert, quartzite and fine-grained schist.
Cairns Region

Hodgkinson Formation
The sample was collected from a headland at the northern end of a small beach on the southern side of Archer Point. The headland consists mainly of grey, thick-bedded, poorly sorted, fine to coarse-grained sandstone (0.1-2 mm; average ~0.8 mm). Framework components range from angular to rounded. Quartz grains (mainly monocrystalline, some polycrystalline) make up 25% of the rock. Some of the monocrystalline quartz grains have straight or slightly curved sides with rounded corners, straight to slightly undulose extinction, and very few inclusions; these may have been derived from felsic volcanic sources. Fresh or only slightly-moderately altered feldspars (15%) are a relatively common framework component, with some grains showing cross-hatched twinning typical of microcline. Detrital muscovite is rare. Lithic fragments are abundant (40%), and dominated by subangular to rounded volcanic fragments up to 2 cm. These range in composition from felsic to mafic, with intermediate to mafic types predominating. Some rounded-subrounded clasts (up to 1.5 mm) of probable metamorphic origin (quartzite, feldspathic quartzite or leucogneiss are also present. The sandstone also contains sparse angular fragments (up to 1.5 mm) of mudstone, chert, metachert, and metasiltstone. The matrix (15-20%) is dominated by very fine metamorphic biotite, thought to be related to a relatively high geothermal gradient associated with the emplacement of numerous Permian granites in the region. The sandstone is distinguished by a scarcity of quartz grains, very little detrital muscovite, a relative abundance of fine, metamorphic biotite, and a high proportion of igneous clasts compared to other sandstones analysed as part of this investigation (2132758/BB5434, 2134407/BB5438, 2153450/BB4542). A sample from Archer Point was collected for geochronology because the rocks have a distinctly different provenance compared to other samples so far analysed from the Hodgkinson Formation.
Cairns Region

Les Jumelles beds
The Les Jumelles beds are a Paleozoic succession of cleaved sandstone and mudstone in the northern part of the Anakie Province which occur as two north-north-easterly trending, parallel belts 60 km long and up to 8 km wide. The site is 53 km north-northwest of Mount Coolon on Pyramid station. Previous age constraints were provided by the overlying Early Devonian Ukalunda Formation and the intrusion of the Coquelicot Tonalite at 471 +/- 4 Ma (L.P. Black, personal communication, 2004 in Fergusson and Withnall, 2013). The unit shows only one, steeply dipping silty cleavage, and contrasts with the adjacent more complexly deformed rocks of the Anakie Metamorphic Group, which show a dominant shallowly dipping S2 foliation folded by open upright folds. Fergusson and others (2001) assigned a late Neoproterozoic to middle Cambrian age to the Anakie Metamorphic Group based on detrital zircon and monazite, and interpreted it as having been deformed during the Delamerian Orogeny at 510-480 Ma (Withnall and others, 1996; Wood and Lister, 2013). Lithologically, the Les Jumelles beds are similar to the Puddler Creek Formation, the lowermost unit of the Seventy Mile Range Group in the Charters Towers Province to the north, and inferred to be Cambrian, based on superpositional evidence. Overlying units in the Seventy Mile Range Group, which include a submarine volcanic succession are late Cambrian to Early Ordovician, with ages constrained by graptolite faunas (Henderson, 1986; Fergusson and others, 2013). The sample is a greenish brown, fine-grained, sublithic sandstone with quartz veinlets, consisting of subrounded quartz and feldspar grains in a greenish matrix of chlorite, biotite and finer quartz and feldspar that shows a pronounced fabric in thin section.
Anakie Region
Purdy, D.J., Cross, A.J., Brown, D.D., Carr, P.A., Armstrong, R.A., 2016. New constraints on the origin and evolution of the Thomson Orogen and links with central Australia from isotopic studies of detrital zircons. Gondwana Research, 39, 41-56.

Poorly sorted, immature, medium-grained sandstone composed of subhedral quartz grains and subsidiary K-feldspar and plagioclase, with small lithic clasts dominated by quartz and mica.
White Devil Mine
Maidment, D.W., Huston, D.L., Donnellan, N., Lambeck, A., 2013. Constraints on the timing of the Tennant Event and associated Au-Cu-Bi mineralisation in the Tennant Region, Northern Territory. Precambrian Research, 237, 51-63.

This is a fine-grained dark greenish grey rock in which a strong foliation is emphasised by thin discontinuous white lenticles. In polished thin section, this sample retains some of its primary fragmental texture despite strong ductile deformation and metamorphic replacement. Clastic particles occur in moderate amount. They are almost entirely K-feldspar, occurring as small angular grains 0.1-0.2 mm in size. Most are single grains, wrapped by the foliation. They are scattered throughout the rock, but tend to be loosely concentrated in particular horizons in the matrix. Minor larger polycrystalline fragments are composed of granular K-feldspar, suggesting derivation from a felsic crystalline source. Minor chlorite forms small flakes enwrapping margins of the K-feldspar grains. A significant proportion of the rock is composed of thin lenticles which are strongly elongated in the trace of the foliation. The lenticles are mostly ~0.4-0.8 mm wide, and many mm to cm long. They are composed of fine-grained foliated ?stilpnomelane or ?biotite flakes, sericite flakes, and tiny magnetite granules. Many of the lenticles contain tiny lath-like crystals, most likely small quench plagioclase laths in basaltic lithic fragments. Titanite forms subhedral grains, some porphyroblastic in size up to 0.2-0.4 mm. Fine-grained matrix is composed of small aligned pleochroic brown stilpnomelane or biotite flakes, small colourless muscovite flakes, and minor tiny magnetite granules. Calcite occurs in moderate amount as anhedral clear grains which are concentrated in granular lenticles and aggregates aligned in the trace of the foliation. They occur in the matrix, in the deformed altered ?basaltic lava clasts, and along contacts between the deformed clasts and matrix.
Reid, A., Jourdan, F., Jagodzinski, E.A., 2012. Project PGC02-01: Report for Gold Fields Australasia Ltd on geochronology from the Haylands Prospect, South Australia. IN Reid, A. and Jagodzinski, L. (eds) PACE Geochronology: Results of collaborative geochronology projects 2011-12. South Australian Department of Primary Industry and Resources, Report Book, 2012/00012, 51-76.

Mount Eclipse Sandstone
The dated sample was collected from an interval of medium- to coarse-grained sandstone, subarkosic, with highly carbonate-cemented zones interbedded with layers containing rip-up clasts, micas and black ‘carbonaceous’-looking zones (drillhole B07124 from a depth interval of 138 –139.1 m from the Bigrlyi U –V deposit). The drill core is held by Energy Metals Ltd at their exploration camp at Bigrlyi. Drillhole B07124 intersects a sequence of interbedded fine- to medium-grained sandstone, fine-grained sandstone to clay and medium- to coarse-grained sandstone representative of the Mount Eclipse Sandstone. The Mount Eclipse Sandstone is currently interpreted to be Late Devonian to Carboniferous in age.
Kositcin, N., Beyer, E.E., Whelan, J.A., Close, D.F., Hallett, L., Dunkley, D.J., 2013. Summary of results. Joint NTGS-GA geochronology project: Arunta Region, Ngalia Basin,Tanami Region and Murphy Province July 2011-June 2012. Northern Territory Geological Survey Record, 2013-004, 39p.

Number of analyses corresponds to the younger component (50% of the population) derived from 2-component mixture modelling of 20 analyses.
Corny Point Paragneiss
Drillhole PYD001 lies in the central southern Yorke Peninsula and penetrated variably magnetite-sericite altered gneissic "granite" with local zones of magnetite-biotite-chlorite-sericite-pyrite-chalcopyrite alteration. The gneissic granite appears to have zones of partial melt, i.e. leucosome, which together with the biotite-rich melanosome defines a gneissic layering. This sample has been selected to determine the age of the protolith to see if it is part of the basement to the Wallaroo Group, i.e. Donington Suite, or whether it represents an apparently higher metamorphic grade equivalent of some portion of the Wallaroo Group. In thin section, the sample is a quartz-feldspar-muscovite-biotite gneiss. The sample preserves a granoblastic gneissic texture. The biotite-muscovite rich zones in the rock alternate with mica-poor zones and this alternation defines the gneissic foliation of the sample. Quartz is recrystallised and shows lobate grain boundaries in some instances. Plagioclase is variable altered by fine-grained sericite. K-feldspar is of lesser abundance than the plagioclase, and is intergrown in the granoblastic texture with the quartz and plagioclase. Muscovite occurs as laths to 1 mm in size, as does biotite. Biotite appears slightly more altered than the muscovite, with chlorite intergrown with some biotite crystals. There is magnetite within the rock present within the granoblastic texture suggesting it is part of the metamorphic mineral assemblage.
Jagodzinski, E.A., Reid, A., Galloway Warland, N., 2017. Project PGC03-08: Yorke Peninsula project of Phoenix Copper Ltd. IN Jagodzinski, E.A. and Reid, A.J. (eds) PACE Geochronology: Results of collaborative geochronology projects 2013-15. Geological Survey of South Australia. Report Book, 2015/00003, 98-118.

Max depositional age. The maximum depositional age of this metasedimentary rock can be defined by the youngest grouping of three grains at 496 +/- 17 Ma.
GSQ Maneroo 1 was drilled in 1989-1990 by the Geological Survey of Queensland, intersecting basement at 1177 metres (Hoffman and others, 1991). Maneroo 1 is near the northern extent of the undercover Thomson Orogen and southern margin of the North Australian Craton, where a significant change in character and trend is observed in geophysical data sets. The basement interval of Maneroo 1 (below the Eromanga Basin) intersects ~21 metres of rhyolite before passing into a sequence of metasiltstone and metasandstone. The rhyolite has a U-Pb SHRIMP date of 472.9 ± 2.7 Ma (Draper, 2006) which provides a minimum age for the underlying metasedimentary interval. Here, we sample the metasedimentary interval to constrain a maximum age of deposition. The sample selected for geochronology consists of interbedded siltstone and sandstone containing clasts of quartz, feldspar, muscovite, biotite and lithic fragments (Murray, 1994).
GSQ Maneroo 1
Kositcin, N., Purdy, D.J., Brown, D.D., Bultitude, R.J., Carr, P., 2015. Summary of results. Joint GSQ-GA geochronology project: Thomson Orogen and Hodgkinson Province, 2012-2013. Queensland Geological Record, 2015/02, 68p.; Purdy, D.J., Cross, A.J., Brown, D.D., Carr, P.A., Armstrong, R.A., 2016. New constraints on the origin and evolution of the Thomson Orogen and links with central Australia from isotopic studies of detrital zircons. Gondwana Research, 39, 41-56.

A more conservative estimate of the maximum depositional age: 1153 +/- 9 Ma. MSWD = 0.66. N= 15 youngest analyses.
Kirkland, CL, Wingate, MTD, Smithies RH, Howard, HM and Quentin De Gromard, R 2014, 185414: quartzite, Bentley Hill; Geochronology Record 1180: Geological Survey of Western Australia, 5p.

Abercrombie Formation
Chisholm, E.I., Fitzherbert, J.A., Deyssing, L., Simpson, C.J., 2014. New SHRIMP U-Pb zircon ages from the Captains Flat area, eastern Lachlan Orogen, New South Wales: July 2012-June 2013. Geoscience Australia. Record, 2014/07, 47p.

Wingate, MTD, Kirkland, CL and Haines, PW 2013, 143747: pebbly sandstone, Pollock Hills; Geochronology Record 1107: Geological Survey of Western Australia, 6p.

It is possible that all of the analyses are of unmodified detrital zircons, in which case the date of 967 +/- 11 Ma (1 sigma) for the single analysis represents a maximum depositional age for the sandstone.
Wingate, MTD, Kirkland, CL and Haines, PW 2013, 143800: sandstone, Dinner Hill; Geochronology Record 1111: Geological Survey of Western Australia, 6p.

It is possible that all of the analyses are of unmodified detrital zircons, in which case the date of 831 +/- 13 Ma represents a maximum depositional age for the sandstone. A more conservative estimate is 903 +/-17 Ma (MSWD = 1.6) for the youngest six analysis.
Wingate, MTD, Kirkland, CL and Haines, PW 2013, 143799: sandstone, Dinner Hill; Geochronology Record 1110: Geological Survey of Western Australia, 6p.

alt. conservative maximum depositional age: 1124 +/- 13 Ma. MSWD=1.6. N=13 youngest
A more conservative estimate of the maximum depositional age can be based on the weighted mean 207-corrected 238U/206Pb* date of 1124 +/- 13 Ma (MSWD = 1.6) for the youngest coherent group of 13 analyses
Wingate, MTD, Kirkland, CL and Haines, PW 2013, 143783: sandstone, Mu Hills; Geochronology Record 1108: Geological Survey of Western Australia, 5p.

Wingate, MTD, Kirkland, CL and Haines, PW 2013, 143784: sandstone, Dovers Hills; Geochronology Record 1109: Geological Survey of Western Australia, 6p.

conglomerate + sandstone

psammite and pelite; interlayered

psammitic schist

The sample of laminated metasiltstone was taken from open file drillcore 09CPD001, Caroline Prospect, from a depth interval of 308.00 – 310.66 m, which was drilled by AusQuest Ltd in 2009 under the Drilling and Geophysics Collaboration funding provided by the NT Government. This greenfields drilling program targeted semi-coincident magnetic and gravity highs in an area of no outcrop in the Simpson Desert region, southeastern Northern Territory. The drillhole 09CPD001 intersected sediments of the Cretaceous Eromanga Basin to a depth of ca 185.1 m, which overlie a sequence of sulfidic laminated metasiltstones, coarse-grained metagabbroic sills and interpreted flow-banded metadacite/tuff of unknown age that was intersected to an EOH depth of 366.7 m. The metasediment comprises interlaminated metamorphosed carbonaceous sandy siltstone and quartz-rich sulfide-bearing sandstone with minor biotite, plagioclase and rare K‑feldspar. The laminated metasiltstones may represent a lower-grade equivalent of the upper-amphibolite- to granulite-facies, Neoproterozoic to Palaeozoic Harts Range Metamorphic Complex. Alternatively, the sequence could represent a currently unrecognised sedimentary succession overlying the Harts Range Metamorphic Complex.
Kositcin, N., Carson, C.J., Hollis, J.A., Close, D.F., Whelan, J.A., Webb, G., Donnellan, N., 2013. Summary of results. Joint NTGS-GA geochronology project: Arunta Region, Davenport Province and Pine Creek Orogen July 2009-June 2011. Northern Territory Geological Survey Record, 2012-008, 49p.

unnamed siltstone
A sample of metasiltstone was taken from open file drillcore 09CPD003A, Caroline Prospect, from a depth interval of 385.30-385.78 m, which was drilled by AusQuest Ltd in 2009 under the Drilling and Geophysics Collaboration funding provided by the NT Government. This greenfields drilling program targeted semi-coincident magnetic and gravity highs in an area of no outcrop in the Simpson Desert region, southeastern Northern Territory. The drill hole 09CPD003A intersected sediments of the Cretaceous Eromanga Basin to a depth of ca 194 m, which overlie a sequence of sulfidic laminated metasiltstones, coarse-grained metagabbroic sills and interpreted flow-banded metadacite/ tuff of unknown age that was intersected to an EOH depth of 537 m. The sample comprises interlaminated quartz-feldspar-biotite metasandstone and partly altered weakly carbonaceous quartz-biotite metasiltstone. This sample may represent a lower grade equivalent of the upper amphibolite- to granulite-facies, Neoproterozoic to Palaeozoic Harts Range Metamorphic Complex. Alternatively, the sequence could represent a currently unrecognised sedimentary succession overlying the Harts Range Metamorphic Complex.

Provenance clusters spanning 1781-1527 Ma; mixture modelled for maximum depositional age. Youngest of two-component mixture modelling of 44 analyses; fraction = 0.19 (i.e. about 8 analyses), misfit = 0.414. Interpreted as best (conservative) maximum age for deposition.
This sample was collected from the JHR Glenbede Downs 1 drill hole, between the 603.51 m to 664.47 m depth interval, within the Millungera Basin, Queensland. The sample was collected from drill cuttings, and was a red sandstone.
GLENBEDE DOWNS 1

psammitic gneiss

psammitic and pelitic gneiss; interlayered

metadiorite

conservative alt. max depositional age 207Pb/206Pb: 1796 - 24Ma MSWD=1.53. N=7 (includes youngest)
Kirkland, CL, Wingate, MTD, Tyler, IM and Sheppard, S 2010, 182102: quartz sandstone, Bindoola Creek; Geochronology Record 884: Geological Survey of Western Australia, 5p.

The sample was from basement to the Eromanga Basin, intersected by stratigraphic drillhole GSQ Eromanga 1, from the interval 1259.44 m to 1266.86 m. GSQ Eromanga 1 was drilled 62 km east of the township of Eromanga in south-western Queensland on the southern Canaway ridge, a basement high between the Adavale Basin proper and the Warrabin Trough. The unit sampled is a dark green-grey, very fine to fine-grained and cleaved sandstone, with a phyllitic sheen in places. In thin section the sandstone appears to be lithic, although the lithic grains are all altered. Quartz and biotite are also present. Chlorite is common and defines the cleavage in the sandstone.
GSQ Eromanga 1
Cross, A.J., Dunkley, D.J., Bultitude, R.J., Brown, D.D., Purdy, D.J., Withnall, I.W., von Gnielinski, F.E., Blake, P.R., 2015. Summary of results Joint GSQ-GA geochronology project: Thomson Orogen, New England Orogen and Mount Isa region, 2010-2012. Queensland Geological Record, 2015/01, 138p.

This sample was collected from the JHR Hampden Downs 1 drill hole, between the 658.38 m to 719.34 m depth interval, within the Millungera Basin, Queensland. The sample was collected from drill cuttings, and is a red sandstone.
HAMPDEN DOWNS 1

This sample was collected from the JHR Rosevale Downs 1 drill hole, between the 603.51 m to 655.33 m depth interval, within the Millungera Basin, Queensland. The sample was collected from drill cuttings, and was a red sandstone.
ROSEVALE DOWNS 1

Chiripee Metamorphics
Coarse-grained qtz-fsp-grt meta-psammite occurring in outcrop as >1m long boudins in qtz-fsp-bt-grt-sill metapelite. This sample was collected from a previously unidentified granulite-facies meta-sedimentary package in the Red Cliff area approximately 25km NE of the Mt Bleechmore Granulite. It is hoped the maximum deposition age, detrital spectra and metamorphic age/s, if any, will help correlate these rocks with one of the other known high-grade meta-sedimentary packages in the region i.e. either the Mt Bleechmore Granulite or Chiripee Gneiss.

Wingate, MTD, Kirkland, CL, Sheppard, S and Hollis, JA 2012, 190639: quartz sandstone, Gibb River Road; Geochronology Record 1035: Geological Survey of Western Australia, 5p.

Lu, Y, Wingate, MTD and Sheppard, S 2017, 190640: quartz sandstone, Gibb Range; Geochronology Record 1386: Geological Survey of Western Australia, 6p.

Carnot Gneiss
This sample is a garnetiferous gneiss sampled from a significant set of outcrops on the southern coast of Eyre Peninsula, a locality known as Redbanks. At Redbanks two main rock types are observed: garnetiferous gneiss and gneissic charnockite. The contact between the two gneissic phases is not clearly intrusive and appears to parallel the gneissic layering. The charnockite contains rafts of variably disaggregated mafic dykes that make up between 5% and 8% of the rock mass. The garnetiferous metasediment is compositionally layered, with some biotite-rich, some cordierite-rich and some garnet-rich zones likely reflecting original differences in bulk composition within a sedimentary pile. This metasedimentary gneiss is part of the Carnot Gneiss. Mafic gneiss is not common within the metasedimentary gneiss, except near the contact with the charnockite. Therefore it is possible that the charnockite intrudes the metasedimentary sequence, although this is by no means certain from the field relationships. The aim of this sample is to investigate the age and provenance of the Carnot Gneiss at this location, and to investigate the timing of metamorphism. In thin section, this sample is a garnet-bearing quartzo-feldspathic gneiss. Compositional layering at the thin section scale has leucocratic, quartz-plagioclase rich domains juxtaposed against garnet-biotite rich domains, reflecting the gneissic compositional banding. Garnet is irregularly shaped and poikiloblastic with inclusions of spinel, biotite and quartz. The matrix is composed of biotite, which is aligned to form the gneissic layering, together with medium-grained dynamically recrystallised quartz, with lesser plagioclase. Cordierite also occurs within the matrix, in some instances with spinel inclusions.
Jagodzinski, E.A., Reid, A.J., Hand, M., 2012. SHRIMP U-Pb geochronology of Archaean to Palaeoproterozoic rocks from the southern Eyre Peninsula. Geological Survey of South Australia. Report Book, 2012/00015, 78p.

This analysis indicates a moderate Th/U ratio (0.59).
Kirkland, CL, Wingate, MTD, Smithies, RH and Evins, PM 2012, 194767: psammitic enclave in gneiss, Mount Scott; Geochronology Record 1025: Geological Survey of Western Australia, 5p.

Broadview Schist
This sample is a representative section of the fine-grained metasedimentary rocks within the ML001DD core. The sample is laminated at the mm to cm scale, comprising alternating bands of more or less siliceous material. There is very little biotite visible in hand specimen and in places there appears to be fine feldspar phenocrysts visible. However, some laminations that appear more siliceous could represent clastic-dominated intervals. Although there are sulphide bearing quartz veins present within the sample, the large ones were removed before being sent for mineral separation. This sample is a medium to fine grained quartz-feldspar-muscovite schist, presumably of metasedimentary origin. The tectonic fabric within the sample is dominated by dynamically recrystallised quartz and feldspar, with mica also aligned parallel to this fabric. At the scale of the thin section, the tectonic fabric does not show significant asymmetry that might permit analysis of deformation kinematics. Quartz shows strong subgrain development forming polygonal textured grains. Plagioclase is pervasively sericite altered and shows hematite dusting, which gives the sample the characteristic red colouration. Muscovite is clear and occurs as 0.3 mm crystals parallel to the main fabric. Green coloured chlorite is present throughout the sample and occurs as elongate mats to ~0.2 mm size. This chlorite may replace biotite, or may be part of the metamorphic assemblage. Opaque grains are present throughout the sample. Zircons were observed, are rounded in appearance, probably reflecting a detrital origin. Narrow carbonate-filled fractures cross cut the schistosity within the sample.
DDH ML001DD
Jagodzinski, E.A., Reid, A., Johnson, G., 2011. Project PGC01-09: Host rock ages of the Moola Cu-Au Prospect, east of the Middleback Range. IN Reid, A. and Jagodzinski, L. (eds) PACE Geochronology: Results of collaborative geochronology projects. Geological Survey of South Australia. Report Book, 2011/00003, 127-143.

felsic volcanic rock

Youngest detrital zircon age component. Two-component mixture-modelling of the 72 post-1780 Ma analyses yielded ages at 1712 ? 4 Ma (2s, fraction = 0.82) and 1753 ? 9 Ma (2s, fraction = 0.18). In Queensland Geological Record 2011/03, the weighted mean of the youngest 82% of this population (i.e. 59 analyses), with age range 1736-1670 Ma, is preferred as the maximum depositional age.
Roxmere Quartzite
Collected by Allan Parsons GSQ for detrial zircon SHRIMP study

Within the diorite between 87.5 and 91.60 m is an interval of fine grained grey and pink laminated metasedimentary rock, which may be either a large enclave or the host rock to the diorite. The contacts between the diorite and metasedimentary rock are sharp, and the upper 50 cm of the latter is affected by hematite alteration, which is also found in the diorite and may be associated with younger felsic intrusives. The metasedimentary rock is composed of lenticular layers between less than 1 mm to 7 mm wide defined by alternating quartz and plagioclase-rich layers. Plagioclase is weakly hematite-stained, sericitised or albitised. Minor foliated biotite is altered to chlorite and leucoxene, and apatite and zircon occur as rare accessory phases. The sedimentary precursor may have been a layered quartzofeldspathic sandstone.
McAvaney, S., Jagodzinski, E.A., 2012. Geochronology and geochemistry of a Kimban diorite, drill hole LED001, Lake Gilles, eastern Gawler Craton. Geological Survey of South Australia. Report Book, 2012/00010, 83p.

metavolcanic and metavolcaniclastic rock

collected by L Hutton (GSQ) for SHRIMP detrital geochron and for comparsion with Soldiers Cap Group with which this sample is tentitatively correlated.
GSQ Dobbyn 1

Kirkland, CL, Wingate, MTD and Evins, PM 2010, 194420: feldspathic sandstone, Mount Blyth; Geochronology Record 923: Geological Survey of Western Australia, 5p.

Mungaroo Formation
siliciclastic sedimentary rock
North Rankin 5
Lewis, C.J., Sircombe, K.N., 2013, Use of U-Pb geochronology to delineate provenance of North West Shelf sediments, Australia. In: Keep, M. & Moss, S.J. (eds), The Sedimentary Basins of Western Australia IV. Proceedings of the Petroleum Exploration Society of Australia Symposium, Perth, WA, 27p.

This sample of metamudstone was collected from a dry creek channel north of the Booroomugga Road, approximately 500 m south-southeast of Goiters Tank on the Sussex property. The sample exhibits sedimentary bedding approximately 5 to 10 cm thick that strikes north-south and dips approximately 45 degrees to the east. This sequence of interbedded metasedimentary and concordant mafic vesicular basaltic rocks is known as the Ballast Formation, which is interpreted to be part of the Ordovician Girilambone Group. The basalts are interpreted to be lava flows (Burton et al., 2012). The age of the Ballast Formation has been constrained by conodont biozonation to be middle to late Darriwillian (Burton et al., 2012), however neither the top nor base of the unit is tightly constrained in age. In the field the sample was suspected to be a crystal lithic metamudstone that appeared to represent a reworked airfall tuff. The sample was collected for geochronology in the hope that it may provide a volcanic age constraint on the timing of deposition of this part of the Girilambone Group. Thin section analysis, however, showed the sample to be a weathered quartz-mica metamudstone.

The sample is a medium grained, quartz-biotite-garnet-sillimanite-muscovite schist, with minor quartz veining. The garnets are fine grained and occur either randomly throughout biotite-rich zones or appear to cluster along likely pre-metamorphic compositional (sedimentary) horizons within the biotite-rich schist. The rock preserves two metamorphic foliations. The early formed foliation, S1, is parallel to a prominent quartz vein set and is present only as biotite within the quartz veins and indicated by the broader compositional domains present within the sample, which may reflect sedimentary compositional layering, S0 parallel to the first generation metamorphic layering, S1. This inferred S0//S1 layering is tightly to isoclinally folded by a second schistosity, S2. The F2 folding has in places disrupted and boudinaged the quartz veins and has formed the second planar foliation, S2, which is axial planar to the folds and is the dominant fabric within the rock. This foliation is defined by alignment of biotite, sillimanite and muscovite laths, together with dynamically recrystallised, polygonal textured and equant quartz grains. Sparse plagioclase is observed, now recrystallised to a similar grain size as quartz. Biotite is common and generally 0.2-0.5 long. Coarse biotite, to 1 mm, is only developed in the fold hinges adjacent the quartz veins. Sillimanite occurs as both needle-shaped crystals parallel to S2 and as small fibrolite clots. Garnet is common, subhedral to anhedral, and some are distinctly elongate, having grown in alignment (and synchronously) with the S2 foliation. It contains small inclusions of quartz and opaques, however, no biotite, sillimanite or muscovite inclusions were observed. In some examples the garnet preserves weakly aligned inclusion trails of quartz that parallel the S2 foliation. Most garnet is fresh, but fractured grains are retrogressed to chlorite.
DDH BUDD 28
Jagodzinski, E.A., Reid, A., Farrell, F., 2011. Project PGC01-04: Geochronology of the Bungalow Prospect. IN Reid, A. and Jagodzinski, L. (eds) PACE Geochronology: Results of collaborative geochronology projects. South Australian Department of Primary Industry and Resources, Report Book, 2011/00003, 42-62.

Cahill Formation
Sample AL09CJC054 is a retrogressed micaceous schist with psammitic and pelitic layering. It contains layer-parallel leucosomes and knobs of a retrogressed phase that was possibly cordierite or andalusite. It crops out immediately beneath the unconformity with the Kombolgie Subgroup and, given its proximity to quartzite outcrops interpreted as Kudjumarndi Quartzite, these rocks were mapped as the Cahill Formation.

Bonya Metamorphics
Sample HU13BLR049z is a compositionally layered calc-silicate para-amphibolite comprising cm-scale bands of alternating hornblende-rich and plagioclase-rich layers. This lithology is a unit of the Bonya Metamorphics interpreted to have a mixed chemical-clastic sedimentary protolith that overlies, and is stratigraphically continuous with, siliciclastic schists of the Bonya Metamorphics. Samples from the Bonya Metamorphics have been dated previously. Claoue-Long and Hoatson (2005) recorded a SHRIMP U-Pb zircon upper intercept age of 1807 +/- 17 Ma and an isotopic resetting age of ca 478 Ma for an interpreted volcaniclastic unit, of which the former may represent an igneous crystallisation age. A metasandstone sample from the same sequence yielded a maximum depositional age of 1807 +/- 21 Ma with a dominant provenance mode at ca 1846 Ma, and less dominant modes at ca 2000 Ma, ca 2520 Ma and ca 2555 Ma (Kositcin et al 2014). The relationship between the sample of Claoue-Long and Hoatson (2005) and outcrops of Bonya Metamorphics in the Bonya Hills to the west are not clear and therefore HU13BLR049z was collected from an area where the unit is better defined.
Kositcin, N., Reno, B.L., Whelan, J.A., 2015. Summary of results. Joint NTGS-GA geochronology project: Arunta Region, July 2014-June 2015. Northern Territory Geological Survey Record, 2015-007, 26p.

Yarraden Schist
This sample was collected from the northern part of the Archer River Shear Zone to the west of the Portland Roads road where it outcrops on the top of a low ridge. It consists of light brown, folded, medium-grained sillimanite schist with relict cordierite. The main fabric of the rock is defined by bands of recrystallised quartz with complex grain boundaries, minor biotite and bands of muscovite and sillimanite that dominantly occur as coarse flakes with some finer aggregates of mica. The micaceous bands are commonly folded and appear to have accommodated most of the strain. Secondary hematite is also common. This unit was previously mapped as a part of the Sefton Metamorphics by Willmott et al. (1977), however, it is lithologically similar to the Yarraden Schist and has been updated in new GSQ mapping.
Sample 2306984/DBCY064C was collected from the northern part of the Archer River Shear Zone to the west of the Portland Road where it outcrops on the top of a low ridge.
Cross, A.J., Dhnaram, C., Lisitsin, V., Bultitude, R.J., Brown, D.D., Purdy, D.J., Von Gnielinski, F., 2019, Summary of results. Joint GSQ-GA geochronology project: Cairns, Cape York and Georgetown regions, 2015-2016. Queensland Geological Record, 2019/01.

The sample is a moderately altered, unweathered, massive, grey-white coloured, fine-grained sandstone with subordinate siltstone intervals. Local soft-sediment deformation features are present. Alteration minerals are sericite, chlorite and carbonate. The upper and lower contacts of the interval with siltstone units are sharp. In thin section quartz is dominant, and occurs as angular to sub-rounded, generally fine grains. Other identified minerals include detrital opaque minerals, detrital feldspar (plagioclase?), lenticular muscovite, and zircon. The lenticular muscovite is oriented and may reflect relict bedding or a shear fabric. Larger grains appear to be cemented with a combination of quartz and clay minerals.
Lewis, C.J., Cayley, R.A., Duncan, R.J., Schofield, A., Taylor, D.H., 2016. New SHRIMP U-Pb zircon ages from the Stavely region, western Victoria: July 2014-June 2016. Geoscience Australia. Record, 2016/27, 203p.

Lochs Gneiss
Biotite gneiss associated with pegmatitic sweats and pods. Located to the north of the Archer River Quarry. Detrital inheritance from this sample would be useful to establish a link with the Sefton metamorphics or for comparison. Sample 2306985/DBCY043 consists of medium grained biotite quartz gneiss with rare sillimanite and pods of quartz muscovite pegmatite. The texture of the rock is defined by bands of quartz and feldspar with complex grain boundaries and layers of aligned euhedral flakes of biotite and some patches of fine muscovite with sillimanite. Quartz is commonly recrystallised.
Sample 2306985/DBCY043 is from the upper reaches of Wrights Creek, part of the Archer River Shear Zone which is a sigmoidal northern extension parallel with the Coen Shear Zone to the south.
Cross, A.J., Dhnaram, C., Lisitsin, V., Bultitude, R.J., Brown, D.D., Purdy, D.J., Von Gnielinski, F., 2019, Summary of results. Joint GSQ-GA geochronology project: Cairns, Cape York and Georgetown regions, 2015-2016. Queensland Geological Record, 2019/01.

The sample site is located north of the Frenchmans Track on the eastern side of the Pascoe River. The mapped bodies of Sefton Metamorphics in the sample area are separated from the main outcropping area in the Iron Range region by the intrusion of the Weymouth Granite and the Janet Ranges Volcanics. Sefton Metamorphics in this area are exposed as a series of small basement windows beneath Cenozoic sediments. Located on a hill capped by the Yam Creek Beds on the southern side of Garraway Creek, 2306986/DPCY011 consists of a boulder of quartzite which was part of a matrix supported metaconglomerate with a sand-sized iron rich matrix which shows a crenulated cleavage. Sample 2306986/DPCY011 is comprised of fine to medium grained quartz with occasional muscovite and hematite. Muscovite is aligned and quartz is consistently fine grained with interlocking boundaries and moderately sorted. The sampled clast was approximately 20 centimetres in diameter. This sample is to provide more depositional timing constraints on the northern part of the Sefton Metamorphics.
GSQ site DPCY011: Located on a hill capped by the Yam Creek Beds on the southern side of Garraway Creek.
Cross, A.J., Dhnaram, C., Lisitsin, V., Bultitude, R.J., Brown, D.D., Purdy, D.J., Von Gnielinski, F., 2019, Summary of results. Joint GSQ-GA geochronology project: Cairns, Cape York and Georgetown regions, 2015-2016. Queensland Geological Record, 2019/01.

Buddycurrawa Volcanics
The Buddycurrawa Volcanics (Benmara Group, Rawlings et al., 2008) form recessive to mildly resistant outcrops in northeastern Boxer (100K mapsheet). The unit omprises a basal ferruginous sandstone unit, overlain by a mixed interval of coherent trachyte, debris flow sandstone and conglomerate, mature sandstone, ferruginous siltstone/fine sandstone and minor stromatolitic chert. A maximum of 300 m is inferred from outcrop width and dips. The basal ferruginous sandstone itself is 10-20 m thick. The Buddycurrawa Volcanics rest conformably on the Breakfast Sandstone and are, in turn, unconformably overlain by the Bowgan Sandstone and, locally, Crow Formation of the South Nicholson Group (Rawlings et al., 2008). Generally, the Buddycurrawa Volcanics is poorly exposed and deeply weathered (Rawlings and Sweet, 2004) and has undergone pervasive and substantial potassic alteration (13.3% wt% K2O, 0.11wt% CaO, 0.32 wt % Na2O) and exhibits elevated REE abundances. However, Rawlings et al. (2008) reported a ‘ca 30-40 m thick trachyte sheet’ with up to 10 m of local relief and good quality exposure, with a blocky rubbly highly fragmented nature. In general, the unit is massive, with simply-twinned k-feldspar phenocrysts up to 1 cm in length, hosted within a brick-red to purplish coloured devitrified fine-grained matrix. Elsewhere, the unit can be highly vesicular, with abundant 1-3 mm diameter vesicles, commonly filled with pale green secondary glauconite. Euhedral tabular phenocrysts of glauconite are also observed within the matrix of the massive variety. The massive variety also hosts unusual vertically aligned siliceous ‘tubes’ or ‘pipes’ (up to 30 cm long, and 30-40 mm diameter) possible representing degassing or volatile expulsion features formed during crystallisation of the lava sheet. This sample was taken from the massive, coarse-grained non-vesicular component of the trachyte ‘sheet’, near the type locality described by Rawlings et al. (2008).
Kositcin, N., Carson, C.J., 2019. New SHRIMP U-Pb zircon ages from the South Nicholson and Carrara Range regions, Northern Territory. Geoscience Australia. Record, 2019/09, 217p.

Caulfield beds
The Caulfield beds are restricted to north-central MOUNT DRUMMOND including outcrops of the Bauhinia Dome, an area previously mapped as Fickling beds by Smith and Roberts (1963). The Caulfield beds form a generally recessive unit, comprising the low-relief core of the Bauhinia Dome (centred on 755000mE 8000000mN northeastern Benmara 100K). The beds are unconformably overlain by the Constance Sandstone (South Nicholson Group) with only minor angular discordance (Rawlings et al., 2008). The base of the Caulfield beds is not exposed. The Caulfield beds are flat-lying to gently dipping and do not appear to be metamorphosed or significantly deformed. Outcrop at the sample locality is rubbly, deeply weathered and highly friable. The sampled unit is a texturally immature medium-grained feldspathic micaceous (muscovite>biotite and minor secondary chlorite) sublithic gritty to pebbly sandstone with local thin discontinuous pebble lags. Minor rounded tourmaline grains and glauconite are present. Bedding is poorly defined. Individual feldspars (in thin section) retain subhedral to euhedral crystal morphology, indicating little mechanical abrasion or rounding due to transport, suggesting the Caulfield beds are proximal to their source region.
Kositcin, N., Carson, C.J., 2019. New SHRIMP U-Pb zircon ages from the South Nicholson and Carrara Range regions, Northern Territory. Geoscience Australia. Record, 2019/09, 217p.; Carson, C.J., Kositcin, N., Anderson, J.R., Henson, P.A., 2023, A revised Proterozoic tectono-stratigraphy of the South Nicholson region, Northern Territory, Australia - insights from SHRIMP U-Pb detrital zircon geochronology. Australian Journal of Earth Sciences, in press.

The sample was collected from near the base of the formation on the lower slopes of a ridge, about 50 m east of Ryan Bend Road and about 11 km (by road) west of its junction with the Carpentaria Highway. The reference section was selected by Jackson et al (1987) around a single grid coordinate (610051mE 8208479mN). The Yalco Formation comprises dominantly fine-grained and parallel-bedded aphanitic dololutite and dolarenite with abundant nodules and laminae of early diagenetic chert, and minor interbedded lithic sandstone (Jackson et al 1987). The dolostones are commonly stromatolitic and contain ripple marks, gypsum pseudomorphs and casts, tepee structures, and desiccation cracks. The minor interbedded sandstone is fine- to coarse-grained, in places conglomeratic, and occurs in lenticular beds. It is mostly parallel-bedded, but low-angle cross-beds and less common ripple laminations are also present. Sample BD16TJM042A is from a cross-bedded, grey-brown-weathering, light grey dolomitic sandstone interbedded within a predominantly dolostone succession
Kositcin, N., Munson, T.J., Whelan, J.A., 2017. Summary of results. Joint NTGS-GA geochronology project: greater McArthur Basin, July 2016-June 2017. Northern Territory Geological Survey Record, 2017-012, 64p.

The sample was collected from the top of the formation in the type section, along a minor tributary of Clarke Creek, about 26 km west-southwest of the junction of Ryan Bend Road and the Carpentaria Highway. The type section was originally selected by Jackson et al (1987) around a single grid coordinate (591425mE 8208666mN), but is more accurately located from 591222mE 8208863mN (base) extending south-southwestward along a creek to the sample site (top). The Smythe Sandstone typically comprises a basal massive, coarse polymictic conglomerate, overlain by a thick succession of poorly sorted and prominently cross-bedded, fine- to medium-grained, pebbly lithic (chert) sandstone, quartz sandstone and minor sandy dolarenite. Sample BD16TJM037 is from medium-bedded, gently southwest-dipping, fine- to medium-grained sandstone exposures forming a low scarp on the south bank of a small creek, and is a purple-grey, light brown-weathering fine-grained sandstone.
Kositcin, N., Munson, T.J., Whelan, J.A., 2017. Summary of results. Joint NTGS-GA geochronology project: greater McArthur Basin, July 2016-June 2017. Northern Territory Geological Survey Record, 2017-012, 64p.

represents a maximum age for deposition of the sedimentary precursor
Melville Bay Metamorphics
A sample of dense, massive, gt-bearing reddish-green quartzite was collected at an abandoned quarry, previously mapped as Drimmie Head Granite, located at the north-western coast of Drimmie Head Peninsula, in northern GOVE. The sample locality is an abandoned quarry of ca. 300x50 m size, and ca. 15m deep. Sample GV14SKR061B was taken from the main lithology present at that quarry, a very hard, dense, massive, reddish-green quartzite with up to cm-sized, subhedral garnet blasts. This quartzite shows locally a relic mm- to cm-thick original sedimentary layering, and dm-to sub-m thick bedding. It contains (mostly elongated) clasts of a fine-grained, grey meta-sandstone featuring sub-mm thin relic sedimentary layering. The quartzite is intruded by veins/dykes and small intrusions of gt-bearing granite (likely Drimmie Head Granite) which crosscuts and intrudes parallel to the original sedimentary bedding. It is thought that this quartzite may pertain to the Melville Bay Metamorphics, a succession of metasedimentary gneisses comprised dominantly of garnet-cordierite-biotite schistose gneiss with subordinate metapsammite. The Drimmie Head Granite, interpreted to intrude the Melville Bay Metamorphics, and indeed based on field relationships represents an area of crystallised in-situ melt derived from the metasedimentary succession during peak metamorphism, yielded SHRIMP U-Pb zircon dating of the crystallisation age of 1867 ± 12 Ma (Rawlings et al 1997). No previous dating has been undertaken on the Melville Bay Metamorphics.
Kositcin, N., Whelan, J.A., Reno, B.L., Kraus, S., Beyer, E.E., 2018. Summary of results: NTGS-GA geochronology project: Arnhem Province, July 2014-June 2016. Northern Territory Geological Survey Record, 2017-008, 37p.

maximum depositional age of the metasandstone
A sample of sericite-bearing metasandstone was collected from the base of Mount Grindall approximately 19 km southwest of Baniyala in BLUE MUD BAY. This area was previously mapped as undivided Bradshaw Complex (Rawlings et al 1997); high-grade rocks were tentatively correlated with the Melville Bay Metamorphics exposed in Gove based on lithological similarities. Based on new mapping, we interpret this metasandstone to be a locally metamorphosed equivalent to the Grindall Formation that crops out along the eastern flank of the Coast Range and on some islands in BLUE MUD BAY (Ahmad and Munson 2013). At the sample location, a succession of relatively flat lying to gently south-west dipping sericite-bearing metasandstone is intruded by granite and muscovite-tourmaline pegmatite; it overlies (unconformably?) steeply dipping biotite±garnet gneiss (NTGS BM15JAW033, collected 1.2 km southeast of BM15JAW028) though no direct contact was observed. All units are unconformably overlain by the Coast Range Sandstone of the McArthur Basin (Haines et al 1999). The sampled lithology comprises relatively homogeneous, fine-grained, altered sericite-bearing metasandstone, which is overprinted by a poorly developed spaced cleavage. Locally, granite intrudes both parallel to and cross-cuts interpreted original sedimentary layering.
Kositcin, N., Whelan, J.A., Reno, B.L., Kraus, S., Beyer, E.E., 2018. Summary of results: NTGS-GA geochronology project: Arnhem Province, July 2014-June 2016. Northern Territory Geological Survey Record, 2017-008, 37p.

The sample site is the eastern bank of a tributary of the Mitchell River (to the south), on the southern side of the main access road to the abandoned settlement of Groganville. The outcrop comprises moderately steeply dipping (50 degrees to the southeast), well-bedded, mainly thin- to medium-bedded sandstone and phyllitic mudstone, with some scattered thicker (to 50 cm) beds of sandstone. The analysed sample was collected from a sandstone bed in the lower part of the outcrop. Detrital muscovite is relatively common in hand specimen. The sandstone is grey to dark brownish grey, poorly sorted, very fine- to coarse-grained (0.1-0.6 mm, average 0.3 mm), with 20% matrix. Most grains are angular to subangular; a few are subrounded to rounded. Quartz (65-70%), mainly as monocrystalline grains, is the dominant framework mineral. The sandstone also contains minor plagioclase (generally unaltered to only slightly altered), K-feldspar (subordinate to plagioclase), detrital muscovite (and lesser biotite) flakes up to 3 mm, polycrystalline quartz, lithic fragments (mainly chert and mudstone), calcite, and accessory tourmaline and zircon (some relatively large grains). Most mica grains show undulose extinction and curved or bent cleavage planes. Biotite grains are little altered. The sampled outcrop forms part of an irregular, north-trending belt of rocks 100 km long and up to 6 km wide in the central-western Hodgkinson Province. It is distinguished from adjacent rock packages by pale pinkish-brown tones on ternary radiometric images. Prior to the acquisition of airborne radiometric data, this assemblage was included in informal subunit Dham, based mainly on lithological characteristics (e.g. Bultitude et al. 1998, 2000). The sample was selected for geochronology to compare its maximum depositional age and provenance spectrum with those yielded by sandstones elsewhere the Hodgkinson Formation, in particular, the revised informal subunit Dham to the east.
Kositcin, N., Bultitude, R.J., 2015. Summary of results - Joint GSQ-GA geochronology project: Hodgkinson Formation of the Mossman Orogen, 2014-2015. Queensland Geological Record, 2015/04, 72p.

The Corunna Conglomerate at Mount Allalone is dominated by medium- to coarse-grained, moderately sorted sandstone containing sub-rounded to rounded clasts of vein quartz, jasper and iron rock. It is usually massive, but contains some heavy mineral laminations which indicate that bedding dips moderately SW. The sandstone contains massive conglomerate horizons usually 1-2 m thick, which have gradational boundaries with the sandstone. Conglomerate is matrix-supported and poorly sorted, containing subrounded to rounded pebble- to cobble-sized clasts of vein quartz and jasper in a medium-grained sandy matrix. Sample R2145223 is a medium-grained massive sandstone containing sparse quartz and jasper pebbles. The hills SE of Mount Allalone contain the same lithologies of the Corunna Conglomerate, but the sandstone contains a foliation defined by strained quartz and a preferred alignment of clasts. Quartz veins intrude the sandstone subparallel to the foliation. Bedding dips moderately ENE, with the foliation dipping steeply E or W. Foliation intensity increases E towards the Allalone Fault Zone. In thin section, the rock displays a coarse-grained framework-supported clastic sedimentary texture, modified by metamorphism and alteration. Quartz occurs as 0.8-2 mm subrounded clastic grains with undulose extinction, and as large (3-5 mm) polycrystalline clasts with a granoblastic texture of strain-shadowed, foliated, anhedral quartz grains. Minor angular lithic fragments interpreted to be banded chert/BIF-type sediments are composed of uniformly fine-grained quartz and opaques, in places with banding of likely primary origin. Some contain intergrown fine-grained sericite. The matrix is composed of small equant anhedral quartz grains forming a granoblastic mosaic. Fine-grained sericite forms ragged patches and concentrations along thin trails, and as trails around the clastic grains. Opaques occur in trace amount in the sericite mats. Notably, the sericite mats are unfoliated.
Eastern foothills of Mount Allalone.
Jagodzinski, E.A., Werner, M., Curtis, S.O., Fabris, A., Pawley, M.J., Krapf, C.B.E., 2020. SHRIMP geochronology of the Mount Double area, Southern Gawler Ranges margin. Geological Survey of South Australia. Report Book, 2020/00006, 94p.

Choc-a-block Orthogneiss
Site DPCY031 is located 60 m east of Portland Road and 60 m North of Choc-a-bloc Creek in the Mangkuma Land Trust area. The sample is a medium to coarse-grained generally allotriomorphic, equigranular foliated biotite granitic gneiss and is currently mapped as a part of the Kintore Granite. It is comprised of coarse subhedral sericitised potassium feldspar (microcline), anhedral quartz, some recrystallised quartz (granoblastic, honeycomb texture in parts), foxy brown biotite (some altered to muscovite), fine muscovite with minor chlorite, zircon in green hornblende associated with muscovite patches and small red titanite crystals associated with amphibole muscovite alteration. It was sampled for SHRIMP U-Pb geochronology as its pronounced foliation contrasts markedly with other local, outcropping examples of the Kintore Granite.
GSQ site DPCY031 is located 60 m east of Portland Road and 60 m North of Choc-a-bloc Creek in the Mangkuma Land Trust area.

This sample was collected from a small road cutting on Horne Road, where the Coolanie Gneiss contains metasediment orientated parallel to the gneissic fabric in the Coolanie Gneiss, comprising layers of foliated metasediment . At the sample locality the Coolanie Gneiss is an equigranular, fine- to medium-grained, pinkish grey quartz-feldspar-muscovite granite gneiss with a fabric dipping moderately to the SE. The metasediment interlayered with the Coolanie Gneiss comprises two lithologies; foliated quartz-biotite-sillimanite schist and biotite-sillimanite-bearing quartzite. Mesoscale tight folds are visible in the schist layers. The sample submitted for geochronology contained both the quartzite and schist. The quartzite is fine-grained and composed of quartz, green biotite, sillimanite and plagioclase. Sillimanite occurs as euhedral to subhedral lath to needle-like crystals typically 300 µm in diameter, and defines the foliation in the quartzite. Quartz occurs as granoblastic aggregates with shadowy extinction 100-400 micron in diameter and is intergrown with small (100-200 micron) euhedral to subhedral grains of plagioclase with multiple twinning. Green biotite 100-300 micron in diameter occurs intergrown with sillimanite and with quartz and plagioclase. The metasediment is fine-grained and shares the same mineral composition as the quartzite but with greater proportions of biotite and sillimanite. It contains a strong schistose fabric defined by bioitite, sillimanite and granoblastic aggregates of quartz.
Jagodzinski, E.A., McAvaney, S.O., 2017. SHRIMP U-Pb geochronology data for northern Eyre Peninsula, 2014-2016. Geological Survey of South Australia. Report Book, 2016/00001, 79p.

five other grains dated from 223.80 � 223.04 Ma interpreted as inherited or detrital components.
Mount Nicholas Coal Measures
Fingal Tier DDH 82
Calver, C.R., Mantle, D.J., Crowley, J.L., Nicoll, R.S., 2021. Triassic coal measures, Tasmania: new U-Pb CA-TIMS ash bed dates and numerical calibration of palynostratigraphy. Australian Journal of Earth Sciences, 68(7), 1005-1016.

Mulgrave Formation
Sample 2306989/BB5603 was obtained from the easternmost lens of quartzose sandstone currently mapped as Mulgrave Formation in the Palmer River area. The analysed sample was collected from the ridge crest with abundant bouldery rubble on the southern side of the main road between Palmerville and Maytown, ~4.6 km east of Palmerville homestead. Bedding was not detected at this locality but the size of the boulders indicates the assemblage is thick bedded. The sandstone at the sample locality is extensively deformed and cut by numerous quartz veins up to ~2 cm thick (most < 6 mm). The sandstone is grey, medium-grained, and moderately to poorly sorted, with ~15-20% matrix. The average grainsize of the framework components is ~0.4 mm, with a range in grain sizes from 0.1 mm to 0.8 mm. Most grains are subangular to subrounded, with angular and, to a lesser extent, well-rounded grains forming a minor component of the framework population. Monocrystalline quartz is the main framework component (~80-85%), accompanied by traces of muscovite, biotite, zircon, tourmaline, opaque(s), feldspar (very rare), polycrystalline quartz (very rare), apatite, and lithic fragments (including chert, shale, very fine-grained schist). Tourmaline is a relatively common accessory mineral, generally as well-rounded grains. The matrix consists mainly of quartz and unidentified phyllosilicates. The latter have a well-developed preferred orientation and define a cleavage in the sandstone. The relative abundance of monocrystalline quartz and the almost total absence of feldspar grains distinguish this sandstone from the more common and widespread quartzofeldspathic sandstones of the Chillagoe and Hodgkinson Formations.
Kositcin, N., Lisitsin, V., Bultitude, R.J., Purdy, D.J., Brown, D.D., von Gnielinski, F.E., Dhnaram, C., 2016. Summary of results - Joint GSQ-GA geochronology project: Thomson Orogen, Mossman Orogen and Cape York, 2015-2016. Queensland Geological Record, 2016/09, 102p.

Manna Conglomerate
Medium- to very coarse-grained, poorly sorted, crystal-rich volcaniclastic sandstone dominated by tightly-packed, angular 1-2 mm crystals of glassy quartz, feldspar laths, and reddish-brown garnet (Eastlake, 2016). It has a very crystal-rich microstructure dominated by free crystals (whole and fragmented) and minor juvenile clasts. Free crystals exceed 65% of the rock, spanning quartz (20%), plagioclase (25%), biotite (15%) and garnet (5%). Quartz forms angular grains and slivers up to 4 mm. Plagioclase forms euhedral prisms and fragments up to 2 mm, partly altered to clay minerals and sericite. Bladed biotite is up to 2 mm and shows vague alignment, possibly related to syn-depositional compaction. Garnet up to 3 mm forms subequant crystals and angular fragments. Abundant irregular and wispy domains of microcrystalline quartz and chlorite are interpreted as recrystallised glass. The textural immaturity (and abundance) of free crystals and juvenile lithic clasts indicates a probable syn-eruptive origin for the rock. It is associated with massive sandstone and conglomerate to the E and NE, which preserve a subvertical, fine-grained cleavage subtly deflected around more competent clasts of well-sorted metamorphosed quartz sandstone and poorly-sorted metamorphosed quartz arenite. Warren et al. (1995) mapped this succession as Yiddah Formation on COOTAMUNDRA, but Lyons et al. (2000) mapped coarse-grained sedimentary rocks along strike to the north (on FORBES) as Manna Conglomerate. Eastlake (2016) regarded the Yiddah Formation on COOTAMUNDRA as two distinct units: (1) Late Silurian medial-fan turbidite facies deposits; and (2) Early Devonian high-energy alluvial fan facies deposits intercalated with minor pyroclastic deposits. The sampled unit was considered part of the latter, which Eastlake (2016) correlated with the earliest Devonian Gurragong Group (419.0 +/- 2.2 Ma and 415.4 +/- 2.8 Ma; Bodorkos et al., 2018).
Outcrop near the base of the W flank of Reefton Hills, about 2.4 km SW of Gidgingidginbung Pinnacle. The site is about 1 km N of Schlunkes Road, and about 16 km SE of Barmedman.
Geological Survey of New South Wales (GSNSW)
Bodorkos, S., Eastlake, M.A.S., Waltenberg, K., Bull, K.F., Gilmore, P.J., Campbell, L.M., Trigg, S.J., Blevin, P.L., Deyssing, L., Williams, B.J., 2021. New U-Pb SHRIMP zircon ages from the Lachlan Orogen, New South Wales: East Riverina Project, July 2016-June 2020. Geoscience Australia. Record, 2021/08, 321p.

Yiddah Formation
coarse grained sandstone
Bodorkos, S., Main, P.T., Bull, K.F., Campbell, L.M., Eastlake, M.A., Gilmore, P.J., Trigg, S.J., Waltenberg, K., 2018. New SHRIMP U-Pb zircon ages from the central Lachlan Orogen, New South Wales: Regional Mapping Projects, July 2015-June 2016. Geoscience Australia. Record, 2018/17, 100p.

Currawalla Shale
coarse grained sandstone
Bodorkos, S., Main, P.T., Bull, K.F., Campbell, L.M., Eastlake, M.A., Gilmore, P.J., Trigg, S.J., Waltenberg, K., 2018. New SHRIMP U-Pb zircon ages from the central Lachlan Orogen, New South Wales: Regional Mapping Projects, July 2015-June 2016. Geoscience Australia. Record, 2018/17, 100p.

Bonya Metamorphics
Sample HU14BLR672 is an andalusite-K-feldspar schist from the Bonya Metamorphics in the Bonya Hills. Andalusite, K-feldspar and sericite-after-cordierite pseudomorphs form cm-scale porphyroblasts with sub-mm inclusions of quartz and biotite. The matrix comprises 1-3 mm biotite intergrown with sillimanite and minor muscovite. Monazite (50-100 micron) occurs both as inclusions in andalusite and in the biotite-sillimanite matrix. Fine (10-20 micron) subrounded and elongate zircons occur throughout the rock, both in the biotite matrix and as inclusions in the andalusite and K-feldspar porphyroblasts.
Kositcin, N., Reno, B.L., Whelan, J.A., 2015. Summary of results. Joint NTGS-GA geochronology project: Arunta Region, July 2014-June 2015. Northern Territory Geological Survey Record, 2015-007, 26p.

maximum depositional age for this sample of the Perenti Metamorphics
Perenti Metamorphics
A sample of Perenti Metamorphics was collected from a ~20 m2 pavement outcrop approximately 1 km west of Tower Rock in southern Macdonald Downs. Sample HU15BLR957 is a migmatite that has mm-scale banding between biotite-bearing melanocratic layers and biotite-absent leucosomes. Melanosomes comprise sub-mm quartz, plagioclase, and K-feldspar, with up to 5 vol % sub-mm biotite, and 5–10 vol % 2–4 mm long sillimanite that is elongate in the direction of the main foliation. Leucocratic layers comprise elongate anhedral 1–4 mm poikiloblastic K-feldspar that includes sub-mm rounded cordierite, quartz, and plagioclase; and 1–2 mm anhedral quartz, cordierite, plagioclase, and sub-mm sillimanite that is perpendicular to the main gneissosity. All phases are stretched and elongate in the main foliation with the exception of sillimanite in the leucosomes.
Georgina Region
Kositcin, N., Reno, B.L., Beyer, E.E., 2018. Summary of results. Joint NTGS-GA geochronology project: Aileron Province, July 2015-June 2016. Northern Territory Geological Survey Record, 2018-005, 36p.

Drillhole FBD2 contains weakly to strongly foliated biotite-rich metasedimentary rocks. There are also narrow, coarse-grained, quartz-feldspar-rich pegmatite-like zones that have a transitional contact with the enclosing biotite-rich rock. In addition to weakly foliated zones there are also zones of moderate strain intensity, with shear bands that dissect the moderately altered sedimentary precursor. These shear bands are defined by muscovite and biotite. Sample R2322236 is representative of the foliated zones within the drillhole. It is a medium-grained rock comprising bands of quartz-plagioclase-K-feldspar-garnet interlayered with biotite, muscovite and sillimanite-rich bands. The banding of the quartzo-feldspathic domains and the mica-rich domains gives the rock the appearance of a pervasively foliated metagranite. The quartz in the quartzo-feldspathic microlithons comprises larger grains that are intergrown with feldspar and which are themselves partially to completely composed of subgrains. These subgrains have irregular subgrain boundaries due to dynamic recrystallisation. Undulose extinction of quartz subgrains is common. The plagioclase is almost completely altered to white mica. K-feldspar is less common that plagioclase, and where present shows undulose extinction and deformation of primary tartan twinning. Minor garnet is present and occurs as clusters of angular grains to around 500 microns in diameter. These garnet crystals may be fragments of earlier formed larger garnet crystals. None of these microgarnet crystals contain inclusions of other minerals. Biotite is green in colour and under cross polars shows a blue interference colours in places, which likely indicates the biotite is now partially, and in places completely, replaced by chlorite. Muscovite occurs intergrown with the biotite in the mica-rich microlithons and as a minor phase within the quartzo-feldspathic microlithons.
Jagodzinski, E.A., Reid, A., Gribbin, G., 2019. U-Pb geochronological data from the Fowler Domain, western Gawler Craton. Geological Survey of South Australia. Report Book, 2019/00018, 58p.

maximum depositional age for this sample of the Kanandra Metamorphics
Kanandra Metamorphics
Sample HU15BLR979 was collected approximately 6 km west of Dingo Bore in western Dneiper. The sample came from a 3 metre wide zone of migmatitic garnet-sillimanite pelitic gneiss interlayered at a 5-10 m scale with the Carmencita Granulite. Sillimanite is intergrown with biotite in mm to cm biotite-rich layers. Leucocratic layers comprise plagioclase-quartz-garnet. Garnet is mainly in the leucocratic layers of the rock, however a different phase of garnet also occurs as mm grains in the biotite-sillimanite layers.
Kositcin, N., Reno, B.L., Beyer, E.E., 2018. Summary of results. Joint NTGS-GA geochronology project: Aileron Province, July 2015-June 2016. Northern Territory Geological Survey Record, 2018-005, 36p.

Mulgrave Formation
This sample of quartzose sandstone was collected from a small gully in the headwaters of a tributary of the Palmer River. The sample site is on the southern side of a station track, ~300-400 m north of, and along strike from, the designated type area of the Mulgrave Formation (in Limestone Creek; Fawckner, 1981). The thin to medium-bedded sandstone forms mainly small, blocky rubble in the bed and bank of the gully. It is grey, fine-grained, and cut by scattered thin (generally < 6 mm thick, but range up to ~1.5 cm) quartz veins, as well as by numerous joints and fractures, which are commonly coated with brown, secondary iron oxide(s). The analysed sandstone has an average grainsize of ~0.15 mm. Framework grains are mainly angular to subrounded and moderately sorted. They are dominated by monocrystalline quartz (~80-85%), with plagioclase (~1-2%) as a minor component. Traces of muscovite, zircon, tourmaline, and opaque(s) were also detected. Most quartz grains show only slight-moderate undulose extinction. The matrix (~15-20%) consists mainly of quartz and unidentified phyllosilicates. The sandstone is moderately deformed and is cut by numerous fine, anastomosing solution seams, marked by irregular concentrations of dark, insoluble minerals and/or carbonaceous material.
Kositcin, N., Lisitsin, V., Bultitude, R.J., Purdy, D.J., Brown, D.D., von Gnielinski, F.E., Dhnaram, C., 2016. Summary of results - Joint GSQ-GA geochronology project: Thomson Orogen, Mossman Orogen and Cape York, 2015-2016. Queensland Geological Record, 2016/09, 102p.

Willandra Sandstone
Bodorkos, S., Main, P.T., Bull, K.F., Campbell, L.M., Eastlake, M.A., Gilmore, P.J., Trigg, S.J., Waltenberg, K., 2018. New SHRIMP U-Pb zircon ages from the central Lachlan Orogen, New South Wales: Regional Mapping Projects, July 2015-June 2016. Geoscience Australia. Record, 2018/17, 100p.

Date in Prot. Compilation of unknown origin. This reference uses unpublished data from D. Maidment
Kookaburra LKD100
Bagas, L., Bierlein, F.P., English, L., Anderson, J.A.C., Maidment, D.W., Huston, D.L., 2008. An example of a Palaeoproterozoic back-arc basin: petrology and geochemistry of the ca.1864Ma Stubbins Formation as an aid towards an improved understanding of the Granites-Tanami Orogen, Western Australia. Precambrian Research, 166(1-4), 168-184.

maximum depositional age for this sample of the Deep Bore Metamorphics
Deep Bore Metamorphics
Sample HU15EEB1004 is an orthopyroxene–garnet migmatite collected approximately 3 km southwest of Deep Bore in western Jinka. Melanocratic portions of the rock comprise mm-scale biotite–K-feldspar–plagioclase–quartz. Quartz and feldspar are subhedral and unaligned in foliation whereas biotite appears interstitial and weakly aligned to form a main foliation. Cm-scale leucocratic layers are subparallel to the main foliation and contain cm-scale orthopyroxene with mm-scale cordierite inclusions. The leucocratic matrix comprises 5–10 mm K-feldspar with micron-scale plagioclase lamellae and inclusions of sillimanite, 2–7 mm plagioclase, and quartz. K-feldspar–orthopyroxene grain boundaries are buffered by a micron-scale quartz mantle. Monazite and zircon occur both in the melanocratic portion of the rock and in the leucosome; however, neither were observed as inclusions in garnet.
Kositcin, N., Reno, B.L., Beyer, E.E., 2018. Summary of results. Joint NTGS-GA geochronology project: Aileron Province, July 2015-June 2016. Northern Territory Geological Survey Record, 2018-005, 36p.

Abercrombie Formation
Clements Formation
Fine-grained quartz-rich sandstone interbedded with sandy siltstone, formerly assigned to the Middle Ordovician Clements Formation of the Wagga Group (Campbell, 2015). However, a recent GSNSW review of stratigraphic nomenclature of Ordovician sedimentary rocks of the Lachlan Orogen across NSW and Victoria (Deyssing et al., 2018) unites fine-grained Early to Middle Ordovician sandstones and siltstones (including the Wagga Group), and the conformably overlying shale-dominated Bendoc Group, within an expanded Adaminaby Group as defined in the eastern Lachlan Orogen of SE NSW (e.g. Fitzherbert et al., 2017). In this amalgamation, pre-Bendoc Group sandstone- and siliciclastic siltstone-dominated successions (including the Clements Formation) are united within an expanded Abercrombie Formation (Deyssing et al., 2018). In thin section, this bedded, sericite-rich metamorphosed quartz arenite contains diffuse cross-beds. Bedding is distinguished by the presence of alternating sericite-rich and sericite-poor matrix domains, which are interpreted to reflect primary mud-rich and mud-poor beds, respectively. Detrital muscovite is common. Stratigraphic age control at this locality is provided by interbedded, thin chert horizons (ERIVLMC0156; Campbell, 2015), which yielded conodont elements of middle to late Darriwilian (Da2-4) age (Percival, 2016; c. 470 Ma to c. 461 Ma; Sadler et al., 2009). Percival (1999) documented conodonts from the Clements Formation on southwestern FORBES which indicate a middle to late Darriwilian age (Da2-4), indistinguishable from the stratigraphic age at this site (Campbell, 2015; Percival, 2016). This sample was selected for detrital zircon geochronology to determine a maximum age for deposition in an area where its true depositional age is biostratigraphically constrained, and to compare the detritral zircon provenance spectrum of the Abercrombie Formation with the overlying Currawalla Shale (ERIVLMC0377) and Willandra Sandstone (ERIVLMC0378).
Outcrop in the floor of the W part of Marble Quarry, which lies on the S side of Burley Griffin Way, 700 m WSW of its intersection with Olivers Road, and about 3.5 km SE of the locality of Quandary. Access to the quarry is via Olivers Road.

Drillhole MSDP13 was cored to 502.4 m at an inclination of 60 degrees W towards Mount Allalone. The hole tested a modest VTEM anomaly within a N-trending magnetic low associated with the Allalone Fault Zone, which has been interpreted as the boundary between the Nuyts and Coulta-Cleve domains. MSDP13 intersected 18.1 m of Cenozoic silty sand and gravels before penetrating metasandstone and variably mylonitised calc-silicate rock of the Corunna Conglomerate between 18.1-492.8 m, and a highly altered ?metasedimentary silicate rock between 492.8-502.4 m, tentatively correlated with the Hutchison Group. All lithologies display variable degrees of shearing and deformation. Sample R2138184 (142-144 m) is a fine- to medium-grained metamorphic rock with pervasive dull orange-red colour (hematite after K-feldspar). Minor thin, dull greenish grey, discontinuous fractures cut the rock. Veins containing quartz, chlorite and pyrite are evident. In thin section, the sample has a granoblastic metamorphic texture with faintly preserved framework-supported clastic sedimentary texture, overprinted by thin fractures and disseminated alteration. Quartz forms small anhedral grains in a granoblastic mosaic. Indistinct ovoid shapes of precursor clastic quartz grains are faintly distinguishable, each grain now occupied by a polycrystalline mosaic (recrystallised quartz) contributing to the wider mosaic. K-feldspar is less abundant than quartz, forming similarly sized grains with ovoid shape. All display a turbid dull reddish brown colour attributable to minute (micron-sized) reddish hematite specks. Small opaque grains are sparsely scattered through the rock. Small fine-grained ragged aggregates of chlorite, sericite and epidote are distributed between the quartz and K-feldspar grain sites. The rock is cut by discontinuous veinlets up to 1.5 mm wide, filled by granular quartz, anhedral K-feldspar grains, minor fine-grained chlorite, and small euhedral epidote.
Jagodzinski, E.A., Werner, M., Curtis, S.O., Fabris, A., Pawley, M.J., Krapf, C.B.E., 2020. SHRIMP geochronology of the Mount Double area, Southern Gawler Ranges margin. Geological Survey of South Australia. Report Book, 2020/00006, 94p.

feldspathic arenite
Lu, Y, Wingate, MTD, Kirkland, CL, Maidment, DW, Phillips, C and Hollis, JA 2016, 206101: feldspathic arenite, Deception Yard; Geochronology Record 1339: Geological Survey of Western Australia, 5p.

xenolith in Nummee Granodiorite
The Nummee Granodiorite contains a laterally continuous zone about 50 m wide and 3 m thick which contains xenoliths of a fine- to medium-grained, compositionally layered quartz-feldspar-biotite metamorphic rock. These felsic xenoliths contain compositional bands 2-4 mm wide defined by a variation in the proportions of quartz and feldspar versus biotite, as well as some dark grey magnetite-bearing laminae. The xenoliths experienced plastic deformation and contain layer-parallel as well as discordant granitic veins. A sample (R2145217) of these xenoliths was collected for geochronology to provide information about their origin (metasedimentary or meta-igneous), their age (magmatic crystallisation or maximum deposition) and the potential timing of deformation, and the nature of the basement into which the Nummee Granodiorite intruded. In thin section, the xenolith displays a granoblastic metamorphic texture with mineralogical banding and subparallel foliation, modified by overprinting alteration. Quartz and K-feldspar dominate the rock, forming equant anhedral grains (0.2-0.4 mm), but ranging up to 1 mm in minor discontinuous coarser-grained bands. Plagioclase is subequal in abundance to K-feldspar. Together, the quartz and feldspar form a granoblastic mosaic, and varied abundances define mineralogical banding 2-4 mm wide. K-feldspar is most abundant in the minor coarser-grained bands. Biotite forms small flakes and aggregates accompanied by small opaque grains, aligned in a weak metamorphic foliation subparallel to the mineralogical banding. Biotite is partially replaced by pale green chlorite. Zircon forms small blocky prismatic crystals displaying growth zoning. Trace pleochroic brown-green hornblende forms small anhedral crystals confined to one particular band, there is a single subhedral garnet (2 mm) at the boundary between a thinner quartz-rich band and a thicker K-feldspar-rich band, and trace epidote forms small grains in some of the chlorite aggregates.
~3 km S of Waulkinna Hill.
Jagodzinski, E.A., Werner, M., Curtis, S.O., Fabris, A., Pawley, M.J., Krapf, C.B.E., 2020. SHRIMP geochronology of the Mount Double area, Southern Gawler Ranges margin. Geological Survey of South Australia. Report Book, 2020/00006, 94p.

maximum depositional age The weighted mean 207Pb/206Pb age of 1934 +/- 47 Ma for the youngest three grains can be used as a maximum depositional age for the Grindall Formation.
Grindall Formation
A sample of fine-grained, yellowish-brown sandstone was collected from an extensive outcrop of interlayered unmetamorphosed sandstones, siltstones, and less frequent mudstones at the southern coast of Morgan Island, Blue Mud Bay. The sandstone forms massive, up to 3m thick, steeply dipping beds intercalated with much thinner (cm- to dm-thick), yellowish-beige and black siltstone and mudstone layers. Sedimentary structures like cross-bedding or load casts are infrequent but present. The usually very fine to fine grained sandstone may occasionally contain a small amount of slightly larger, sub-mm sized quartz grains. The sampled outcrop forms part of the southern limb of a large anticline. The outcrop forms part of the Grindall Formation, a siliciclastic sedimentary sequence believed to represent the protolith of at least part of the widespread granites in the eastern Arnhem Land area. The Melville Bay Metamorphics further north (northern Gove Peninsula) could be the metamorphosed equivalent of the Grindall Formation. At Morgan Island, the Grindall Formation is intruded by the Bukudal Granite, a medium grained, fayalite-cordierite-bearing granite.
Kositcin, N., Kraus, S., Whelan, J.A., 2016. Summary of results. Joint NTGS-GA SHRIMP geochronology project: Arnhem Province, July 2014-June 2015. Northern Territory Geological Survey Record, 2015-010, 25p.

Crow Formation
The Crow Formation (Rawlings et al., 2008) is a largely recessive unit that outcrops poorly throughout the western two-thirds of MOUNT DRUMMOND. The Crow Formation is composed of up to 2500 m of interbedded siltstone, sandstone, shale and lesser conglomerate (Rawlings et al., 2008). The sampled unit represents an ‘unnamed’ unit (Psos) as mapped on MOUNT DRUMMOND (Rawlings et al., 2008). The unit is 20-30 m thick at this location, is a prominent white, buff to creamy coloured feldspathic, locally friable, medium-grained sandstone, characterised by well-developed current lineations on bedding surfaces and reddish-purple oxidation spots. The Crow Formation (Rawlings et al., 2008) is a largely recessive unit that outcrops poorly throughout the western two-thirds of MOUNT DRUMMOND. The Crow Formation is composed of up to 2500 m of interbedded siltstone, sandstone, shale and lesser conglomerate (Rawlings et al., 2008). The sampled unit represents an ‘unnamed’ unit (Psos) as mapped on MOUNT DRUMMOND (Rawlings et al., 2008). The unit is 20-30 m thick at this location, is a prominent white, buff to creamy coloured feldspathic, locally friable, medium-grained sandstone, characterised by well-developed current lineations on bedding surfaces and reddish-purple oxidation spots. The sample site is ~ 2.2 km to the west of South Nicholson seismic line (GA17-SN05, Henson et al., 2018). The unit at this location strikes east-west (dipping 40º to the north), and crosses the GA17-SN05 seismic line orthogonally where it coincides with a strong north-dipping reflector in the seismic profiles. Rawlings et al. (2008) subdivided the Crow Formation into a number of broad facies subdivisions; the unnamed unit of the Crow Formation at this locality closely matches the ‘shallow-water facies’ of Rawlings et al. (2008) however, no ripple marks, mud-clasts or synaeresis cracks were observed.
Kositcin, N., Carson, C.J., 2019. New SHRIMP U-Pb zircon ages from the South Nicholson and Carrara Range regions, Northern Territory. Geoscience Australia. Record, 2019/09, 217p.

Wangalinji Member
The Wangalinji Member is the basal member of the Playford Formation (Wildcow Subgroup of the South Nicholson Group). Rawlings et al. (2008) describes the Wangalinji Member as comprising a lower, coarse-grained to granule and pebbly cross-bedded sandstone, overlain by interbedded siltstone and fine-grained sandstone, laminated shales and fine-grained lithic sandstone up to 390 m thick at the type section. Rare cherts and carbonates are also present. The member is reported as gradational and conformable with the overlying Top Lily Sandstone Member and unconformably overlies the top unit of the McNamara Group (the Widdallion Sandstone Member). At the sampling location, which lies on the type measured section described by Rawlings et al. (2008), the Wangalinji Member is a white- to cream-coloured, fine- to medium-grained feldspathic quartz sandstone with a characteristic ‘chalky’ gritty friable surface texture. Although the outcrop is rubbly, massive bedding as much as 1-2 m thickness is apparent, exhibiting small-scale (<1 m) cross-bedding indicating younging is up and to the north. Bedding dips moderately to the north (ca 15-20 degrees).
Kositcin, N., Carson, C.J., 2019. New SHRIMP U-Pb zircon ages from the South Nicholson and Carrara Range regions, Northern Territory. Geoscience Australia. Record, 2019/09, 217p.

No Mans Sandstone Member
The No Mans Sandstone Member is the uppermost member of the Playford Formation (Wildcow Subgroup of the South Nicholson Group) and is recognised only in the Mitchiebo region, where it outcrops in the northern part of a long ridge of outcrop, previously mapped as Constance Sandstone by Smith and Roberts (1963) and Sweet (1984). The member is 130 m thick at the type section and may thicken to as much as 200 m, further east in the Mitchiebo region. Exposure across the type section approaches 100% and consists mainly of coarse-grained sandstone with granule to pebble lags. Several fine-grained intervals also display similar coarse lags (Rawlings et al., 2008). The unit exhibits sharp, probably erosional, conformable contacts with both the underlying and overlying Top Lily Sandstone Member and Crow Formation, respectively (Rawlings et al., 2008). The sample location, which lies on the measured section described by Rawlings et al. (2008) is a white, slightly feldspathic, quartz sandstone, with large 1-10 m scale trough cross-bedding indicating the primary bedding (younging upright), dipping gently to the north. Outcrop is characterised by alternating 1-2 m scale recessive layers, with thinner (<1 m) more resistant quartz sandstone beds. The sampled unit is taken from the quartz sandstone component of the outcrop.

Drummond Formation
The Drummond Formation (Pmd, Rawlings et al., 2008) is the lowermost formation of the McNamara Group on MOUNT DRUMMOND. Rawlings et al. (2008) describe ‘four readily mapped units’ of the Drummond Formation (from the base, Pmd4 to top, Pmd1) dominated by lithic to quartzose sandstones, minor chert, claystone, siltstone and stromatolitic dolomitic rocks, deposited in a shallow marine-intertidal to fluvial depositional environment. The Drummond Formation unconformably overlies the Surprise Creek Formation but has a conformable contact with the overlying Brumby Formation (Rawlings et al., 2008). At the sample location, the Drummond Formation is a package of buff coloured alternating siltstone-sandstone beds. Symmetrical ripple marks are common on the upper surfaces of the sandstone beds with siltstone layers typically flaggy and fissile with minor cross bedding and ripple marks indicative of shallow water conditions. Bedding moderately dips (30-40°) to the northwest. The sample location immediately overlies, in apparent conformable contact, a finely laminated grey-buff dolostone (ca 20 m thick) with well-formed abundant columns of stromatolites. The underlying contact with the Surprise Creek Formation is concealed. The sampled layer is a recrystallised feldspathic quartz sandstone with minor euhedral muscovite flakes (<1%), and ~30-40 modal% feldspar. K-feldspar grains often retain tabular euhedral crystal morphology. Matrix quartz appears to have been recrystallised, with grain boundary migration and development of texturally equilibrated triple-point junctions. Apatite is a common accessory phase.
Kositcin, N., Carson, C.J., 2019. New SHRIMP U-Pb zircon ages from the South Nicholson and Carrara Range regions, Northern Territory. Geoscience Australia. Record, 2019/09, 217p.; Carson, C.J., Kositcin, N., Anderson, J.R., Henson, P.A., 2023, A revised Proterozoic tectono-stratigraphy of the South Nicholson region, Northern Territory, Australia - insights from SHRIMP U-Pb detrital zircon geochronology. Australian Journal of Earth Sciences, in press.

maximum age for deposition of the sedimentary precursor to the migmatitic gneiss
A sample of unnamed biotite gneiss was collected from the base of Mount Grindall approximately 19 km southwest of Baniyala in Blue Mud Bay. This area was previously mapped as undivided Bradshaw Complex (Rawlings et al 1997) and high-grade rocks were tentatively correlated with Melville Bay Metamorphics exposed in GOVE on the basis of lithological similarities. No previous dating has been undertaken in this area. At the sample location, platform and beach exposures comprise biotite gneiss which is locally garnet-sillimanite bearing and contains rare rafts or mega-selvages (up to 3 m wide) of cordierite-biotite ± sillimanite rock. The steep- to sub-vertical gneissosity is variably developed and appears to grade from true gneiss into weakly foliated granite. Muscovite-tourmaline pegmatite intrudes the gneiss and a shallowly south-southwest dipping, relatively low-grade metasedimentary succession which may unconformably overly the gneiss, though no direct contact was observed in the field. All units are unconformably overlain by the Coast Range Sandstone. The sampled lithology comprises relatively homogeneous, fine- to medium-grained biotite gneiss with rare garnet and biotite-sillimanite clots. Gneissic layering is characterised by centimetre scale biotite-rich and feldspar-rich bands. The gneissosity is overprinted by rare tight folds which plunge shallowly west. Rare quartzite xenolithis are aligned in gneissosity.
Kositcin, N., Whelan, J.A., Reno, B.L., Kraus, S., Beyer, E.E., 2018. Summary of results: NTGS-GA geochronology project: Arnhem Province, July 2014-June 2016. Northern Territory Geological Survey Record, 2017-008, 37p.

The analysed sample was collected from a medium-sized boulder at the base of a low cutting beside a track on the ridge, 230 m northeast of the Last Hit mine at Munburra. Exposure is relatively poor (mainly as scattered bouldery rubble). The sample is part of a relatively thick bed of dark grey sandstone, within an assemblage of mainly steeply dipping, thin- to medium-bedded sandstone and siltstone. This sample was analysed in order to extend the coverage of analysed samples from the formation, and to determine if it contains relatively young zircons similar to those previously detected in sandstones analysed from Cape Flattery (2165077/BB5491) and Nob Point (2165075/BB5486A) to the southeast (Kositcin et al., 2015b). In detail, the sandstone is very fine- to coarse-grained (0.1-1 mm, average 0.3 mm), and poorly sorted, with 20-25% very fine-grained matrix. Highly angular to subangular grains predominate, with a few subrounded grains. Monocrystalline quartz grains make up 65-70% of the rock. Most show variable degrees of undulose extinction, and a few are characterised by subgrain development. Feldspars are a minor framework component, with plagioclase much more abundant than rare K-feldspar. Most of the feldspar grains are little altered. Detrital muscovite is also a relatively common minor (3%) component. Most muscovite shows undulose extinction and some have curved or bent cleavage planes. Rare plagioclase has deformed twin planes. The sandstone also contains scarce polycrystalline quartz grains, sparse small angular to subangular lithic fragments, including discoidal to elongate mudstone (up to 1 cm), chert (up to 0.5 mm), felsic and intermediate-mafic volcanics, fine-grained muscovite schist, and subrounded quartzite (up to 0.6 mm), as well as accessory biotite (extensively replaced by chlorite), calcite, tourmaline and zircon. The matrix comprises mainly quartz, feldspar, sericite/muscovite, chlorite and calcite.
Kositcin, N., Bultitude, R.J., 2015. Summary of results - Joint GSQ-GA geochronology project: Hodgkinson Formation of the Mossman Orogen, 2014-2015. Queensland Geological Record, 2015/04, 72p.

Booda Formation
This sample was collected by Phil Gilmore of the Geological Survey of NSW, from outcrop from the southern slopes of the Oxley Range, approximately 30 km east-southeast of the town of Burke, northern NSW. The sample is a moderately weathered grey to beige, very fine to fine-grained, quartz-rich sandstone interbedded with siltstone from a steeply dipping sequence of Booda Formation. In the Oxley Range, the Booda Formation is unconformably overlain by relatively flat-lying conglomerates and sandstones of the Moira Formation and Mount Oxley Formation. This sample was collected to obtain a detrital zircon age spectrum for comparison with other samples of Booda Formation, and with samples of other sedimentary rocks of the southern Thomson Orogen and northern Lachlan Orogen.
Fraser, G.L., Kositcin, N., Thorne, J.P., 2019. New SHRIMP U-Pb zircon ages from the southern Thomson Orogen, northern Lachlan Orogen and Koonenberry Belt. Geoscience Australia. Record, 2019/16, 154p.

quartz metasandstone
Wingate, MTD, Kirkland, CL, Hollis, J and Phillips, C 2015, 206184: metasandstone, Palm Springs; Geochronology Record 1243: Geological Survey of Western Australia, 6p.

andalusite, staurolite, garnet, biotite muscovite schist
Kirkland, CL, Wingate, MTD, Hollis, J and Phillips, C 2015, 206187: pelitic schist, Tanami Road; Geochronology Record 1244: Geological Survey of Western Australia, 6p.

Wingate, MTD, Kirkland, CL, Hollis, J and Phillips, C 2015, 206121: metasandstone, Sophie Downs homestead; Geochronology Record 1240: Geological Survey of Western Australia, 6p

Age range from 2756-1725 Ma, dominant mode is 1850-1860 Ma, shoulders on main peaks at ca 1820 Ma and 1900 Ma, small clusters at 1924, 2025 and 2053 Ma plus scattered individual dates
Woodah Sandstone
A sample of medium- to coarse-grained sandstone of the Woodah Sandstone was collected from southwest Morgan Island, southwest BLANE. At the sample location the Woodah Sandstone unconformably overlies fayalite-biotite granite (interpreted to be Bukudal Granite) and a succession of interlayered sandstone and mudstone of the Grindall Formation. The Woodah Sandstone defines the base of the Alyangula Subgroup (Groote Eylandt Group) of the McArthur Basin and is interpreted to have been deposited in a braided fluvial environment (Ahmad et al 2013). The Woodah Sandstone is characterised by an up to two metre thick basal conglomerate which grades into a medium- to coarse-grained, moderately well-sorted, orange sandstone. Conglomerate is the dominant lithology and is poorly-sorted, comprising pebble-, cobble- and boulder-sized clasts that range from angular to sub-rounded, which are supported in a quartz-hematite matrix. Based on lithological similarities, clasts are interpreted to have been predominantly derived from the Grindall Formation, with subordinate quartz pebbles and rare granite clasts. The sampled lithology is a medium-grained orange sandstone dominated by quartz with rare feldspar grains, with cm-scale lamination and graded bedding fining upwards.
Arnhem Region
Kositcin, N., Whelan, J.A., Edgoose, C.J., 2015. Summary of results. Joint NTGS-GA geochronology project: McArthur Basin, July 2014-June 2015. Northern Territory Geological Survey Record, 2015-008, 13p.

represents a maximum age for deposition of the sedimentary precursor
Melville Bay Metamorphics
A sample of Melville Bay Metamorphics was taken from Wargarpunda Point to characterise the timing of metamorphism in the Arnhem Province. Sample GV14BLR010B is a garnet-biotite-plagioclase-quartz+/-cordierite granulite facies migmatite gneiss comprising metamorphosed interlayered mudstone-greywacke and sandstone. This particular sample is from a leucosome-dominated domain comprising intergrown, anhedral, 5-10 mm quartz-K-feldspar-plagioclase with up to 5% 1-5 mm anhedral elongate cordierite in equilibrium with the leucocratic matrix. Garnet up to 2-3 cm, interpreted as a peritectic phase that grew during the melt-forming reaction, occurs in the leucocratic matrix. Garnet includes sillimanite, cordierite, ilmenite, and pyrite, and is commonly mantled by a later phase of cordierite.

Evelyn Creek volcanics
The sample site is approximately 2.5 km SSW of the Milparinka-Hawker Gate Track, south of the Mount Poole Homestead, and 11.5 km from the track's intersection with the Silver City Highway at Milparinka. The metasedimentary outcrop is predominantly composed of metasiltstone and metasandstone. The outcrop is 15 metres wide and blocky and situated approximately 20 metres east of what has been identified as the Evelyn Creek volcanics by Greenfield et al. (2010). The sampled metasandstone is relatively fresh, exhibiting some weathering. It is fine-grained, foliated and exhibits some haematitic spotting. The sample was collected to assess the detrital zircon age spectrum of this sedimentary package, and for comparison with sedimentary rocks in the western Thomson Orogen, immediately to the east across the Olepoloko Fault.
Tibooburra Region
Fraser, G.L., Kositcin, N., Thorne, J.P., 2019. New SHRIMP U-Pb zircon ages from the southern Thomson Orogen, northern Lachlan Orogen and Koonenberry Belt. Geoscience Australia. Record, 2019/16, 154p.

One of the tectonic models proposed for the Hodgkinson Formation is that the formation represents an accretionary wedge/prism assemblage (e.g., Henderson and Donchak, 2013). In such a scenario the rocks could be expected to become younger to the east or northeast, essentially at right angles to the tectonic grain of the province. The headland at Nob Point comprises one of the most northeasterly outcrops of Hodgkinson Formation rocks. A sample was collected from this location to determine its maximum depositional age and to compare its provenance spectrum with the spectra of other samples analysed from the formation. The analysed sample was obtained from the wave-cut platform on the northern side of the headland at Nob Point. The assemblage in this area consists mainly of medium- to thick-bedded sandstone with scarce very thin beds of black, carbonaceous mudstone. Bedding is very well preserved. The rocks are folded into a large, open, shallow, southerly plunging anticline, with an axial-plane cleavage that is only visible locally (Bultitude and others, 1991). The sample is from a thick bed of dark grey, poorly sorted, medium- to coarse-grained sandstone (average grainsize ~0.6 mm) containing ~15% matrix. Highly angular to subangular grains predominate - a few are subrounded. Monocrystalline quartz grains make up ~70% of the rock. Plagioclase and K-feldspar are minor (total feldspar content ~10%) framework components. Some of the K-feldspar grains show cross-hatched twinning typical of microcline. Most of the feldspar grains are either fresh or only slightly altered. The rock also contains traces of detrital muscovite, polycrystalline quartz, and small lithic fragments (including mudstone, chert, mafic-felsic volcanics?, and quartzite or 'ribbon quartz'), as well as accessory zircon, tourmaline and strongly deformed, detrital biotite.
Kositcin, N., Bultitude, R.J., Purdy, D.J., Brown, D.D., Carr, P.A., Lisitsin, V., 2015. Summary of results. Joint GSQ-GA geochronology project: Kennedy Igneous Association, Mossman Orogen, Thomson Orogen and Iron Range Province, 2013-2014. Queensland Geological Record, 2015/03, 154p.

Mount Walker Member
The analysed sample was collected from a boulder of lithic sandstone beside the road to Mount Poverty. The sandstone is fine- to coarse-grained (average grainsize ~0.6 mm) and poorly sorted, with ~20% very fine-grained matrix. Most framework grains are subangular to subrounded. Lithic fragments, up to ~5 mm across, make up a significant part (~40%) of the rock. A range of rock types are represented, including porphyritic and aphyric mafic volcanics, quartzite, sandstone, siltstone, mudstone, and chert. The intraformational mudstone fragments are generally highly angular, whereas some of the mafic volcanic and quartzite clasts are subrounded to rounded. Quartz, mainly as monocrystalline grains, is the dominant (~30%) mineral fragment. Sparse polycrystalline quartz grains up to ~2 mm across and some plagioclase and K-feldspar grains are also present. Epidote is relatively common. Detrital muscovite was not detected. Very fine-grained biotite of metamorphic origin is common in the matrix.
Kositcin, N., Bultitude, R.J., Purdy, D.J., Brown, D.D., Carr, P.A., Lisitsin, V., 2015. Summary of results. Joint GSQ-GA geochronology project: Kennedy Igneous Association, Mossman Orogen, Thomson Orogen and Iron Range Province, 2013-2014. Queensland Geological Record, 2015/03, 154p.

Warrow Quartzite
This sample was taken from a band of fine- to medium-grained quartzite approximately 8 m thick, structurally interleaved within the Minbrie Gneiss. The quartzite contains a gneissic fabric steeply dipping to the ESE parallel to both the fabric in the Minbrie Gneiss and the contacts between the quartzite and Minbrie Gneiss. On the western edge of the quartzite band is a clinopyroxene-plagioclase-quartz calc-silicate band approximately 15 m thick, presumably part of the same sedimentary sequence. Like the quartzite the calc-silicate has a gneissic fabric steeply dipping to the ESE. The quartzite is dominantly composed of quartz, with minor feldspar (~5%) and biotite (~5%). The quartz is recrystallised, with grains up to 600 µm in diameter, often elongate parallel to the fabric, with shadowy extinction. Grains of perthitic potassium feldspar and potassium feldspar with cross-hatch twinning are up to 600 micron in diameter and plagioclase grains up to ~300 micron in diameter. Biotite grains are 100-300 micron in diameter, and define the fabric in the quartzite. Some biotite grains have developed a pronounced asymmetry.
Jagodzinski, E.A., McAvaney, S.O., 2017. SHRIMP U-Pb geochronology data for northern Eyre Peninsula, 2014-2016. Geological Survey of South Australia. Report Book, 2016/00001, 79p.

The Hodgkinson Formation at Cape Flattery forms wave-cut platforms, small headlands, and bouldery outcrops along the coast, where they are unconformably overlain by the middle Jurassic Dalrymple Sandstone. The sample was collected from a very thick bed of bluish grey, poorly sorted sandstone on the southern side of Campbells Cove, Cape Flattery. In thin section, the sandstone is medium- to coarse-grained (~0.8 mm) and poorly sorted, with ~10% matrix. Monocrystalline, subrounded to rounded quartz (~70%) is the dominant framework mineral, and is notable (compared to other Hodgkinson Formation sandstones) for the presence of numerous water-clear grains with straight to only slightly undulose extinction, straight or curved sides, and rounded corners, suggesting a volcanic source. Minor polycrystalline quartz, rutilated quartz and quartz with highly undulose extinction is also present. The sandstone contains minor calcite (~5%) representing fossil fragments. Lithic fragments (~10%) consist mainly of intraformational mudstone and siltstone, together with minor chert, ?metachert, quartzite, and rare intermediate-mafic ?volcanic clasts. The mudstone/siltstone fragments make up the largest clasts, at least some of which were deposited while only partly lithified. These wrap around other framework grains and commonly have lenticular, 'flame-like' terminations which infill narrow interstices between adjacent framework grains. Feldspar grains are scarce (<5%), especially compared to other Hodgkinson Formation sandstones examined in detail from farther south and southwest. Most are at least partly altered, untwinned (although some show polysynthetic or, more rarely, cross-hatched twinning), and are also significantly smaller than the average quartz grain. Rare small grains of detrital muscovite, commonly showing curved cleavage planes and/or highly undulose extinction are also present. Calcite is common in the matrix, as an interstitial infilling.
Kositcin, N., Bultitude, R.J., Purdy, D.J., Brown, D.D., Carr, P.A., Lisitsin, V., 2015. Summary of results. Joint GSQ-GA geochronology project: Kennedy Igneous Association, Mossman Orogen, Thomson Orogen and Iron Range Province, 2013-2014. Queensland Geological Record, 2015/03, 154p.

Barnard Metamorphics
The Barnard Metamorphics are the major component of the Barnard Province which occurs as a narrow, north-northwest trending, 70 km long sliver along the coast between Cairns and Innisfail. The Province is a distinct element of the Thomson Orogen and separated from the Greenvale and Charters Towers Provinces by the younger Hodgkinson Province. Deep seismic data (Korsch and others, 2012) indicates that the Greenvale and Barnard Provinces may be continuous at depth. The Barnard Metamorphics comprise multiply deformed arenite, phyllite, quartzite, greenstone, chlorite schist, quartz muscovite schist, muscovite-chlorite and biotite-muscovite schist, gneiss, migmatite and amphibolite (Bultitude and Champion, 2013). These reach greenschist- to upper amphibolite facies and may have been thrust up during later deformation of the Hunter Bowen Orogeny (Donchak, 1997), or emplaced by transcurrent faulting of material from the Charters Towers region (Henderson and others 2011). The Barnard Metamorphics are poorly exposed and outcrop is restricted to a series of headlands and islands. A sample from Narragon Beach near the southern extent of the unit yielded a metamorphic/recrystallisation age of 451.8 +/- 2.6 Ma (2132757/BB5433a, Kositcin and others, in prep.) and the unit is intruded by the Tam O'Shanter Granite (455.7 +/- 3.6 Ma, Bultitude and Champion, 2013). We chose to sample a lower-grade part of the unit in an attempt to clarify a maximum depositional age and purely detrital age spectrum. Sample 2165080/PCTH007 was obtained from the Bramston Beach area ~ 55 km south of Cairns. It was sampled from a small outcrop in thick scrub adjacent to the car park on the northern bank of Joyce Creek. The sample is a multiply deformed muscovite-biotite schist with ~80% quartz, ~15% biotite, and ~5% muscovite.

Yancannia Formation
The SHRIMP sample is half core from 174.15 to 175.10 m from drill hole BH2a, drilled by Pangaea Minerals Pty Ltd in 2011. The hole intersected metasedimentary rocks to 339m depth. Deeper in the hole, altered mafic to intermediate intrusive rocks extend to 427 m depth. The drill-hole is from a region of no surface exposure immediately east of the interpreted Olepoloko Fault, inferred as the western margin of the southern Thomson Orogen. The zone is interpreted as the southern extension of the Yancannia Formation, and this drilling provides a sample approximately 40 km southeast from surface outcrops of Yancannia Formation at Yancannia. The sample was collected from depth interval 174.15 to 175.10 m. The sampled rock is a greenish grey, medium- to fine-grained sandstone with a weak anastomosing foliation. The sampled interval was free of fractures or veins. Geochronology was conducted to obtain a detrital zircon age spectrum for comparison with metasedimentary rocks elsewhere in the southern Thomson Orogen.
Fraser, G.L., Kositcin, N., Thorne, J.P., 2019. New SHRIMP U-Pb zircon ages from the southern Thomson Orogen, northern Lachlan Orogen and Koonenberry Belt. Geoscience Australia. Record, 2019/16, 154p.

The sample site is located 35 km WSW of Lakeland Downs, on Bonney Glen station This subunit (Dhr9) forms a N-trending belt 15 km long and up to 5 km wide, distinguished from adjacent Hodgkinson Formation units by pronounced red tones on ternary radiometric images, reflecting relatively high potassium counts. It was sampled to determine if the distinctive radiometric signature reflects a significantly different provenance to the adjacent metasediments. The rocks in the area of the sample site form massive bouldery outcrops lacking bedding, and comprise grey to brown, poorly sorted, very coarse-grained sandstone, with minor interlayered mudstone, siltstone and fine-grained sandstone. Minor detrital muscovite is visible in most samples. Rounded quartz granules and pebbles (up to 3 cm), and/or angular clasts (up to 30 cm, but mostly <3 cm) of dark grey-black, fine-grained sandstone, siltstone, and mudstone are present in many outcrops. The sandstone clasts contain detrital muscovite and are well-rounded, whereas the mudstone fragments are angular. The rocks are generally strongly indurated and very competent, and are locally cut by sparse quartz veins up to ~30 cm thick. Framework grains (0.5-3.5 mm; average 1 mm) in the dated sample are angular to subangular. Quartz (80%) is the dominant framework mineral, mainly as monocrystalline grains. Fresh to little-altered plagioclase is slightly more abundant than K-feldspar. Angular lithic fragments (up to 3 mm) of fine-grained sandstone, siltstone, mudstone and rare chert, are also a minor component. The sample contains scattered flakes of detrital muscovite up to 2 mm, and the larger flakes are deformed, with bent cleavage planes and highly undulose extinction. Zircon, titanite, garnet and tourmaline are the main accessory minerals. Biotite is very rare, mainly preserved as relict grains within muscovite flakes and as small deformed detrital grains in interstices. The interstitial matrix component is relatively minor (<10%).

Drill-hole GSQ Tickalara 1 was drilled in 1986 by the Geological Survey of Queensland as a stratigraphic hole through the Eromanga Basin and penetrating underlying basement rocks in the western part of the southern Thomson Orogen. The sample analysed and reported here was collected from depth interval 1205.32-1207.32 metres. The rock is a grey-green, fine- to medium-grained quartzose metasandstone with a poorly developed cleavage defined by anastomosing chlorite. This sample was analysed to obtain a detrital zircon age spectrum for comparison with other samples of Warratta Group and Thomson beds in the Thomson Orogen.
GSQ Tickalara 1

Mulgrave Formation
The Mulgrave Formation is one of three elongate units that crop out adjacent to the Palmerville Fault along the western margin of the Hodgkinson Province/Mossman Orogen. These are considered distinct from, and older than, rock assemblages to the east in the main part of the Hodgkinson Province (Chillagoe Formation; Fawckner, 1981; Bultitude and Donchak, 1992; Bultitude and others, 1993). The Mulgrave Formation is dominated by fine-grained, quartz-rich greywacke and subordinate chert, hematitic mudstone and metabasalt (Bultitude and others, 1993). Existing age constraints are poor but it is considered Ordovician due to similarity with the Early Ordovician Judea Formation (Broken River Province) and its spatial association with the Late Ordovician Mountain Creek Conglomerate which may contain clasts of the Mulgrave Formation sandstone (Henderson and Donchak, 2013). The Mulgrave Formation was selected for geochronology to test correlation of these rocks with the Thomson Orogen rather than the Hodgkinson Province/Mossman Orogen. The sample site is along a ridge to the east of the Palmerville Road and consists of a series of resistant fine sandstone boulders. The sample is a grey to buff, fine-grained, matrix rich sandstone dominated by sub-rounded quartz grains.

The sample was collected from a thick, subvertical bed of dark grey sandstone on the eastern bank of Limestone Creek, on the downstream side of the road to Groganville (abandoned site). These rocks form part of subunit Dhr3, which consists of thin to medium-bedded sandstone, siltstone and mudstone, with scattered thicker (up to 50 cm thick) sandstone beds. It is extensively deformed, particularly the mudstone-rich parts, which show 'broken formation' development in places. The unit forms part of a belt up to 2.5 km wide extending for 40 km from south of the Mitchell River north-northwestwards towards the Palmer River. It was originally mapped as part of informal subunit Dham (Bultitude et al. 1998), but was subsequently delineated as a discrete subunit based on airborne radiometric imagery, where its distinctive dark tones on ternary radiometric images contrast markedly with the paler tones of the adjacent Hodgkinson Formation rocks. The average grainsize of the framework components is 0.5 mm, with most grains in the 0.1-0.6 mm range. A noteworthy feature is the presence of a minor component of larger grains in the 1-2 mm size range; polycrystalline quartz grains are relatively common in this population. Most framework grains are angular to subangular, with some subrounded to rounded grains. Quartz, as monocrystalline grains showing undulose extinction, is the dominant framework mineral (70%). The sandstone also contains minor plagioclase (generally only slightly sericitised), detrital muscovite and lesser biotite, scarce K-feldspar, polycrystalline quartz, and chlorite (at least some of which replaces biotite), rare calcite, and accessory zircon and tourmaline. Detrital micas show undulose extinction, and cleavage planes are commonly curved or bent. Lithic fragments (up to 1.5 mm) are scarce (<5%) and consist mainly of mudstone, siltstone, chert, and schist. Intraformational mudstone fragments form the largest clasts. Matrix components make up 15-20% of the rock.
Kositcin, N., Bultitude, R.J., 2015. Summary of results - Joint GSQ-GA geochronology project: Hodgkinson Formation of the Mossman Orogen, 2014-2015. Queensland Geological Record, 2015/04, 72p.

Kitoba Member
The sample is from a prominent outcrop of massive grey sandstone on the western side of the Burke Developmental Road, in the far west of the Hodgkinson Formation <200 m from the contact with the Chillagoe Formation. The Kitoba Member is distinguished by prominent thick, amalgamated intervals of coarse-grained sandstone, implying that the western Hodgkinson Province was more proximal to source than the central part. The Kitoba Member is the westernmost subunit in the Hodgkinson Formation. It is faulted against the Chillagoe Formation to the west and the OK Member to the east. The age of the member is unknown, but may be only slightly younger than (or even contemporaneous with) the Chillagoe Formation. The Kitoba Member is interpreted to represent the base of the Hodgkinson Formation in this part of the province, and was sampled for geochronology to determine if its maximum depositional age supports this interpretation. The sandstone contains a range of lithic clasts (including mudstone, siltstone, fine-grained sandstone, quartzite, muscovite schist, ribbon quartz, rare mafic volcanics and rare myrmekite) up to 3 cm across, and is poorly sorted (0.3-4 mm; average 1 mm), with 10% matrix. Framework clasts are angular to subangular and dominated by monocrystalline quartz (60%) and little-altered feldspar (15-20%) comprising plagioclase and K-feldspar in equal amounts. Some K-feldspar grains are coarse (up to 4 mm), with subhedral outlines and well-preserved crystal shapes, implying they have not been transported far. The sandstone contains minor lithic fragments (5%), micas (5%; mainly muscovite, but also biotite replaced by chlorite), polycrystalline quartz (3%), and accessory zircon, titanite and tourmaline. The matrix comprises quartz, feldspar, sericite, chlorite and epidote. Monocrystalline quartz invariably shows undulose extinction. Muscovite is deformed, with undulose extinction and curved or bent cleavage planes. Some plagioclase grains have curved twin planes.

Limbla Member
The Aralka Formation occurs in the northeast and, to a lesser extent, in the north-central parts of the Amadeus Basin. Originally the unit was included in the basal part of the Pertatataka Formation by Wells et al (1967). Based on correlations with other Neoproterozoic glacial successions, the age of the Aralka Formation has been estimated at about 600 Ma (Edgoose 2013). This is supported by Re-Os geochronology results from samples within the Wallara-1 drill hole that yielded ages of 658 +/- 5 Ma (Kendall and Creaser 2004) and 657.2 +/- 5.4 Ma (Kendall et al 2006). These ages constrain the timing of the underlying Sturtian glaciation (Areyonga Formation). The Aralka Formation overlies the Areyonga Formation and is unconformably overlain by the Olympic Formation (Preiss et al 1978). The Aralka Formation is dominated by poorly exposed to concealed siltstone and shales, but includes two better exposed members; 1) the lower Ringwood Member dominated by limestone and dolostone with distinctive stromatolites, and 2) the upper Limbla Member, a dominantly clastic unit, characterised by pebbly and sandy limestone and festoon-bedded sandstone. The sample collected for geochronology has been identified as Limbla Member and is a well-bedded, laminated quartz sandstone with occasional cross-bedding that forms a small ridge surrounded by aeolian plains near Halfway Dam. Maidment et al (2007) dated detrital zircons from a sample from the Limbla Member from the Hale River area in the northeastern part of the basin. Analyses gave a range of ages between ~2500 Ma and ~1080 Ma, with modes at ~1760 Ma, ~1580 Ma, ~1400 Ma, ~1180 Ma and ~1080 Ma, with the youngest detrital zircon at ~1070 Ma.

Cyclops Member
The Pertatataka Formation consists mainly of grey-green and purple-brown laminated micaceous siltstone and shale with thin interbeds of sandstone and limestone. Two members are restricted to the northeast of the basin: the lower Waldo Pedlar Member and the upper Cyclops Member (Wells et al 1967). The Cyclops Member lies near the top of the Pertatataka Formation, a short distance below the Julie Formation, and overlies thick shales of the main part of the Pertatataka Formation, which in turn overlie the Waldo Pedlar Member. The Cyclops Member contains flaggy sandstone and rhythmically thinly-bedded sandstone (Wells et al 1970). Previous SHRIMP U-Pb zircon analysis of detrital zircons from the Cyclops Member near Ross River Homestead yielded a spectrum dominated by ages between ~1900 Ma and ~1700 Ma with a secondary cluster at ~2500 Ma, and a spread of ages between ~1260 Ma and ~800 Ma (Maidment et al 2007). The youngest age of ~807 Ma is significantly older than the inferred depositional age of the unit of ~575 Ma (Maidment et al 2007). The sample collected for geochronology is a cyclic, rhythmically bedded, fine- to medium-grained quartz sandstone.

Hervey Group
Crystal-rich rhyolitic ignimbrite, comprising 15% euhedral creamy-white feldspar (1-3 mm) and 10% vitreous quartz (1-2 mm), in a purple-grey aphanitic groundmass (Eastlake, 2016). The rock contains elongate, wispy lenses (fiamme in the non-genetic sense of Bull and McPhie, 2007) ranging from 15 mm to several centimetres in length, oriented parallel to the fabric in the matrix to define eutaxitic texture (Eastlake, 2016). Fiamme cores are corroded and vuggaceous, but in less weathered specimens they preserve a porphyritic texture. Quartz typically forms subequant phenocrysts 0.5-2.5 mm across, with embayed margins and crystallographic faces partly developed on many crystals. Feldspar phenocrysts form euhedral prisms up to 2 mm long (and width:length up to 1:4), which are extensively altered to fine-grained sericite. The matrix is finely microcrystalline material with an irregular fabric (defined by aligned wispy components deformed around competent phenocrysts), interpreted as a dense welding texture. Fiamme preserve a delicate microstructure comprising a rim of radiating quartz crystals and an inner mosaic of more coarsely microcrystalline quartz, interpreted to result from intense devitrification of glassy components, such as densely welded/flattened pumice lapilli. The ignimbrite overlies an E-dipping package of medium-grained sublitharenite (Eastlake, 2016), which Warren et al. (1995) mapped as a sub-fan channel facies within the latest Silurian Yiddah Formation. However, Eastlake (2016) noted that the Curraburrama State Forest succession comprises immature thick-bedded lithic sandstone, pebbly lithic sandstone, and matrix-supported polymictic conglomerate, all featuring sedimentary structures indicating high water flow during deposition. These contrast starkly with the well-developed Bouma sequences within fine- to medium-grained quartz sandstone-dominated turbiditic successions elsewhere in the Yiddah Formation, especially near Barmedman (Eastlake, 2015).
Moderately-weathered angular outcrops of felsic volcanic rock near the top of a low, wooded rise in the SE corner of Curraburrama State Forest, about 500 m W of private property 'Ellersmore', and about 17 km NE of Barmedman.
Bodorkos, S., Eastlake, M.A.S., Waltenberg, K., Bull, K.F., Gilmore, P.J., Campbell, L.M., Trigg, S.J., Blevin, P.L., Deyssing, L., Williams, B.J., 2021. New U-Pb SHRIMP zircon ages from the Lachlan Orogen, New South Wales: East Riverina Project, July 2016-June 2020. Geoscience Australia. Record, 2021/08, 321p.

The Sefton Metamorphics are the only constituent of the Iron Range Province which forms part of the Coen Inlier in eastern Cape York. Outcrop in this area is deeply weathered and generally restricted to fairly small, isolated areas but it is likely that these rocks extend under cover of the Pascoe River and Carpentaria Basins and into the Coral Sea. To date, only large-scale geological mapping and reconnaissance geochronology has been completed. The Sefton Metamorphics dominantly comprise quartz-muscovite schist and also include a significant portion of hematite schist, magnetite schist, phyllite, calc-silicate, marble and greenstone (Willmott and others, 1973). These are metamorphosed to sub-greenschist to greenschist facies (locally amphibolite) and at least four deformations are identified (Blewett and others, 1997). Age constraints are: 1) intrusion of the Weymouth Granite, Kintore Granite, and Blue Mountains Adamellite at ~410-405 Ma (Black and others, 1992a, b), 2) identification of a sponge spicule and organic matter within recrystallised limestone at Bolt Head suggesting a Paleozoic age (Trail and others, 1969), and 3) U-Pb analysis of detrital zircon from a metaconglomerate yielding an imprecise maximum deposition age of ~1200 Ma from five grains between 1062 +/- 29 Ma and 1232 +/- 18 Ma (Blewett and others, 1998). Additionally, Cross and others (in prep.) recently presented a maximum depositional age of ~785 Ma from a drill core sample of the Sefton Metamorphics (2152166/SEF_a). Sample 2165082/PCTH010 is a medium-grained quartz-muscovite schist with accessory garnet. It was collected ~21 km south of Lockhart River township from a small boulder along an old track east of the main Nundah track in the vicinity of Mount Carter.

Halls Reward Metamorphics
The Halls Reward Metamorphics are considered part of the Thomson Orogen and are the easternmost unit in the Greenvale Province. They comprise amphibolite facies mica schist, quartzite, biotite-muscovite gneiss and metamorphosed mafic and ultramafic units (Fergusson and others, 2013). The Halls Reward Metamorphics were previously thought to represent Proterozoic crust juxtaposed against Cambrian to Ordovician rocks of the Greenvale Province (Arnold and Rubenach, 1976; Withnall, 1989; Withnall and others, 1991). However, Nishiya and others (2003) dated metamorphism at ~510-500 Ma. These workers also chemically dated detrital zircons, revealing populations in the 600-500 Ma age range and around 1000 Ma. The imprecision of these data led us to sample the Halls Reward Metamorphics for U-Pb SHRIMP geochronology. The sample selected is a strongly foliated quartz-muscovite schist from a cutting in the disused Greenvale railway loop ~4.5 km northwest of Greenvale township. The sample site is ~1. 5 km southwest and along strike from the samples of Nishiya and others (2003).

Nebine Metamorphics
The sample analysed here was collected from depth interval of 589.8-590.0 metres (Moreton Plains drillhole) and consists of weathered, pale green, fine-grained quartz rich siltstone. In thin section the sample consists predominantly of quartz with subordinate white mica and chlorite, and accessory opaque minerals, tourmaline and zircon. The sample exhibits a weak cleavage, axial planar to small fold hinges defined by clay and opaque minerals, and appears to have experienced lower metamorphic grade than the schists intersected in GSQ Eulo 1, approximately 130 km to the NW of the Moreton Plains drillhole. Geochronology was conducted to produce a detrital zircon age spectrum for this siltstone for comparison with other samples from the Nebine Metamorphics and with other metasedimentary samples of the southern Thomson Orogen and northern Lachlan Orogen.
Moreton Plains

This sample was collected from an outcrop in a belt of Hodgkinson Formation rocks assigned to informal subunit Dham. This belt forms a major, northerly trending zone, 15-20 km wide and 100 km long, distinguished from nearby subunits to the west by paler tones on ternary radiometric images. The belt was sampled for zircon geochronology to determine if it contains relatively young zircons (anticipated from its easterly position), and to compare the resultant detrital zircon age spectrum with the spectra yielded by samples collected from other subunits in the formation. The sample was collected from a thick, subvertical sandstone bed exposed in the bed of a tributary of the Mitchell River, on the downstream side of the crossing of the main road to Groganville (abandoned site). The sandstone contains scattered grains of detrital muscovite, and is interlayered with an assemblage of mainly thin- to medium-bedded, finer grained sandstone, siltstone and mudstone. The sandstone is dark grey, fine- to coarse-grained (0.1-0.6 mm, average 0.3 mm), and poorly sorted, with 15-20% matrix. Most grains are angular to subangular, with some subrounded to rounded grains. Quartz, as monocrystalline grains, is the dominant framework mineral (70%). Many of the grains are characterised by only slightly undulose extinction (in contrast to many of the other sandstones analysed from the formation) and a few have subhedral outlines, suggesting a volcanic origin. The sandstone also contains minor (8%) plagioclase (generally only slightly altered), K-feldspar, detrital muscovite and polycrystalline quartz grains, and accessory chlorite, zircon, and tourmaline. Detrital muscovite shows undulose extinction, and cleavage planes are commonly curved or bent. The sandstone also contains minor calcite, and sparse (2-3%), small (up to 0.6 mm) clasts of very fine-grained schist, chert, mafic volcanics, mudstone, ribbon quartz, and quartzite. Sericite is common in the matrix.

Thomson beds
Drill-hole GSQ Bulloo 1 was drilled by the Queensland Department of Mines in 1986 as a stratigraphic hole through the southwestern part of the Eromanga Basin. The total depth of the hole was 631 metres, with the final ~40 metres intersecting basement rocks beneath the Eromanga Basin, consisting of folded, metamorphosed sandstone, with a steep axial planar cleavage and subvertical quartz veins (Murray, 1994). The sample analysed here was collected from the depth interval 612.14 to 621.90 metres and is a fine- to medium-grained sandstone, with lesser siltstone intervals, with a steeply-dipping weak cleavage. This sample was analysed to obtain a detrital zircon age spectrum for comparison with other samples interpreted to represent the Thomson beds.
GSQ Bulloo1

Budginigi Ignimbrite
Bodorkos, S., Bull, K.F., Campbell, L.M., Eastlake, M.A., Gilmore, P.J., Trigg, S.J., 2016. New SHRIMP U-Pb ages from the central Lachlan Orogen and New England Orogen, New South Wales: July 2014-June 2015. Geoscience Australia. Record, 2016/21, 101p.

Yarraden Schist
The unit that this sample (2306983/DBCY075) was collected from was originally mapped as Sefton Metamorphics by Willmott et al. (1973). It occurs as a screen associated with the intrusion of an un-named granite of the Early Devonian, Flyspeck Supersuite. Outcrop at the sample site is poor and consists of schist with veins of pegmatite and gneiss and occurs as subcrop. Sample 2306983/DBCY075 is a light-brown medium-grained quartz biotite sillimanite schist. The dominant fabric is defined by recrystallised quartz and bands of coarse biotite and muscovite with fine acicular sillimanite. Hematite staining is common at grain boundaries.
Fine grained quartz muscovite schist from south of the William Thomson Range.

Youngest detrital age component Age range 1979-1943 Ma.
Nourlangie Schist
The Nourlangie Schist in the eastern Pine Creek Orogen is likely to be the metamorphosed equivalent of the Wildman Siltstone (Mount Partridge Group) which outcrops to the west. It appears to overlie the Cahill Formation, and is transitional into the Myra Falls Metamorphics (Needham 1988). The Nourlangie Schist is intruded by the Jim Jim Granite and Oenpelli Dolerite, and unconformably overlain by the Katherine River Group. This sample of garnet-biotite-sillimanite-staurolite-quartz schist was obtained from drillcore stored at Cameco Australia Pty Ltd's core farm (drillhole ALG002) at Myra Camp. Monazite is also present in the schistose fabric.

Drillhole UOD Weribone 1 hole penetrated the Surat Basin and underlying Thomson Orogen to a total depth of 2436.90 metres where it bottomed out in metamorphosed rocks interpreted to be Timbury Hills Formation (Union Oil Development Corporation, 1963). The sample selected for geochronology was collected from the depth interval of 2382.6 to 2383.0 metres and is a grey to green, fine-grained, quartz-rich sandstone, with a well-developed cleavage parallel to the lithological layering. SHRIMP analyses of detrital zircons from this sample of sandstone were aimed at characterising the zircon provenance of sedimentary rocks in this region.

Pioneer Sandstone
The Pioneer Sandstone is a shallow marine to tidal medium- to coarse-grained, feldspathic and arkosic sandstone confined to the central-northern Amadeus Basin. The lower part of the formation is characterised by planar laminations with some cross-laminations, whereas the upper part is dolomitic with tabular cross-beds and also contains discrete dolostone. The top of the formation is often characterised by an irregular erosional surface containing scours filled with pink dolostone with columnar stromatolites (Edgoose 2013). The age of the Pioneer Sandstone is only constrained by its stratigraphic position: Walter et al (1995) equated it with the Olympic Formation, largely based on the 'cap dolostone' units in the two successions. The sample was collected from an area mapped as Olympic Formation on ALICE SPRINGS, where an unusually thick (~710 m) sequence of siltstone, sandstone and diamictite capped by a stromatolite-bearing carbonate (informally named the Undoolya Sequence) is interpreted as being stratigraphically above the Bitter Springs Formation and below the Pertatataka Formation, in a small basin created by salt tectonics in the underlying Bitter Springs Formation (Kennedy 1993). Preliminary NTGS investigations indicate that this sequence is probably a locally thickened succession of Pioneer Sandstone unconformably overlying the Johnnys Creek Member of the Bitter Springs Formation, and overlain by the Pertatataka Formation. A ~10 cm thick medium-grained sandstone bed (Unit III of the Undoolya Sequence; Kennedy 1993) was sampled, within a sequence of siltstone that is directly overlain by a stromatolite-bearing cap dolostone near the top of the succession. In thin section, the sample is dominated by interlocking angular to subrounded 100-500 um quartz grains. Angular to rounded rock fragments (300-500 um) make up ~2% of the sample and include pyroxene, micrite, glauconite and chalcedony chert. The matrix comprises micro-quartz, Fe-oxides and lesser calcite.

The sample is unaltered, dominantly fine- to medium-grained sandstone, with lesser siltstone and minor sedimentary breccia.In thin section quartz is dominant and comprises angular to sub-rounded grains, generally smaller than 600 um. Feldspar (plagioclase?) grains exhibit distinctive twinning in cross-polarised light. Other identified minerals include: muscovite, opaque minerals (including pyrite), apatite and zircon. The groundmass consists of quartz and possible feldspar +/- clay minerals.
Lewis, C.J., Cayley, R.A., Duncan, R.J., Schofield, A., Taylor, D.H., 2016. New SHRIMP U-Pb zircon ages from the Stavely region, western Victoria: July 2014-June 2016. Geoscience Australia. Record, 2016/27, 203p.

four other grains dated from 219.50 � 218.19 Ma interpreted as inherited or detrital components.
Mount Nicholas Coal Measures
Fingal Tier DDH 82
Calver, C.R., Mantle, D.J., Crowley, J.L., Nicoll, R.S., 2021. Triassic coal measures, Tasmania: new U-Pb CA-TIMS ash bed dates and numerical calibration of palynostratigraphy. Australian Journal of Earth Sciences, 68(7), 1005-1016.

Youngest zircon population - one or two grains
Utopia Quartzite
The sample is a silicified and recrystallised pale grey quartzite, with poorly preserved bedding and rare cross-bedding lamination, and is typical of the Utopia Quartzite. Bedding thickness is approximately 15 cm, but is locally in the range 5-30 cm. Rarely preserved cross-beds give occasional younging directions. The sample was taken from the northern limb of a large, reclined synclinal/anticlinal fold of Utopia Quartzite and underlying Ledan Schist. The contact between the two units is conformable on the regional scale, but local disconformities and shearing may be present as a result of a weak decollement between the quartzite and metapsammite of the Ledan Schist. The sample was taken away from the contact, well within the Utopia Quartzite.
Hollis, J.A., Beyer, E.E., Whelan, J.A., Kemp, A.I.S., Schersten, A., Greig, A., 2010. Summary of results. NTGS laser U-Pb and Hf geochronology project: Pine Creek Orogen, Murphy Inlier, McArthur Basin and Arunta Region, July 2007-May 2008. Northern Territory Geological Survey Record, 2010-001, 142p.

Gaylad Sandstone
The Gaylad Sandstone is confined to the northeast of the basin, and was originally correlated with the Olympic-Pioneer succession (Preiss et al 1978). Freeman et al (1991) recognised that the Gaylad Sandstone conformably underlies the Pertatataka Formation and overlies the Olympic Formation-Pioneer Sandstone succession in a regional unconformity. The formation consists of quartz sandstone, lithic sandstone, subarkose, orthoconglomerate and rare debris-flow diamictite, and has been interpreted to have been deposited in the interval 700-600 Ma based on regional correlations with the underlying Olympic Formation (Freeman et al 1991). Recent work by Kennedy and Christie-Blick (2011) may call into question the age and stratigraphic associations of the Gaylad Sandstone; it may be an equivalent to the upper part of the Olympic-Pioneer succession. Another interpretation is that the Gaylad Sandstone may be a localised, proximal equivalent of the Waldo Pedlar Member of the Pertatataka Formation (P. Haines, pers comm 2013). A well bedded, slightly feldspathic and silicified quartz sandstone was collected from the type section of the Gaylad Sandstone, as defined by Field (1991). In thin section, the sample is predominantly interlocking quartz crystals 400-500 um in size. Subrounded to rounded feldspars up to 500 um comprise ~25% of the rock, with another 2% composed of elongate mica to 0.1 cm and subrounded to rounded rock fragments. The small proportion of matrix is mostly Fe-oxide crystals.

Glenthompson Sandstone
The sample is a medium-grained sandstone with disseminated and veined pyrite throughout. In thin section mineral assemblages are seen to be quartz (dominant) and minor plagioclase in a fine grained matrix of quartz, sericite and clays. Accessory sulphide minerals are present. Quartz grains are sub-angular to rounded, and vary from unstrained (i.e. of igneous origin) to recrystallised (i.e. sourced from metamorphic basement-like rocks). This suggests a mixed provenance, possibly involving a combination of proximal and distal sedimentary sources. No clear bedding features are identified.
Lewis, C.J., Taylor, D.H., Cayley, R.A., Schofield, A., Skladzien, P.B., 2015. New SHRIMP U-Pb zircon ages from the Stavely region, western Victoria: July 2013-June 2014. Geoscience Australia. Record, 2015/26, 62p.

One-third of core segment: 4019'0" to 4019'4".
Mallabie 1
Fraser, G.L., Neumann, N.L., 2016. Under the Nullarbor: New SHRIMP U-Pb zircon ages from the Coompana, Madura and Albany-Fraser Provinces, and Officer Basin, western South Australia and eastern Western Australia. Geoscience Australia. Record, 2016/16, 70p.

Sample 2179753 was collected from diamond core from the interval 659.03-659.13 m (2152'2-2152'6). This interval of the Mallabie 1 core overlies a thick interval between 3006'-3956' that is dominated by amygdaloidal basalts of unknown age. This basaltic interval separates the stratigraphic level of sample 2179753 from the lower stratigraphic level of sample 2179751. The sample is a reddish-brown, relatively fine-grained, massive, quartz-rich sandstone. The rock is clearly bedded, consisting of alternating coarser and finer grained bands of similar composition. In thin-section the rock is dominated by a grain-supported framework of subrounded and subequant quartz grains. Microcline and carbonate cement forms <5% of the rock. There is no evidence of a tectonic fabric. The sample was analysed to provide a detrital zircon age spectrum for comparison with (i) the Mallabie 1 arkose (sample 2179751) from a deeper level within the same drillhole, and (ii) possible correlative sedimentary units within the Officer Basin.
Mallabie 1
Fraser, G.L., Neumann, N.L., 2016. Under the Nullarbor: New SHRIMP U-Pb zircon ages from the Coompana, Madura and Albany-Fraser Provinces, and Officer Basin, western South Australia and eastern Western Australia. Geoscience Australia. Record, 2016/16, 70p.

Baledmund Formation
The unit sampled is a massive, granule- to pebble-sized, texturally immature volcaniclastic sandstone of the Baledmund Formation, which is part of the Kopyje Group within the Cobar Supergroup. Volcaniclastic sandstone and agglomerate are relatively minor constituents of the Baledmund Formation, which is dominated by siltstone and lesser quartz arenite and limestone (MacRae, 1987). Brachiopod faunas in the lower part of the formation are referable to the latest Silurian-earliest Devonian Rietzella capricornae zone (MacRae, 1987; Burton et al., 2012), and limestone-hosted conodonts at stratigraphically higher levels are referable to the Early Devonian Pedavis pesavis zone (Pickett, 1980). The Baledmund Formation interfingers with the Florida Volcanics, which have previously yielded a U-Pb SHRIMP zircon date of 421.7 +/- 2.3 Ma (Black, 2005). The textural immaturity of this volcaniclastic sandstone is consistent with rapid sedimentary reworking of a proximal volcanic source. It is therefore likely that the maximum age for deposition of this part of the Baledmund Formation (defined by dating the youngest detrital zircon component) will approximate the true depositional age of the volcaniclastic sandstone. This texturally immature volcaniclastic sandstone contains abundant but very unevenly distributed crystals (up to 5.5 mm long) and angular fragments (down to 0.1 mm) of quartz, perthitic alkali feldspar and bent plagioclase, as well as rare mica laths up to 1.5 mm long (now replaced by secondary muscovite). Parts of the rock are noticeably crystal-poor and may be pumice fragments or coherent volcanic clasts, although the pervasive alteration (quartz-sericite with minor chlorite and carbonate) has diffused any boundaries. Small non-welded relict shards were observed in the finely microcrystalline presumed matrix, and well-formed zircon crystals are conspicuous.
Bodorkos, S., Blevin, P.L., Eastlake, M.A., Downes, P.M., Campbell, L.M., Gilmore, P.J., Hughes, K.S., Parker, P.J., Trigg, S.J., 2015. New SHRIMP U-Pb zircon ages from the central and eastern Lachlan Orogen, New South Wales: July 2013-June 2014. Geoscience Australia. Record, 2015/02, 158p.

Max depositional age. These eight 238U/206Pb ages span the range 504-490 Ma, and their weighted mean age of 498.7 +/- 5.8 Ma is interpreted to define a maximum depositional age for this sample of the Puddler Creek Formation.
Puddler Creek Formation
The Puddler Creek Formation is the lowest exposed unit of the Seventy Mile Range Group in the Charters Towers Province. It is up to 9 km thick and comprises a gently dipping sequence of micaceous, continentally derived siltstone, sandstone and greywacke (Henderson, 1986; Berry and others, 1992). Felsic volcanic rocks that overly the Puddler Creek Formation (Mount Windsor Volcanics) have a magmatic U-Pb (SHRIMP) date of 479 +/- 5 Ma (Perkins and others, 1993) while graptolites towards the top of the Seventy Mile Range Group may be as young as Chewtonian (~472 Ma) or Darriwilian (~469 Ma) (see Henderson and Hutton, 2013). The Puddler Creek Formation was selected for geochronology to determine a maximum depositional age for the base of the Seventy Mile Range Group and to compare detrital spectra with the remainder of the Thomson Orogen. The sample selected (2165194/PCTH019) is a mottled brown to buff, medium-grained, well sorted sublithic sandstone with sub-angular quartz, fine-grained metasedimentary lithic fragments and minor detrital muscovite. It was collected from Britannia Station ~33 km south of Charters Towers in a road cutting along Bluff Road.
Charters Towers Region
Kositcin, N., Bultitude, R.J., Purdy, D.J., Brown, D.D., Carr, P.A., Lisitsin, V., 2015. Summary of results. Joint GSQ-GA geochronology project: Kennedy Igneous Association, Mossman Orogen, Thomson Orogen and Iron Range Province, 2013-2014. Queensland Geological Record, 2015/03, 154p.; Purdy, D.J., Cross, A.J., Brown, D.D., Carr, P.A., Armstrong, R.A., 2016. New constraints on the origin and evolution of the Thomson Orogen and links with central Australia from isotopic studies of detrital zircons. Gondwana Research, 39, 41-56.

Glenroy Formation
The sample analysed here was collected from depth interval 473.35-473.65 metres (Weilmoringle 1A drillhole) and consists of a sand-rich interval within an otherwise mudstone-dominated sedimentary package. The rock is a light-green, fine-grained sandstone. Bedding is moderately inclined relative to the drill-hole axis, and the sample exhibits a weak cleavage. No previous radiometric age measurements have been made on samples from the Glenroy Formation. Geochronology was conducted to produce a detrital zircon age spectrum for this sandstone for comparison with other metasedimentary samples of the southern Thomson Orogen and northern Lachlan Orogen.
Weilmoringle 1A

Youngest detrital zircon component. The maximum depositional age for this sample can be defined by the youngest grain which has a 238U/206Pb age of 626 +/- 16 Ma (2sigma)
GSQ Machattie 1 was drilled in 1987 by the Geological Survey of Queensland to a depth of 1179.6 m. The hole penetrated 1121 m of Eromanga Basin sediments before reaching indurated sedimentary basement (Williams, 1988). The basement interval comprises 58.5 m of moderately dipping (~45 degrees), fine- to medium-grained quartz-feldspar-lithic sandstone and pebbly sandstone, planar laminated dark grey shale and minor thin interbeds of siltstone. The basement rocks have experienced significant metamorphism resulting in a weakly granoblastic texture (Murray, 1994). Sample 2165195/TH1500 is a metasandstone comprised of 45% recrystallised and elongate quartz, 20% muscovite as fine-grained and tabular crystals and minor proportions of subrounded (detrital) plagioclase which exhibits incipient mica development, biotite, calcite, alkali feldspar, subrounded clasts of chert and zircons. The rock has a weakly granoblastic texture, and a foliation defined by elongate quartz. The basement in GSQ Machattie 1 is considered part of the same sedimentary package as basement in HPP Goleburra 1. These occupy a similar structural location adjacent to the North Australian Craton and are termed the Machattie beds (Carr and others, 2014). Basement in HPP Goleburra 1 has a maximum depositional age of 1074 +/- 23 Ma and a detrital age spectrum dominated by a main peak at ~1180 Ma (Brown and others, 2014; Cross and others, in prep.).
GSQ Machattie 1
Kositcin, N., Bultitude, R.J., Purdy, D.J., Brown, D.D., Carr, P.A., Lisitsin, V., 2015. Summary of results. Joint GSQ-GA geochronology project: Kennedy Igneous Association, Mossman Orogen, Thomson Orogen and Iron Range Province, 2013-2014. Queensland Geological Record, 2015/03, 154p.; Purdy, D.J., Cross, A.J., Brown, D.D., Carr, P.A., Armstrong, R.A., 2016. New constraints on the origin and evolution of the Thomson Orogen and links with central Australia from isotopic studies of detrital zircons. Gondwana Research, 39, 41-56.

Sample PCTH013 is from the central part of the Sefton Metamorphics in the Iron Range area. It was collected from a small outcrop in the bank of the West Claudie River ~12 km northwest of Lockhart River township. The sample is a weathered quartz-muscovite schist.

Drill-hole Yarrallee 1 penetrated the Eromanga Basin and underlying Thomson metamorphic basement to a total depth of 687.32 metres (Planet Exploration Pty Ltd, 1970). The Yarrallee 1 drill-hole intersects the Gumbalara zone, a very large area of low and relatively bland magnetic response essentially paralleling the southern margin of the Thomson Orogen. The sample selected for geochronology was collected from the depth interval of 684.3 to 687.2 metres and is a grey to green, finely-bedded, very fine-grained pelitic siltstone, showing soft sediment and (polyphase) tectonic folding. Quartz veining is present and sulfide mineralisation occurs in some fractures and bedding planes. SHRIMP analysis of this sample will provide an indication of the maximum depositional age of this unit, and a zircon provenance age spectrum, for comparison with other regional metasedimentary rocks.
Yarralee 1

Timbury Hills Formation
Drill-hole AAO Glenroy 1 penetrated the Surat Basin and underlying Thomson Orogen to a total depth of 1197.6 metres where it bottomed out in metamorphosed rocks interpreted to be Timbury Hills Formation (Mines Administration PTY LTD, 1965). The sample selected for geochronology was collected from the depth interval of 1194.97 to 1195.88 metres and is a grey to green, massive, medium-grained quartzite with no obvious bedding. SHRIMP analyses of detrital zircons from this sample were aimed at characterising zircon provenance, for comparison with regional sedimentary rocks from farther west in the Thomson Orogen, and from the Lachlan Orogen.
Glenroy 1

Thomson beds
Drillhole GSQ Thargomindah was drilled by the Queensland Department of Mines as a stratigraphic hole through the south-western part of the Eromanga Basin. The hole was drilled to a depth of 1092 metres, with the final ~36 metres interpreted to represent deformed metasedimentary basement rocks of the Thomson Orogen. The sample analysed here was collected from the depth interval 1071.55 to 1072.35 metres, and consists of fine- to medium-grained quartz sandstone, with a weak bedding-parallel cleavage that dips at ~45 degrees. The sample was analysed to obtain a detrital zircon age spectrum for comparison with similar sedimentary rocks from GSQ Eromanga 1 and GSQ Quilpie 1.
GSQ Thargomindah

The sample was taken from drill-hole TDH6 at a depth interval of 855.54 to 856.50 metres. The drill-hole is situated very close to, and slightly south of, a prominent northeast-southwest-trending magnetic feature known as the Culgoa Shear Zone in the south-eastern Thomson Orogen (Doublier et al., 2018). The Culgoa Shear Zone defines the northern margin of a sedimentary depocentre of poorly-constrained age, known as the Paka Tank Trough. The sample analysed here is interpreted to come from the Paka Tank Trough. The sample is a fine-grained, grey-green, relatively massive rock with intermittent elongate quartz lenses aligned in a strong preferred orientation oblique to the core. At the time of core inspection the rock was interpreted as a possible volcanic, with the quartz lenses representing an original porphyritic texture. The rock was sampled for U-Pb geochronology to provide an age for volcanic activity and a stratigraphic age constraint on the surrounding sedimentary sequence. Subsequent petrographic observations suggest the rock is more likely a volcaniclastic sandstone rather than a lava.
Nimrod TDH6

The sample is a weakly altered, slightly weathered, massive, fine- to medium-grained silty-sandstone with minor pyrite (~ 0.5%) veinlets throughout. In thin section quartz is dominant, comprising angular to rounded, generally fine grains (< 250 um). Other identified minerals include: detrital feldspar (plagioclase?), zircon, muscovite, and opaque minerals. It is uncertain if the mica is of detrital or diagenic origin. Minor chlorite alteration is noted, particularly around grain boundaries. Grains appear to be cemented with a combination of quartz and clay minerals.

could also be an earlier metamorphic event
A sample of calc-silicate rock was collected from the southern Melville Bay area, approximately 12 km west of Gove Airport in Gove. Meta-carbonate rocks have previously been identified as xenoliths in S-type granites and as bands of calc-silicate rock in the Melville Bay Metamorphics to the north (Plumb and Roberts 1992; Rawlings et al 1997); calc-silicate xenoliths are also described in undivided Bradshaw Complex in the south (Rawlings et al 1997). New mapping has identified exposures of calc-silicate rock and marble in the southern Melville Bay area. The sampled outcrop comprises pavements and blocky exposures of calc-silicate rock and impure marble. The calc-silicate rock is fine- to medium-grained and contains diopside and garnet (both phases occurring as porphyroblasts up to 1 cm diameter), quartz, wollastonite, calcite, and minor biotite (<2%). Compositional layering is typically centimetre-scale with alternating diopside-rich and poor layers. The metacarbonate succession is intruded by garnet–cordierite– biotite granite of the Drimmie Head Granite. It also occurs locally as xenoliths within the granite.
Arnhem Region

Irindina Gneiss
The sample site is part of an area of low-grade metasedimentary rocks north and northeast of Pinnacle Well in the Mallee Bore area. Regional magnetic data indicates that the site is situated at the eastern limit of the Irindina Province, which is characterised by marked magnetic trends and associated faults. Rocks in the area lack the strong, generally west-trending strain overprint of higher-grade rocks of the Irindina Province. However, as in the higher-grade rocks, folds in these lower-grade rocks are simple and upright. Approximately 2 km to the west-northwest are the migmatitic rocks of the Irindina Province. On the basis of the preceding points, the sample was dated to determine if it was part of the Irindina Province, or whether it was a section of a fault-emplaced basement metasedimentary succession on the margins of the Irindina Province. The sample site comprises a finely interlayered succession of metapsammitic, quartz-rich metapsammitic and andalusite-rich metapelitic rocks; the quartzitic metapsammitic rock was sampled for geochronology. The succession is tightly folded on upright folds with steeply plunging east-southeast fold axes. No visible melts were observed and the metapelitic and metapsammitic rocks are comprised of quartz-feldspar-biotite +/- andalusite. The metamorphic grade is amphibolite facies and these rocks are interpreted to be lower-grade equivalents of granulite-facies, migmatitic quartz-feldspar-biotite-garnet +/- sillimanite metapelitic and metapsammitic rocks of the Irindina Province exposed further to the west.
Hollis, J.A., Beyer, E.E., Whelan, J.A., Kemp, A.I.S., Schersten, A., Greig, A., 2010. Summary of results. NTGS laser U-Pb and Hf geochronology project: Pine Creek Orogen, Murphy Inlier, McArthur Basin and Arunta Region, July 2007-May 2008. Northern Territory Geological Survey Record, 2010-001, 142p.

OK Member
The OK Member is a narrow, chert-dominated belt on the eastern margin of the Kitoba Member, near the western margin of the Hodgkinson Province. It is also structurally intercalated with Kitoba Member rocks to the north, and therefore might be expected to form one of the oldest parts of the Hodgkinson Formation. However, radiolaria with three-bladed spines, which are considered characteristic of late Devonian (or younger) strata, occur in chert samples collected from the southeastern part of the member (24 km SE of Bellevue homestead), so an interlayered sandstone was sampled for analysis, to check the radiolarian age and to compare the detrital-zircon provenance spectrum with those from sandstones elsewhere in the Hodgkinson Formation. The sample was collected on the southern bank of the Mitchell River, from a thick sandstone bed interlayered with strongly cleaved, thin-bedded siltstone and dark grey mudstone. The sandstone is strongly indurated, very competent, relatively coarse-grained and poorly sorted, with 15-20% matrix. Framework grains are 0.3-3 mm (average 0.6 mm), mostly angular to subangular (some are subrounded), and dominated by monocrystalline quartz (65%). The sandstone also contains sparse polycrystalline quartz up to 1 mm; feldspar (8%) comprising plagioclase (partly replaced by sericite +/- calcite) and turbid K-feldspar (extensively replaced by clay minerals) in roughly equal amounts; lithic fragments up to 2 mm (5%) comprising fine-grained quartzite, ribbon quartz, mudstone, and rare feldspathic quartzite, mafic volcanics and chert; detrital muscovite up to 1 mm (2-3%); rare, small biotite (largely replaced by chlorite); interstitial calcite, and zircon. Widespread evidence for deformation and compaction includes: ubiquitous undulose extinction (and some incipient subgrain development) in monocrystalline quartz; undulose extinction and bent cleavage planes in muscovite, and curved twin planes or fracturing in some plagioclase grains.

Bonya Metamorphics
A sample of fine-grained, equigranular metasandstone was collected from an area of interlayered metamorphosed siltstones, sandstones and calcareous sedimentary rocks, previously mapped as Bonya Schist, approximately 3 km north of Bonya Bore, in central JERVOIS RANGE. At the sample location, the lithologies have been strongly folded, and a variably developed axial planar slaty cleavage is apparent in the more micaceous rocks. The sampled unit comprises equigranular quartz with a minor feldspar component; fine laminations up to 5 cm apart are defined by magnetite. No sedimentary structures were observed at this location. Directly to the east of this package of folded rocks is a mylonitised felsic intrusive rock, previously interpreted to be a porphyry intruding the Bonya Schist. SHRIMP U-Pb zircon dating of this felsic intrusive rock yielded a magmatic crystallisation age of 1778 +/- 5 Ma (Hussey and Claoue-Long 2003, unpublished data). Due to the pervasive degree of deformation along the contact it is unclear if the metasedimentary rocks unconformably overlie the felsic intrusion or were intruded themselves. It is also unclear what the relationships are between the metasandstone and porphyroblastic cordierite schist to the east and west, the dominant lithology of the Bonya Schist.
Kositcin, N., Beyer, E.E., Whelan, J.A., 2014. Summary of results. Joint NTGS-GA geochronology project: Arunta Region, July 2013-June 2014. Northern Territory Geological Survey Record, 2014-008, 30p.

two other grains dated (218.35 and 218.34 Ma) interpreted as containing inherited or detrital components
Mount Nicholas Coal Measures
tuffaceous volcaniclastic rock
GY27 Gray
Calver, C.R., Mantle, D.J., Crowley, J.L., Nicoll, R.S., 2021. Triassic coal measures, Tasmania: new U-Pb CA-TIMS ash bed dates and numerical calibration of palynostratigraphy. Australian Journal of Earth Sciences, 68(7), 1005-1016.

Johnnys Creek Member
The Bitter Springs Formation comprises three members (Gillen, Loves Creek and Johnnys Creek members) consisting of dolostone, limestone, siltstone, sandstone, halite, evaporites, and a basaltic unit. Its depositional age is currently constrained to approximately 820 Ma based on geochemical correlation of the basalt with the Amata Dolerite in the Musgrave Province. The Amata Dolerite forms part of a continental flood basalt province and has been dated at ca 800 Ma (Sm-Nd whole rock + clinopyroxene + plagioclase, Zhao and McCulloch 1993; Zhao et al 1994), and 824 +/- 4 Ma (U-Pb baddeleyite; unpublished data quoted in Glikson et al 1996). The Johnnys Creek Member lies at the top of the Bitter Springs Formation and is widespread in the central-western portion of the Amadeus Basin. The unit consists of red-beds, dolomitic limestone or dolostone with siltstone and stromatolitic beds with occasional sandstone beds. The unit contains distinctive microfossils and stromatolites that have been used to correlate the unit across the basin (Edgoose 2013), with the lower part of the Buldya Group in the Officer Basin and with the lower part of the Burra Group of the Adelaide Geosyncline (Grey et al 2011, Hill et al 2011). Basalts in the Bitter Springs Formation have been confirmed as comprising a single unit near the top of the Johnnys Creek Member (Edgoose and Normington 2014).The Johnnys Creek Member is disconformably overlain by the Areyonga Formation and this is typically marked by the development of a rubbly, fractured regolith palaeosurface (Lindsay 1993). The sample was collected from a 3-4 m bed of fine-grained sandy dolostone within dolostone and dolomitic siltstone beds. In thin section, quartz grains are subangular to rounded and range between 100 um and 500 um in length, with rounded rock fragments to 500 um. Fine-grained Fe-oxide minerals and carbonate minerals dominate the matrix, with lesser micro-quartz, chalcedony chert and rhombic dolomite crystals.

The OON Mirintu 1 drillhole is situated in the western part of the southern Thomson Orogen, approximately 110 km WNW of Hungerford in southwestern Queensland. The sample analysed here was collected from depth interval 901.75-902.75 metres and consists of a pale cream-coloured bleached quartzite interbedded with pale green phyllite. This sample was analysed to characterise the detrital zircon signature of sedimentary rocks from this part of the Gumbalara Zone, and for comparison with other (meta)sedimentary rocks of the southern Thomson Orogen.
Mirintu 1

Thomson beds
GSQ Quilpie 1 was drilled by the Geological Survey of Queensland in 1983. The drill hole penetrated the Eromanga Basin and underlying Thomson Orogen to a total depth of 1214.19 metres where it bottomed out in metamorphic basement. The sample selected for geochronology was collected from the depth interval of 1203.3 to 1205.5 metres and is a grey, fine-grained, chloritic metasiltstone. It contains sparse, thin (to 2 mm) quartz veins some of which contain pyrite. Disseminated euhedral pyrite crystals up to 4 mm in size are also present. SHRIMP analyses of detrital zircons from this sample will provide an indication of the maximum depositional age of this unit, and a zircon provenance age spectrum. It will also provide age constraints to aid interpretation of the seismic line BMR84-14, and provide regional context for comparison with regional sedimentary rocks in the Thomson Orogen and the Lachlan Orogen.
GSQ Quilpie 1

This sample was collected from a tributary of Limestone Creek, on the northern side of an access track on Bellevue station. The outcrop consists of moderately deformed, steeply dipping (70 degrees to the east-northeast), thin- to medium-bedded sandstone and mudstone. Relatively coarse detrital muscovite is visible in hand specimen. The sandstone is poorly sorted, and fine- to coarse-grained (0.1-0.7 mm; average 0.4 mm). Most grains are angular to subangular. Quartz, as monocrystalline grains showing variable degrees of undulose extinction, is the dominant framework mineral (65-70%). Other framework components include minor feldspar (5%; with plagioclase dominant over K-feldspar), detrital muscovite (3%), sparse lithic fragments (chert, mudstone, vein quartz, intermediate-mafic volcanics), and accessory calcite, tourmaline, and zircon. Most feldspar grains are little altered; however, a few are extensively replaced by sericite and calcite. Matrix components are abundant (25%) and comprise quartz, sericite, chlorite, feldspar, and calcite. Muscovite shows undulose extinction and cleavage planes in the larger grains are curved or bent. Mudstone fragments commonly have wispy terminations that project into interstices between more competent framework grains such as quartz and feldspar. The sandstone is also cut by very thin, irregular, anastomosing dissolution seams (marked by concentrations of opaque, amorphous material), which probably represent a penetrative deformation fabric. The outcrop is part of an irregular north-trending belt 70 km long and up to 10 km wide ( informal subunit Dhr5) which adjoins subunit Dhr6 to the east, and is distinguished from the latter by distinctly darker (pink to maroon) tones on ternary radiometric images. The subunit was sampled for geochronology to extend the coverage of analysed samples in the Hodgkinson Formation, and to compare the detrital-zircon age spectrum with those yielded by sandstones elsewhere in the Hodgkinson Formation.

Easter Monday Formation
Well-exposed outcrops of Easter Monday Formation occur on low rounded hills, mostly west of the township of Tibooburra. The sample was collected on Mt Sturt Station from outcrop on the eastern side of a topographic peak. This peak is approximately 350 metres east from a farm track; the sample site cannot be seen from the track. The sample is a homogeneous, massive, fine- to medium-grained metasandstone exhibiting planar fabric development, compositional banding and hematitic spotting. The Easter Monday Formation is dominated by metamudstone and metasandstone but also includes minor tuffaceous beds that provide the only depositional age constraint (497.2 +/- 2.6 Ma; Black, 2006). The Easter Monday Formation is intruded by the Tibooburra Granodiorite, a well exposed, I-type granodiorite emplaced at 420.6 +/- 3.3 Ma (Black, 2007; Vickery, 2010). Elsewhere, small granodiorite exposures (Dynamite Tank Granodiorite, Creswells Tank Granodiorite) and various felsic dykes are also grouped into the Tibooburra Suite and have similar ages (i.e. c. 420-427 Ma, Vickery, 2010). The Easter Monday Formation is regarded as part of the Warratta Group which is interpreted to postdate the Delamerian Orogeny (c. 504-498 Ma; Greenfield et al., 2010), and to unconformably overlie the early to mid-Cambrian Teltawongee Group. The sample location lies to the east of the Olepoloko Fault, thus lying within the Thomson Orogen. Detrital zircons from this sample near the western margin of the Thomson Orogen were analysed for comparison with zircon provenance spectra from sedimentary rocks elsewhere in the Thomson Orogen, and from the Koonenberry Belt immediately to the west.
Tibooburra Region

Warnes Sandstone Member
The Warnes Sandstone Member forms a massive unit within the Kurinelli Sandstone, near the base of the Ooradidgee Group. A unit of silicified quartz sandstone was sampled from the Murray Downs Dome ca 30 km E of Murray Downs homestead.

Lennee Creek Formation
Taken from silicified quartz sandstone at the base of the Lennee Creek Formation 3 km east of Coulters Waterhole. This is the stratigraphically highest part of the Hatches Creek Group that can be sampled within current land access constraints. Overlying the Lennee Creek Formation is a continuation of clastic sedimentation in the Canulgerra Sandstone, Vaddingella Formation and Yaddanilla Sandstone, before the sequence disappears under Cenozoic cover. The Lennee Creek Formation is interpreted as a transgressive sequence deepening upwards from shelf sands at the base into deeper water shelf sediments.

Pacoota Sandstone
The Pacoota Sandstone is a thick (~750 m) siliciclastic succession constituting the basal unit of the Larapinta Group in the northern Amadeus Basin. Shergold et al (1991) defined four informal sequences, in ascending stratigraphic order: (1) a transgressive succession featuring age-diagnostic body fossils plus trace fossil-bearing sandstones of the Skolithos ichnofacies; (2) a tidal and storm-dominated sequence comprising bioturbated sandstones with well-developed Skolithos but lacking age-diagnostic fossils; (3) a series of rapid transgressions comprising phosphatic and glauconitic clastic sediments; and (4) the most areally extensive, and probably disconformable on (3), storm and tidally dominated sandstones rich in ichnofossils but impoverished in body fossils. Sample LA19VJN122 was collected ~100 km W of Kings Canyon. It is an orange-red, medium-bedded, moderately-sorted, medium- to coarse-grained, silicified feldspathic sandstone with clay cement. Some poorly-preserved Skolithos were observed, but no body fossils, and the outcrop could not be assigned to any of the four informal sequences of Shergold et al (1991). The Pacoota Sandstone is unconformable on the late Cambrian Goyder Formation and is probably unconformably overlain by the mid Lower Ordovician Horn Valley Siltstone (Edgoose 2013). A diverse fossil fauna constrains its age to 508-480 Ma (Shergold et al 1991). SHRIMP U-Pb analysis of detrital zircons from the Pacoota Sandstone at Ellery Creek (HERMANNSBURG) and Ross River Gorge (ALICE SPRINGS) yielded maximum depositional ages of 496 +/- 6 Ma (Buick et al 2005) and 540 +/- 7 Ma (Maidment 2005) respectively; the former agrees well with stratigraphic constraints from fossil evidence. LA-ICPMS U-Pb analysis of detrital zircons in HENBURY gave a maximum depositional age of 522 +/- 5 Ma (Normington et al 2018). Sample LA19VJN122 was collected to further constrain the age of deposition, and lateral variations in provenance for the unit to the west.
Beyer, E.E., Verdel, C., Normington, V.J., Magee, C.W., 2020. Summary of results. Joint NTGS-GA geochronology project: western Amadeus Basin, July 2019-June 2020. Northern Territory Geological Survey Record, 2020-006, 43p.

Mereenie Sandstone
The Mereenie Sandstone is widely distributed across the Amadeus Basin, and has a maximum thickness of 1000 m. It is a white to pale brown sandstone consisting of well-rounded, well-sorted, fine- to medium-grained quartz. The lower part of the unit has trough, long angle and wedge-shaped cross beds; the upper part has trough cross beds indicative of aeolian deposition. Ripple marks are common throughout. Vertical burrows, similar to Skolithos, can be found in the lower part of the succession; horizontal burrows and arthropod tracks have also been identified. Sample LA19VJN151 is from an isolated exposure ~100 km NNW of Kings Canyon. It is a buff to orange, thinly bedded, well-sorted, medium-grained feldspathic sandstone with clay cement. The outcrop is finely laminated and planar bedded with some asymmetric ripples. There are no fossils in the Mereenie Sandstone; however, trackways in the Mereenie Sandstone at Kings Canyon are referable to the ichnogenus Diplichnites and imply a late Silurian to Lower Devonian age (Gouramanis and McLoughlin 2016). In the western Amadeus Basin, the Mereenie Sandstone conformably overlies the Late Ordovician Carmichael Sandstone; in the east, it is regionally unconformable on older units of the Larapinta Group or on the Cambrian Pertaoorrta Group. It underlies the Late Devonian Parke Siltstone (west) or Hermannsburg Sandstone (east) of the Pertnjara Group, although this relationship appears locally unconformable. SHRIMP U-Pb detrital zircon analysis of Mereenie Sandstone from Ellery Creek (HERMANNSBURG) revealed abundant ca 0.5-0.6 Ga zircons and no grains younger than ca 0.49 Ga (Maidment 2005). Normington et al (2018, 2019) obtained similar results, with maximum depositional ages of 486 +/- 5 Ma and 505 +/- 5 Ma for the Mereenie Sandstone in HENBURY using the LA-ICPMS U-Pb method. Sample LA19VJN151 was chosen to identify any lateral changes in maximum depositional age and provenance from east to west.
Beyer, E.E., Verdel, C., Normington, V.J., Magee, C.W., 2020. Summary of results. Joint NTGS-GA geochronology project: western Amadeus Basin, July 2019-June 2020. Northern Territory Geological Survey Record, 2020-006, 43p.

Cleland Sandstone
The Cleland Sandstone forms prominent strike ridges and low rounded hills in the western Amadeus Basin (Idirriki Sub-basin) and appears to thicken northward (Wells et al 1970). The maximum thickness is estimated at 1100 m in the area north of the Glen Edith Hills (MOUNT LIEBIG). Ranford (1969) included the unit in the Pertaoorrta Group. The Cleland Sandstone is typically red to purple, thin to medium-bedded, medium to coarse-grained, feldspathic, micaceous sandstone. Pebble beds and scattered pebbles occur throughout but are most common near the base. Overall, there is a coarsening of the unit towards the west. Sample ML19VJN002 was taken from the informal type section in the Cleland Hills, ~115 km NW of Kings Canyon. Outcrop at the sample site is ferruginised and partly silicified, and consists of red-orange, thinly-bedded, very poorly sorted and very coarse-grained sandstone with abundant feldspar and mica. The sample was taken from a bed with no apparent clasts, although clasts are common elsewhere in the section. Clasts range from granule to large pebble size, are rounded to subrounded, and consist mostly of quartzite. Sedimentary structures are common and include trough, planar, and low angle cross beds, as well as clay galls. No fossils have been found in the Cleland Sandstone. However, its stratigraphic position indicates a middle to late Cambrian age. The Cleland Sandstone grades laterally into the late Cambrian Hugh River Shale along the northern margin of the Idirriki Sub-basin, conformably underlies the late Cambrian Goyder Formation in the Idirriki Sub-basin, and conformably underlies the early Ordovician Pacoota Sandstone further west, including in the Cleland Hills (MOUNT LIEBIG). Its lower contact is not exposed (Ranford et al 1965), but the Cleland Sandstone is probably unconformable on the middle Cambrian Tempe Formation (Kennard and Lindsay 1991, Gravestock and Shergold 2001) and other early Cambrian units.
Beyer, E.E., Verdel, C., Normington, V.J., Magee, C.W., 2020. Summary of results. Joint NTGS-GA geochronology project: western Amadeus Basin, July 2019-June 2020. Northern Territory Geological Survey Record, 2020-006, 43p.

Mount Currie Conglomerate
The Mount Currie Conglomerate is a thick succession of conglomerate within the Mount Currie Sub-basin along the SW margin of the Amadeus Basin. It is best exposed at Mount Olga (Kata Tjuta), where it is 650 m thick. The conglomerate consists of rounded to subrounded pebble to boulder size clasts (typically 10-20 cm, ranging up to 0.7-1.5 m) of felsic volcanic rocks, with less common quartzite, vein quartz, granite, and basalt. The matrix is a coarse-grained sandstone with ~5% feldspar and mica within a clay cement. The unit is divided into three informal members. The basal member is restricted to the N margin of the sub-basin and comprises conglomerate with spherical, tightly packed sandstone clasts (of Winnall Group). The middle member is a polymictic conglomerate comprising poorly-sorted, subangular to well-rounded clasts of porphyritic rhyolite with lesser basalt and sandstone. It transitions into the upper member, where granite and basalt clasts outnumber rhyolite. Sample PR19VJN001 is from a boulder field 8.5 km NW of Mount Currie. We targeted exposures of the conglomerate matrix on the slopes of the boulder field, to avoid sampling of clast-hosted zircons. he age of the Mount Currie Conglomerate is poorly constrained. Wells et al (1970) correlated it with the late Ediacaran to early Cambrian Arumbera Sandstone. Haines et al (2010) revised Amadeus Basin stratigraphy in WA, and suggested the Mount Currie Conglomerate is early Cambrian; however, Haines et al (2016) raised the possibility that it was deposited late in the Ngaanyatjarra Rift (ca 1 Ga). Here, the Mount Currie Conglomerate is tentatively correlated with the lower part of the Pertaoorrta Group, implying a late Ediacaran to early Cambrian age. SHRIMP U-Pb dating of detrital zircons from Mount Currie Conglomerate from Kata Tjuta (AYERS ROCK) yielded a maximum depositional age of 999 +/- 27 Ma (Camacho et al 2002). Sample PR19VJN001 was collected to further constrain the age of deposition.

lower volcaniclastic sandstone
Sample GS20PGF085 is a meta-siltstone/mudstone collected from 515.0-520.0 m, which is the upper continuation of sample GS20PGF058 (520.0-525.7 m) and therefore is of similar composition. The sample is thinly bedded and weakly foliated; its mineralogy is dominated by quartz, feldspar and sericite with minor chlorite and traces of opaque minerals. There are 1-5 micron-thick quartz veins scattered in the groundmass, which are overprinted an S1 foliation
Cross, A.J., Farias, P.G., Huston, D.L., 2022. Summary of results. Joint NTGS-GA geochronology project: Rover mineral field, Warramunga Province, July-December 2020. Northern Territory Geological Survey Record, 2022-005, 31p.

Sample BW20PGF090 is a meta-siltstone/mudstone collected from 428.6-433.14 m within the turbiditic package that hosts the Rover 1 mineralisation (Castile Resources Limited; Coles 2009; Valenta et al 2020). The sample is located ~12 m above the mineralisation. It is a mixture of fine-grained meta-siltstone/mudstone (90%) and coarse-grained volcaniclastic sandstone (10%). The petrography reveals a chlorite-sericite-altered, clast- to matrix-supported, massive crystal-rich, coarse-grained volcaniclastic sandstone. The clastic components of the sandstone (quartz and feldspar crystals and fragments) are subhedral to angular. Most of the 0.5-1 mm quartz crystals and fragments are embayed with cuspate borders. The fabric is matrix-supported, and locally clast-supported. There is no bedding or layering detected at the thin section scale; however, there is weakly-defined graded bedding at drill core-scale. The anastomosing foliation is defined by sericite and chlorite.
Cross, A.J., Farias, P.G., Huston, D.L., 2022. Summary of results. Joint NTGS-GA geochronology project: Rover mineral field, Warramunga Province, July-December 2020. Northern Territory Geological Survey Record, 2022-005, 31p.

Sample BW20PGF156 was collected from the interval 411.0-413.3 m within the volcaniclastic sandstone part of the turbiditic package that hosts the Explorer 142 mineralisation (Coles 2009; Valenta et al 2020). The sample is part of a ~20 m-thick massive sandstone unit located ~60 m above the mineralisation. Petrographically, it is a sericite-altered, matrix-supported, massive, crystal-rich and coarse-grained volcaniclastic sandstone. The composition is 40-50%, 50-150 micron angular quartz fragments; 30-40%, 50-100 micron sub-angular feldspar crystals; and 20-30%, 50-100 micron opaque minerals, all in a sericite-quartz matrix. There is a weak S1 foliation marked by the sericite.

Warrawoona Group
PORT HEDLAND_BEDOUT ISLAND_169026.1
Nelson, DR 2004, 169026: volcaniclastic metasandstone, Lawson Well; Geochronology Record 61: Geological Survey of Western Australia, 5p.

MXCURD002 is located ~95 km SW of Tennant Creek, at the Curiosity prospect, and was drilled to a depth of 590 m by Castile Resources Limited in 2015 (Burke 2015). Sample GS19DLH0056 is a moderately to strongly foliated, felsic volcaniclastic sandstone. The rock contains 20-30% 0.5-2 mm anhedral and undulose quartz phenoclasts; 3-5% 0.5-1 mm relatively fresh microcline phenoclasts; 2-3% 2-7 mm sericitic siltstone clasts; and sparse 0.5-1 mm, fresh plagioclase phenoclasts, all in a very fine-grained, strongly foliated, silty sericite-quartz matrix. The fabric wraps around the phenoclasts. Local quartz growth beards develop in the fabric against some of the quartz phenoclasts. This sample was submitted for geochronology to determine a maximum depositional age in order to help constrain the volcanic and depositional history of the Rover field.
Cross, A., Huston, D.L., Farias, P., 2021. Summary of results. Joint NTGS-GA geochronology project: Rover mineral field, Warramunga Province, January-June 2020. Northern Territory Geological Survey Record, 2021-003, 20p.; Huston, D.L., Cross, A., Skirrow, R., Champion, D.C., Whelan, J., 2020, The Tennant Creek mineral field and Rover fields: Many similarities but some important differences. IN: MacDonald, G.C. (ed.) Annual Geoscience Exploration Seminar (AGES) proceedings, Alice Springs, Northern Territory 24-25 March 2020. Northern Territory Geological Survey, 70-83.

Croydon Well
Nelson, DR 2000, 142942: metasandstone, Croydon Well; Geochronology Record 327: Geological Survey of Western Australia, 5p.

NELSON, D. R., 2002, 169120: metasandstone, Desert Queens Bath; in Compilation of geochronology data, 2001: Western Australia Geological Survey, Record 2002/2, p. 84-88.

Brumby Formation
The Brumby Formation (Pmb, Rawlings et al., 2008) conformably overlies the Drummond Formation, but the upper contact with the Shady Bore Quartzite is not exposed, although a conformable contact is assumed. Similar to the underlying Drummond Formation, the Brumby Formation is considered to have been deposited in a mainly shallow marine environment with some deeper marine, low energy facies higher in the formation (Rawlings et al., 2008). Rawlings et al. (2008) suggest a depositional age similar to that determined for the Paradise Creek Formation (McNamara Group, ca 1658–1653 Ma, e.g. Page et al., 2000), with which the Brumby Formation and the underlying Drummond Formation are considered approximately laterally equivalent. The sampled unit is a massively to thickly bedded, very fine-grained, very well-sorted and well-rounded quartz sandstone. Rounded quartz grains are mantled by interstitial quartz cement. Minor opaques are present (<1%).

In MOUNT DRUMMOND, Rawlings et al. (2008) describe the Surprise Creek Formation as consisting of well-rounded pebble to boulder conglomerate (with rhyolite clasts near the base, presumably Top Rocky Rhyolite), interlayered with sub-lithic to quartz sandstone (displaying small scale trough beds and current lineations) up to 200 m in stratigraphic thickness. The stratigraphic affinity of the Surprise Creek Formation in MOUNT DRUMMOND is ‘unassigned’ (Rawlings et al., 2008). The depositional environment is probably a proximal braided fluvial system, with local alluvial fans (Rawlings et al., 2008). This sample (GA 2786161) was collected some 15-20 m above a basal cobble to boulder conglomerate, unconformably underlain by package of interlayered Top Rocky Rhyolite (ca 1725 Ma) and quartz sandstone. The sampled unit is a highly silicified matrix-supported pebble conglomerate with a poorly sorted, sub-angular coarse sand matrix. Bedding is indistinct and poorly defined.

Top Lily Sandstone Member
A second sample of the Top Lily Sandstone Member was collected immediately underlying the major unconformity with the overlying Georgina Basin, some 23 km to the west of the type section for Top Lily Sandstone Member (GA 2785628). This sample is a creamy feldspathic quartz sandstone with purplish fractures and irregular staining, with locally large (<2 m) cross-beds. Bedding dips locally as much as 70-80 degrees to the NNW but is typically shallow to flat lying elsewhere. The unconformity (roughly 2 m up stratigraphy) with the overlying Georgina Basin (locally the Cambrian Wonarah Formation) is characterised by highly silicified matrix-supported breccia of angular cherty or flinty clasts.

A total of 84 analyses were collected from 84 zircon crystals. Nine analyses have excessively high 206Pbc (> 0.95%). Another two analyses yield individual 207Pb/206Pb dates that are older than 1400 Ma, but are more than 10% discordant. These eleven analyses are interpreted as unreliable and are not considered further. The remaining 73 analyses are characterised by low to moderate U contents (34-687 ppm, median 169 ppm), a wide range of Th/U (0.02-3.06, median 0.66), and low 206Pbc (maximum 0.61%, median 0.03%). The 73 accepted analyses are divided into seven groups: Group 1 is a single analysis with an individual 238U/206Pb date of 517 +/- 14 Ma (2sigma); Group 2 consists of 27 analyses from 27 zircons with individual 238U/206Pb dates between c. 590 Ma and 520 Ma; Group 3 consists of four analyses from four zircons with individual 238U/206Pb dates between c. 795 Ma and 645 Ma; Group 4 consists of eleven analyses from eleven zircons with individual 238U/206Pb dates between c. 980 Ma and 850 Ma; Group 5 consists of 20 analyses from 20 zircons with individual 238U/206Pb dates between c. 1285 Ma and 1025 Ma; Group 6 consists of four analyses from four zircons with individual 207Pb/206Pb dates between c. 2080 Ma and 1620 Ma; and Group 7 consists of six analyses from six zircons with individual 207Pb/206Pb dates pre-2500 Ma.The individual 238U/206Pb age of 517 +/- 14 Ma (2sigma) is interpreted as a maximum depositional age for the 900 m interval of the Lesueur Sandstone (Yalgorup Member). This age is considerably older than the biostratigraphically (S. speciosus to M. crenulatus Zones) determined Late Triassic depositional age of this unit.
Harvey 1
Queensland Department of Mines and Energy
Lewis, C.J., 2017. SHRIMP U-Pb isotopic results, GSWA Harvey 1, Western Australia. Geoscience Australia. Record, 2017/20, 110p.

Velkerri Formation
fine grained siltstone
Elliott 1
Yang, B., Smith, T.M., Collins, A.S., Munson, T.J., Schoemaker, B., Nicholls, D., Cox, G., Farkas, J., Glorie, S., 2018. Spatial and temporal variation in detrital zircon age provenance of the hydrocarbon-bearing upper Roper Group, Beetaloo Sub-basin, Northern Territory, Australia. Precambrian Research, 304, 140-155.

Carnegie Formation
The Carnegie Formation is a thick siliciclastic unit recognised across the Amadeus Basin in WA and locally into the NT. It is dominated by immature, red-brown, fine- to medium-grained lithic and feldspathic sandstone and interbedded micaceous siltstone, with cement that is often calcareous (Haines et al 2015). Minor conglomerate interbeds are present locally. Sedimentary structures include cross-beds, ripples, erosive sole marks, and desiccation cracks; some sandstone beds have channel-like morphologies. The Carnegie Formation is generally less than 2000 m thick and thins north to as little as 70 m in the Boord Ridges. Maximum thickness is interpreted in a depocentre west of the Sir Frederick Range, where the formation is estimated to be up to or greater than 3400 m thick (Haines et al 2012). Sample MR19CSV111 was collected in the Northern Territory from a low ridge ~2 km E of the border and ~70 km SW of Kintore. At the sample locality, the Carnegie Formation is monotonous red, medium-bedded, medium-grained feldspathic sandstone. The depositional age of the Carnegie Formation is late Ediacaran to Cambrian, based on its stratigraphic relationship with the underlying Ediacaran Julie Formation and the overlying late Ediacaran or early Cambrian Ellis Sandstone. These relationships are best exposed in the Boord Ridges/ Gordon Hills area in WA (Haines and Allen 2014). Normington et al (2019) correlated the Carnegie Formation with the Pertaoorrta Group. SHRIMP U-Pb dating of detrital zircons from a sandstone of the Carnegie Formation in WA yielded a maximum depositional age of 819 +/- 13 Ma (Haines et al 2015). This result is considerably older than the late Ediacaran to Cambrian depositional age inferred from stratigraphic position. Sample MR19CSV111 was collected to further constrain the age of deposition, and any lateral variations in provenance for the unit between WA and the NT.

Sample GS20PGF190 is a meta-siltstone/mudstone collected from the interval 525.7-531.5 m, which is the downhole continuation of sample GS20PGF058 (520.0-525.7 m. As observed in other samples from Curiosity, GS20PGF190 preserves an ill-defined bedding and spaced S1 foliation. The groundmass is dominated by quartz, feldspar and sericite, with trace opaque minerals. The coarser grains are typically in the basal section of the cm-thick beds, which gradually transition to very fine-grained facies.

Top Lily Sandstone Member
The Top Lily Sandstone Member (within the Playford Sandstone) is a white to reddish, fine-grained lithic sandstone, with minor pebble lags and numerous current and shallow water indicators. The member is 143 m thick in the type section, but up to 1100 m thick elsewhere (Rawlings et al., 2008). Kositcin and Carson (2019) reported detrital zircon age spectra for two samples of the Top Lily Sandstone Member. The first (GA 2785628) was collected in the measured section described by Rawlings et al. (2008), in the footwall (southern side) of the north-dipping Mitchiebo Fault (e.g. Carr et al., 2019). It contains a population defining a maximum depositional age of 1546 +/- 26 Ma, which is the best available maximum age for Playford Sandstone deposition, and confirms a Mesoproterozoic or younger age for the Top Lily Sandstone Member, and overlying units in the measured section. The second sample (GA 2786167) was collected ~25 km W of the measured section, in the hanging (northern) wall of the Mitchiebo Fault, near the unconformity with the overlying Georgina Basin. It contains no zircons younger than ca. 1620 Ma, and a well-defined zircon population defines a maximum depositional age of 1656 +/- 12 Ma. Although this age spectrum does not preclude Mesoproterozoic deposition, Anderson et al. (2019b) and Carson et al. (2020a) interpreted this sample of the so-called Top Lily Sandstone as a late Paleoproterozoic equivalent of the McNamara Group, rather than South Nicholson Group as previously mapped. Sample GA 3305196 was collected to verify this interpretation, and to better constrain the local distribution of Mesoproterozoic versus Paleoproterozoic units. It was collected ~35 km WNW of the Playford Sandstone measured section (Rawlings et al., 2008), in the hanging (northern) wall of the Mitchiebo Fault. It comprises white-pink, well-sorted silicified sandstone, with sub-angular to sub-round quartz and massive beds up to 30 cm thick. Upright bedding dips gently to the NNE.
Kositcin, N., Carson, C.J., Anderson, J.R., Doublier, M.P., Murr, J., 2020. Exploring for the Future - New SHRIMP geochronology constraints on the basin evolution of the South Nicholson region. Geoscience Australia. Record, 2020/25, 109p.; Carson, C.J., Kositcin, N., Anderson, J.R., Henson, P.A., 2023, A revised Proterozoic tectono-stratigraphy of the South Nicholson region, Northern Territory, Australia - insights from SHRIMP U-Pb detrital zircon geochronology. Australian Journal of Earth Sciences, in press.

University of Melbourne
Only a few grains considered to be magmatic. Inherited grains about 500 Ma.
Pinnak Sandstone
McGoldrick, P.J., Gleadow, A.J.W., 1977. Fission-track dating of Lower Palaeozoic sandstones at Tatong, north central Victoria. Carnarvon Basin, Western Australia. Geological Society of Australia Journal, 24(8), 461-464.

Age taken from GSNSW's MinView. Not directly reported in Meffre et al 2007
Adaminaby Group
Quartz-rich sandstone. Contain mostly quartz (74 - 96%) with almost no volcanic fragments (50.2%) and, more importantly, no mafic volcanic fragments.
Meffre S., Scott R.J., Glen R.A. & Squire R.J. (2007) Re-evaluation of contact relationship between Ordovician volcanic belts and the quartz-rich turbidites of the Lachlan Orogen., Australian Journal of Earth Sciences 54, 363-383.

Crow Formation
The Crow Formation (Rawlings et al., 2008) is a largely recessive unit that outcrops poorly throughout the western two-thirds of MOUNT DRUMMOND. The Crow Formation is composed of up to 2500 m of interbedded siltstone, sandstone, shale and lesser conglomerate (Rawlings et al., 2008). This sampled unit represents an ‘unnamed’ unit (Psos) as mapped on MOUNT DRUMMOND (Rawlings et al., 2008). This sample was collected from a rounded ~150 m wide isolated hill where the lithology is markedly different to other unnamed Crow Formation samples, GA 2785613 and GA 2786168. The unit is a weathered dark reddish to purple texturally immature, micaceous and feldspathic highly friable sandstone, moderately bedded with variable bedding thicknesses, between 3-30 cm, and containing 1-2 m scale trough cross-beds. Bedding dips 10º towards 023º. The field relationships with adjacent units (Burangoo Sandstone Member, GA 2786169, 500 m to the north, and another, lithologically different, unnamed unit of the Crow Formation, GA 2786181, 400 m to the south) are impossible to discern due to poor intervening outcrop and Cainozoic cover.

Tobacco Member
The Tobacco Member is the uppermost unit of the Crow Formation (Wild Cow Subgroup, South Nicholson Group; Rawlings et al., 2008), forming resistant strike ridges in the Mittiebah and Canyon Ranges, western MOUNT DRUMMOND (Boxer and Mittiebah 100K mapsheets). At the type section in the central Mittiebah Range (Rawlings et al., 2008), the 300-600 m thick Tobacco Member conformably overlies the lower Crow Formation, and is conformably overlain by the Mittiebah Sandstone. Elsewhere, the Tobacco Member is unconformably overlain by the Mittiebah Sandstone. The unit is a diffusely bedded, quartz to lithic, locally ferruginous (+/- micaceous, +/- glauconitic), fine- to medium-grained sandstone, with interbedded white tabular shale and siltstone. Local pebble to cobble conglomerate lags are common. Low angle trough beds and hummocky cross-stratification (indicative of storm action) are also common (Rawlings et al., 2008). The depositional environment is interpreted as a shallow-water to tidal and storm influenced marine shelf (Rawlings et al., 2008). This sample was collected 60 km NW of Mittiebah Station (NT), in the Canyon Range region of NW MOUNT DRUMMOND. It is a pink to orange, medium- to coarse-grained, sub-angular to sub-round, well-sorted, laminated to medium bedded (up to 15 cm) quartz sandstone. Bedding is upright and dips moderately (~30 degrees) to the east. Cross-beds are common. The sample was collected to support the integrated structural-stratigraphic model proposed by Anderson et al. (2019b) and Carson et al. (2020a) in which a number of successions, previously identified as Mesoproterozoic South Nicholson Group, are, in some cases, late Paleoproterozoic in age. This model has regional structural and basin evolution implications. This sample of the Tobacco Member was collected to better discriminate the areal extent and distribution of Mesoproterozoic versus Paleoproterozoic clastic sedimentary rocks across MOUNT DRUMMOND.
Kositcin, N., Carson, C.J., Anderson, J.R., Doublier, M.P., Murr, J., 2020. Exploring for the Future - New SHRIMP geochronology constraints on the basin evolution of the South Nicholson region. Geoscience Australia. Record, 2020/25, 109p.

Burangoo Sandstone
The Burangoo Sandstone Member (Sweet et al., 1981; Rawlings et al., 2008) is a unit within the Constance Sandstone (Accident Subgroup), characterised as a fine- to coarse-grained lithic, sublithic to quartz sandstone with pebble lags. Trough cross beds are up to 1m in scale. Rawlings et al. (2008) suggest the lower contact with the underlying Pandanus Siltstone Member is sharp and apparently comformable as is the upper contact with the overlying Wallis Siltstone Member. Sweet (2017) however, argues for a 'minor unconformity' with the underlying Pandanus Siltstone Member. The unit is estimated to be up to 320 m thick at the type locality, but is typically around 130-150 m thick (Rawlings et al., 2008; Sweet, 2017). A shallow-marine to intertidal paleoenvironment is inferred by Rawlings et al. (2008). No previous geochronology on the Burangoo Sandstone Member has been conducted in the Northern Territory. Magee et al. (2012) and Carson et al. (2011) determined maximum deposition ages for the Burangoo Sandstone Member at 1602 +/- 30 Ma and 1566 +/- 45 Ma respectively, immediately to the east of the NT-QLD border in the Lawn Hill Platform region. It is worth noting that Queensland geologists have elevated the stratigraphic status of the Burangoo Sandstone Member to formation level (i.e. the Burangoo Sandstone, e.g. Sweet, 2017) and also place this unit into the lower Wild Cow Subgroup rather than the Accident Subgroup. At the sample location, the Burangoo Sandstone Member is a flaggy friable cream to tan coloured feldspathic 'dirty' quartz to sublithic sandstone, locally ferruginous, with bedding thickness between ca 40 cm and <5 cm, with narrow interbedded layers of fissile siltstone. Small to medium scale trough cross-beds are evident. Stratigraphic and lithological relationships with adjacent outcrops of Crow Formation are obscured by intervening Cainozoic cover.

Bessie Creek Sandstone
coarse grained arenite
Sever 1

Ballara Quartzite
Sample 3316526/DPMI130 was collected from a quartzite ridge 260 m west of Mount Maggie Granite sample site 3316525/DPMI129. The site is ~10.7 km northwest of Mount Maggie and forms the margin of a circular structure comprising the Corella Formation, Mount Maggie Granite and unnamed mafic intrusive rocks. The narrow zone between Mount Maggie Granite site DPMI129 and this ridge comprises biotite schist intruded by foliated aplite, pegmatite and mafic rocks. The quartzite at DPMI130 is foliated but locally exhibits planar and cross bedding. It is dominated by medium- to coarse-grained recrystallised quartz but also includes minor feldspar, amphibole and titanite. Previous mapping showed this site as comprising Corella Formation (Wilson et al., 1980). We sampled this quartzite because the metasedimentary rocks in this area are directly intruded by the Mount Maggie Granite. Our rationale was that if the granite at 3316526/DPMI130 is of similar age to other Wonga Igneous Subprovince samples (~1740 Ma, Neumann et al., 2009) then this quartzite must be considerably older because it has been deposited and buried to mid-crustal levels prior to intrusion. This would be inconsistent with recent age data from elsewhere in the Corella Formation that indicate depositional ages of ~1750-1740 Ma (see Kositcin et al., 2019), raising the possibility that this quartzite is part of the Ballara Quartzite rather than the Corella Formation.
Kositcin, N., Purdy, D.J., Bultitude, R.J., Brown, D.D., Hoy, D., 2021. Summary of results. Joint GSQ-GA geochronology project: Mary Kathleen Domain and rocks under younger cover east of the Mount Isa Inlier, 2019-2020. Queensland Geological Record, 2021/01, 112p.

Steel Dragon 1
Lech, M.E., Lewis, C.J., White, L.T., Abbott, S.T., 2018. Triassic provenance analysis of the Roebuck Basin, North West Shelf of Australia. ASEG/SEG Conference Papers, 2018(1), 6p.

Coonabildie Formation

Mittiebah Sandstone
The Mittiebah Sandstone of the western South Nicholson Basin is tentatively interpreted as equivalent to the Constance Sandstone in the eastern SNB. It consists of fine- to coarse-grained, quartz-dominated to lithic sandstone, with minor interbeds of siltstone and pebble to cobble conglomerate (Ahmad and Munson, 2013b). The Mittiebah Sandstone overlies the Tobacco Member of the Crow Formation and is unconformably overlain by the Paleozoic Georgina Basin. Anderson et al. (2019a) reported detrital zircon data from a sample (GA 2676116) collected 13 km along strike from (and SW of) the Mittiebah Sandstone measured section (Rawlings et al., 2008), which yielded a maximum depositional age of 1586 +/- 7 Ma, confirming the Mittiebah Sandstone at that location is Mesoproterozoic or younger. However, Anderson et al. (2019a) also reported data from Mittiebah Sandstone (GA 2676117) ~50 km NW of the current sample, which together with the underlying Crow Formation (GA 2785621) and Bowgan Sandstone (GA 2785620) in the hanging wall of the Benmara Fault (Kositcin and Carson, 2019), resemble late Paleoproterozoic successions, rather than Mesoproterozoic as previously interpreted (Anderson et al., 2019b; Kositcin and Carson, 2019). Carson et al. (2020a) concluded that these units were stratigraphic equivalents of the mid-McNamara Group, deposited during ca. 1640 Ma extension along the Benmara Fault, and proposed an expanded Benmara Group. GA 3305198 was collected to test the hypothesis that "Mittiebah Sandstone" in the hanging wall of the Benmara Fault is late Paleoproterozoic, rather than Mesoproterozoic. The sample selected for geochronology is a white, fine-grained, thickly bedded to laminated, subangular to subround, saccharoidal quartz sandstone. It was collected in the Canyon Range region W of the Benmara Fault.
Kositcin, N., Carson, C.J., Anderson, J.R., Doublier, M.P., Murr, J., 2020. Exploring for the Future - New SHRIMP geochronology constraints on the basin evolution of the South Nicholson region. Geoscience Australia. Record, 2020/25, 109p.; Carson, C.J., Kositcin, N., Anderson, J.R., Henson, P.A., 2023, A revised Proterozoic tectono-stratigraphy of the South Nicholson region, Northern Territory, Australia - insights from SHRIMP U-Pb detrital zircon geochronology. Australian Journal of Earth Sciences, in press.

Breakfast Sandstone
The Breakfast Sandstone (Benmara Group, Rawlings et al., 2006, 2008) comprises a thin succession of white to pink, medium- to coarse-grained, silicified sub-lithic sandstone and rare chertified stromatolitic carbonate in the Benmara region, NW MOUNT DRUMMOND. The Breakfast Sandstone was previously included as part of, and undifferentiated from, the Benmara beds (Smith and Roberts, 1963), a now defunct name which also included the overlying Buddycurrawa Volcanics (Rawlings et al., 2008). Although Rawlings et al. (2008) reported that the Breakfast Sandstone forms resistant strike ridges in two "reference areas" (e.g. Canyon Range at 707300mE 8000700mN, some 5 km SSE of the sample locality), in other locations, the unit is poorly exposed, consisting of subcrop of silicified quartz sandstone. Trough cross beds, ripples, and desiccation cracks are common and interpreted to represent a moderate to high energy fluvial to shallow marine depositional environment (Rawlings et al., 2008). The Breakfast Sandstone stratigraphically overlies the Murphy Metamorphics and Connelly Volcanics of the Murphy Province. The contact with the underlying units of the Murphy Province is not directly exposed, but the relationship is assumed to be unconformable; the contact with poorly-sorted ferruginous sandstone of the overlying Buddycurrawa Volcanics is conformable (Rawlings et al., 2008). Carson et al. (2020b) reported an age for the Buddycurrawa Volcanics between ca. 1660 Ma and 1630 Ma, which provides a minimum depositional age for the Breakfast Sandstone of ca 1660 Ma. The analysed sample was collected ~14 km SSE of Benmara Station. The sample is a cross-bedded silicified sandstone, comprising well-sorted, rounded quartz. Bedding is up to 30 cm thick, upright and dips gently (~10 degrees) to the west. Silicified, matrix-supported, angular quartz sandstone and pebble conglomerate are also observed.
Kositcin, N., Carson, C.J., Anderson, J.R., Doublier, M.P., Murr, J., 2020. Exploring for the Future - New SHRIMP geochronology constraints on the basin evolution of the South Nicholson region. Geoscience Australia. Record, 2020/25, 109p.

migmatite
Kirkland, CL, Wingate, MTD and Bodorkos, S 2008, 183466: banded gneiss, Latitude Hill; Geochronology Record 746: Geological Survey of Western Australia, 5p.

Boomarra Metamorphics
Sample 3316528/DPMI110 was collected from a low continuous strike ridge of psammitic schist and quartzite. This is accessed via a network of station tracks west of the Burke Developmental Road in the vicinity of Pigeon House Mountain on the southern part of Boomarra Station. The strike ridge forms the western margin of the outcropping Mary Kathleen Domain. Areas to the west are covered by Cenozoic and Jurassic-Cretaceous sediments and sedimentary rocks. The quartzite sampled at site 3316528/DPMI110 is mapped as part of Boomarra Metamorphics/m, a moderately magnetic subunit (Geological Survey of Queensland, 2011). Prior to this investigation the main constraint on the age of the Boomarra Metamorphics is a crystallisation age of 1776 +/- 8 Ma from a felsic volcanic rock exposed ~3 km to the south (Carson et al., 2009). Page & Sun (1998) also reported depositional ages of 1774 +/- 4 Ma and 1775 +/- 4 Ma for felsic volcaniclastic rocks now mapped as part of the Boomarra Metamorphics. The quartzite is dominated by strained and recrystallised quartz and lesser amounts of muscovite, feldspar and altered phases. This sample was selected for geochronology to compare the provenance spectrum with spectra from the nearby Corella Formation (sample 3316527/DPMI108) and from core samples of metasedimentary rocks of unknown affinities intersected at depth in holes drilled to the west and north.
Kositcin, N., Purdy, D.J., Bultitude, R.J., Brown, D.D., Hoy, D., 2021. Summary of results. Joint GSQ-GA geochronology project: Mary Kathleen Domain and rocks under younger cover east of the Mount Isa Inlier, 2019-2020. Queensland Geological Record, 2021/01, 112p.

RVDD0002 is located ~60 km SW of Tennant Creek township and was drilled to a depth of 545.6 m by Todd River Resources Limited in April 2019 (Wetherley and Elliston 2019). Lithological logging of the cored part of drillhole RVDD002, from the eastern part of the Rover field, identified two broad units: an upper quartz-feldspar porphyritic dacite (101.90-118.20 m), and a heterogeneous lower unit consisting mostly of felsic to intermediate volcaniclastic and volcanic rocks (118.20-545.60 m = end of hole). Sample BW19DLH0006 is a dark grey, chloritic, massive, coarse- to very coarse-grained intermediate volcaniclastic sandstone. In detail, there is a sharp contact between fine- to medium-grained volcaniclastic sandstone and fine-grained volcaniclastic sandstone. The fine- to medium-grained volcaniclastic sandstone contains 20-30% 0.1-1 mm pervasively sericite-altered, angular to sub-angular feldspar clasts (with rare relic feldspar); 10-20% 0.1-0.5 mm pervasively chlorite +/- carbonate-altered, angular amphibole (?) clasts; 2-3% 0.5-2 mm sericite-chlorite altered, angular to sub-angular lithic (altered glass?) clasts; and <0.5% 0.1-0.2 mm subhedral quartz clasts, in a chlorite-sericite-altered matrix that may be altered, fine-grained (0.1-0.5 mm) glassy sand. The fine-grained sandstone consists predominantly of the chlorite-sericite altered (glassy?) matrix with very minor clasts of chlorite-altered amphibole(?). The thin section contains one 3-5 mm, chlorite +/- carbonate-altered (after amphibole?) clast surrounded by an aureole of sericite-altered feldspar. The clast contains several 0.1-0.5 mm sub- to euhedral, sericite +/- carbonate-altered plagioclase inclusions. The sample is cut by a 0.1-0.3 mm planar quartz vein containing 0.5-1% 0.05-0.2 mm anhedral opaque grains. This volcaniclastic rock was selected for geochronology to determine a maximum depositional age to help constrain the timing of volcanism and associated sedimentation in this region.
Cross, A., Huston, D.L., Farias, P., 2021. Summary of results. Joint NTGS-GA geochronology project: Rover mineral field, Warramunga Province, January-June 2020. Northern Territory Geological Survey Record, 2021-003, 20p.; Huston, D.L., Cross, A., Skirrow, R., Champion, D.C., Whelan, J., 2020, The Tennant Creek mineral field and Rover fields: Many similarities but some important differences. IN: MacDonald, G.C. (ed.) Annual Geoscience Exploration Seminar (AGES) proceedings, Alice Springs, Northern Territory 24-25 March 2020. Northern Territory Geological Survey, 70-83.

University of Melbourne
Pinnak Sandstone
McGoldrick, P.J., Gleadow, A.J.W., 1977. Fission-track dating of Lower Palaeozoic sandstones at Tatong, north central Victoria. Carnarvon Basin, Western Australia. Geological Society of Australia Journal, 24(8), 461-464.

Nelson, DR 2004, 172840: coarse-grained sandstone, Rainbow Prospect; Geochronology Record 50: Geological Survey of Western Australia, 5p.

Mooline Formation
Ashburton Region
Nelson, DR 2004, 148925: coarse lithic sandstone, Koonong Pool; Geochronology Record 250: Geological Survey of Western Australia, 6p.

Golden Cockatoo Formation
MARBLE BAR_178045.1
Nelson, DR 2005, 178045: sandstone, Quininya Well; Geochronology Record 567: Geological Survey of Western Australia, 5p.

Murphy Region
Anderson, J.R., Lewis, C.J., Jarrett, A.J.M., Carr, L.K., Henson, P.A., Carson, C.J., Southby, C., Munson, T.J., 2019. New SHRIMP U-Pb zircon ages from the South Nicholson Basin, Mount Isa Province and Georgina Basin, Northern Territory and Queensland: July 2017-June 2018. Geoscience Australia. Record, 2019/10, 101p.

The Coombing Formation contain Darriwilian to Gisbornian (Early to Middle Ordovician) graptolites.
Coombing Formation
Meffre 2007 paraphrased: a volcaniclastic sandstone from the Coombing Formation near Lyndhurst, contains mostly feldspar and volcanic fragments (65 - 91%) with almost no quartz (< 2.6%).
Meffre S., Scott R.J., Glen R.A. & Squire R.J. (2007) Re-evaluation of contact relationship between Ordovician volcanic belts and the quartz-rich turbidites of the Lachlan Orogen., Australian Journal of Earth Sciences 54, 363-383.

Maurice Formation
The Maurice Formation is recognised across the Amadeus Basin in WA, and locally in the NT. Exposures in the NT are limited to a low range straddling the border, south of Lake MacDonald (MOUNT RENNIE). Haines et al (2015) described the Maurice Formation in WA as containing a lower recessive unit of red-brown, micaceous siltstone and friable, fine-grained sandstone, and an upper unit dominated by red-brown, immature micaceous sandstone with subordinate siltstone and local conglomeratic sandstone. Sample MR19CSV109 was collected in the NT from a low ridge ~2 km E of the border and ~70 km SW of Kintore. Outcrop at the sample locality is red, moderately-sorted, medium-grained sandstone; sedimentary structures include cross-stratification and current lineations. It is unclear whether the upper or lower unit of the Maurice Formation (as defined by Haines et al 2015) was sampled, as the persistence of that subdivision into the NT has not yet been determined. In the absence of palaeontological constraints, an early Cambrian age is indicated for the Maurice Formation, based on stratigraphic position. It overlies the late Ediacaran Ellis Sandstone, and underlies the middle Cambrian Cleland Sandstone. Haines et al (2010) regarded the Maurice Formation as a likely correlative of the upper Winnall Group, and a probable equivalent more distally to the upper Arumbera Sandstone in the NE of the basin. However, Normington et al (2019) correlated the unit more closely with the Pertaoorrta Group. Detrital zircon SHRIMP U-Pb dating of lithic sandstone from the lower and upper units of the Maurice Formation in WA yielded maximum depositional ages of 831 +/- 13 Ma and 698 +/- 20 Ma respectively (Haines et al 2015). These results are considerably older than the early Cambrian depositional age inferred from stratigraphic position. Sample MR19CSV109 was collected to further constrain the age of deposition, and any lateral variations in provenance for the unit between WA and the NT.

Ellis Sandstone
The Ellis Sandstone is recognised across the Amadeus Basin in WA, and locally in the NT. Exposures in the NT are limited to a low range straddling the border, south of Lake MacDonald (MOUNT RENNIE). It typically comprises cross-bedded kaolinitic sandstone and pebbly sandstone, with subordinate calcareous sandstone and siltstone (Edgoose 2013). Pebble clasts include sandstone, quartzite, and chert (Haines et al 2015). Sedimentary structures comprise trough and tabular cross-bedding with current lineations common; mud pellets are abundant in some beds (Haines et al 2015). Sample MR19CSV110 was collected in the NT from a low ridge ~2 km E of the border and ~70 km SW of Kintore. At the sample locality, the Ellis Sandstone is red, well-bedded, poorly-sorted, medium-grained quartz sandstone with laminations and cross-bedding. The age of the Ellis Sandstone is late Ediacaran or Cambrian, based on observed or inferred stratigraphic relationships. It overlies the late Ediacaran Carnegie Formation and/or Cryogenian-Ediacaran Areyonga-Julie succession (formerly Boord Formation, WA), interfingers with the late Ediacaran to early Cambrian Sir Frederick Conglomerate (WA), and underlies the early Cambrian Maurice Formation. Haines et al (2010) correlated the Ellis Sandstone with the lower Winnall Group and (along with the Sir Frederick Conglomerate) with the Mount Currie Conglomerate, and more distally, to the middle Arumbera Sandstone in the NE of the basin. However, Normington et al (2019) correlated the unit more closely with the Pertaoorrta Group. Detrital zircon SHRIMP U-Pb dating of a lithic quartz sandstone from the Ellis Sandstone in WA yielded a maximum depositional age of 967 +/- 11 Ma based on the youngest grain (Haines et al 2015), which is considerably older than the late Ediacaran to Cambrian age inferred from stratigraphic position. Sample MR19CSV110 was collected to further constrain the age of deposition and lateral variations in provenance between WA and the NT.

Kelly Group
volcaniclastic metasandstone
Nelson, DR 2002, 168993: volcaniclastic metasandstone, Bob Bore; Geochronology Record 162: Geological Survey of Western Australia, 4p.

Wyman Formation
PORT HEDLAND_BEDOUT ISLAND_168992.1
Nelson, DR 2004, 168992: volcaniclastic metasandstone, Bob Bore; Geochronology Record 161: Geological Survey of Western Australia, 5p.

Top Lily Sandstone Member
The Top Lily Sandstone Member (Rawlings et al., 2008) is characterised as a white to reddish fine-grained lithic sandstone, with minor pebble lags and numerous current and shallow water indicators such as current lineations, ripples and large cross-beds. The member is 143 m thick in the type section, but is reported to be up to 1100 m thick elsewhere (e.g. Ten Mile Anticline, some 40 km to the west). The lower contact with the Wangalinji Member is gradational whereas the upper contact with the No Mans Sandstone Member is sharp and locally erosional but ‘essentially’ conformable (Rawlings et al., 2008). A marine shallow-water shelf or tidal channel paleo-environment is proposed. Existing age constraints for the Top Lily Sandstone Member (and other members of the Playford Sandstone) are poor. Page et al. (2000) obtained a maximum deposition age of ca 1591 Ma from the underlying Lawn Hill Formation (McNamara Group; Century Pb-Zn mine, ca 120 km east) in the Lawn Hill Platform region, which also provides a maximum constraint for deposition of the Top Lily Sandstone Member. However, Rawlings et al. (2008) conclude that the most reliable estimate for the age of the members of the Playford Sandstone is the broad correlation with the lower Roper Group in the McArthur Basin for which a ca 1493 Ma tuff age (Jackson et al., 1999) is reported. There has been no previous geochronology conducted directly on the Top Lily Sandstone Member. The sampled unit is taken from the measured section (mid-way up the unit) described in Rawlings et al. (2008) and is easily accessed from the Mittiebah-Wangalinji track. Outcrop is poor but comprises massive to thickly bedded (flaggy in places) dark grey to purplish fine-grained quartz sandstone; current parting lineations are visible on bedding surfaces.

Volcaniclastic sandstone or felsic volcaniclastic rock with abundant angular quartz phenoclasts and minor K-feldspar and muscovite phenoclasts. Quartz grains are deformed and locally recrystallised. Fine grained groundmass is moderately sericitised with weak to moderate alignment which defines a weak tectonic foliation (cleavage). Diffuse quartz-chlorite veins are also deformed.
Cross, A.J., Clark, A.D., Schofield, A., Kositcin, N., 2020, New SHRIMP U-Pb zircon and monazite geochronology of the East Tennant region: a possible undercover extension of the Warramunga Province, Tennant Creek. IN: Czarnota, K., Roach, I., Abbott, S., Haynes, M., Kositcin, N., Ray, A. and Slatter, E. (eds.), Exploring for the Future: extended abstracts. Geoscience Australia. Record, 4.

Coen Metamorphic Group
The Coen Metamorphic Group covers the northern extent of the Savannah Province and is in contact with the Iron Range Province and the Newberry Metamorphic Group of the Etheridge Province. The purpose of analysing DBCY051/2614016 is to ascertain if the sample, which has lithological characteristics of the Coen Metamorphic Group, is part of the same unit or, has late Mesoproterozoic to Neoproterozoic zircons that are diagnostic of the Sefton Metamorphics that outcrop to the north in the Iron Range Province. Metamorphic age determinations from this sample may provide information on the movement of the adjacent Yintjingga fault zone which is considered to be a northern splay of the Palmer River Fault zone that separates the Proterozoic North Australian Craton from the late Neoproterozoic to Paleozoic Thomson Orogen and Paleozoic Hodgkinson Province to the east (Wellman, 1995). The sample was collected from a scree slope of large boulders along a track to the south of Lockhart River (~35 km south of Nundah Homestead). The sampled specimen comprises garnet-biotite-sillimanite gneiss. Large garnets (up to 5 cm in hand sample) are cracked and infilled with fine biotite as well as a fine matrix of white mica and sillimanite.
Lewis, C.J., Dhnaram, C.R., Brown, D.D., Bultitude, R.J., Lisitsin, V.A., 2021. Summary of results. Joint GSQ-GA geochronology project: Georgetown, Coen and Cairns regions, 2016-2017. Queensland Geological Record, 2021/05, 62.

Constance Sandstone
The Constance Sandstone (South Nicholson Group) extends across the Northern Territory and Queensland (Carter et al., 1961), although its stratigraphic position and definition have been revised several times (Sweet, 2017 and references therein). Rawlings et al. (2008) delineated five members within it (the Hedleys Sandstone Member, Pandanus Siltstone Member, Burangoo Sandstone Member, Wallis Siltstone Member and the Schultz Sandstone Member), and also tentatively correlated it with the Mittiebah Sandstone of the South Nicholson Group in MOUNT DRUMMOND. Outcrop samples of the Constance Sandstone and the Schultz Sandstone Member in Queensland have previously returned maximum deposition ages of 1599 +/- 19 Ma and 1577 +/- 21 Ma, respectively (Carson et al., 2011). Their detrital zircon age spectra are similar, with a prominent mode at ca. 1760 Ma and a subordinate population at ca. 1600 Ma. DDH 83-3 was drilled by Amoco Australia Petroleum in 1983 in western Queensland (Dorrins et al., 1983). It intersects Constance Sandstone, and Anderson et al. (2019a) reported three detrital zircon age spectra, with maximum depositional ages of 1569 +/- 37 Ma (85.27-85.37 m), 1578 +/- 53 Ma (176.09-176.18 m), and 1591 +/- 18 Ma (234.60-234.91 m). These spectra are difficult to interpret as the zircon populations are small, but the shallowest sample contained a single zircon with an age of 1382 +/- 51 Ma (2sigma), based on two analyses. Maximum depositional ages defined by single zircons are generally considered unreliable, and the aim of the present sample is to verify this putative ca. 1382 Ma population. The sandstone analysed in this Record was collected from the depth interval 93.24-93.29 m in DDH 83-3, some 8 m below the shallowest sample reported by Anderson et al. (2019a). It comprises a pale grey-green claystone-siltstone with minor fine-grained micas and minor very thin dark lenses.
Kositcin, N., Carson, C.J., Anderson, J.R., Doublier, M.P., Murr, J., 2020. Exploring for the Future - New SHRIMP geochronology constraints on the basin evolution of the South Nicholson region. Geoscience Australia. Record, 2020/25, 109p.

The sample was collected from a cutting on Etty Bay Road, 6 km SE of Innisfail. These weathered, poorly exposed siliciclastic rocks are mapped as part of the Barnard Metamorphics (Bultitude et al., 1999) of the Barnard Province (Bultitude and Champion, 2013), exposed along the coast N and S of Innisfail. It is faulted against the mainly Devonian-aged Hodgkinson Formation of the Hodgkinson Province to the W, along the Russell¿Mulgrave Shear Zone (Bultitude et al., 1999). The Barnard Metamorphics are thought to be late Proterozoic¿early Paleozoic: in the S, they host granitoids with U¿Pb zircon ages of 459 +/- 8 Ma and 456 +/- 4 Ma (cited by Bultitude & Champion, 2013), and amphibolite near Mission Beach yielded a U¿Pb zircon age of 451.8 +/- 2.6 Ma for metamorphism (Kositcin et al., 2015a). More recently, however, a schistose metasedimentary rock from a lower grade part of the unit N of Innisfail yielded a maximum depositional age of 427.1 +/- 5.5 Ma (Kositcin et al., 2015b). The most likely explanation for this unexpectedly young age is that these rocks are part of the Hodgkinson Formation which has been tectonically interleaved with the Barnard Metamorphics along the Russell-Mulgrave Shear Zone, raising the possibility of unexplained structural complexity locally. A sample from the S part of this belt of relatively low-grade rocks was collected for dating in order to get a better idea of the extent of these younger rocks, and to compare with previously published provenance spectra for the Hodgkinson Formation (Kositcin et al., 2015b; Cross et al., 2016). The analysed sample comprises mainly very fine-grained (average grainsize 0.2 mm) quartz and muscovite (25-35%), with traces of polysynthetically twinned feldspar, and tourmaline. Triple-point junctions between quartz grains are common. Muscovite forms slender, elongate grains concentrated in thin, irregular lenticles with a pronounced preferred orientation, which defines the macroscopically visible schistosity.
Lewis, C.J., Dhnaram, C.R., Brown, D.D., Bultitude, R.J., Lisitsin, V.A., 2021. Summary of results. Joint GSQ-GA geochronology project: Georgetown, Coen and Cairns regions, 2016-2017. Queensland Geological Record, 2021/05, 62.

The Corella Formation is the main component of the Mary Kathleen Group, which unconformably overlies the Argylla Formation (Derrick et al., 1976, 1977a, b; Hutton & Withnall, 2013) in the northern and central parts of the domain. Igneous rocks from the Argylla Formation yielded several U-Pb zircon dates in the range ~1775-1780 Ma (Neumann et al., 2009; Geoscience Australia, 2011), constraining the maximum age of the Corella Formation to ~1770 Ma. However, ongoing work in the Tick Hill area in the far southern part of the domain suggest calc-silicate rocks currently mapped as Corella Formation (GSQ, 2011) are either intruded by ~1775-1780 Ma and significantly older granitic rocks, or are tectonically interleaved with them (Le, 2020; Dirks et al., 2020; unpublished reports to GSQ). This is not the first time the possibility of the Corella Formation containing rocks older than the Argylla Formation has been mooted. Blake et al. (1978), Bultitude et al. (1978), and Blake (1980, 1982, 1983, 1987) suggested the Corella Formation included an older assemblage, based on apparent interfingering relationships in the southern part of the domain between calc-silicate rocks and granitic gneisses similar to those exposed in the nearby Kalkadoon-Leichhardt Domain to the west. Glassy quartzite ~815 m SW of the abandoned Tick Hill gold mine and mapped as unnamed subunit kc/q of the Corella Formation (GSQ, 2011) was sampled to provide some control on the age of the formation in the southern part of the Mary Kathleen Domain. Feldspathic quartzite east of Duchess previously yielded a maximum depositional age of 1752 +/- 2 Ma (Kositcin et al., 2019). The quartzite near Tick Hill forms low rubbly outcrops on a ridge, in an area of poor outcrop. No relic sedimentary structures were recognised in the quartzite. Nearby outcrops comprise mainly calc-silicate rocks metamorphosed to middle-upper amphibolite grade. The rocks are strongly deformed, commonly with a mylonitic fabric.
Kositcin, N., Purdy, D.J., Bultitude, R.J., Brown, D.D., Hoy, D., 2021. Summary of results. Joint GSQ-GA geochronology project: Mary Kathleen Domain and rocks under younger cover east of the Mount Isa Inlier, 2019-2020. Queensland Geological Record, 2021/01, 112p.

Quandong Conglomerate
The sample was collected from the largest exposure of the Quandong Conglomerate in the core of the Walker Creek Anticline (HENBURY). At this location, the unit is predominantly pebble conglomerate and pebbly sandstone, but it also contains interbeds of sandstone. Sample HB17ND402 is an immature, coarse- to medium-grained, gritty quartz sandstone. Cross beds are common, and bed thickness varies from 10 cm to massive. It is underlain by massive-bedded sandstone of the Areyonga Formation, and overlain by thinly bedded to flaggy, fine-grained micaceous sandstone interpreted to belong to the Winnall Group.

Tempe Formation
Sample HB17CJE561 was collected from low outcrop of Tempe Formation near the base of a moderately sloping low hill. It comprises pale grey to buff coloured sandy dolostone with weak solution weathering. It is weakly laminated and has poorly preserved cross beds in some horizons. Bedding varies ca. 8-15 cm in thickness. At the sample location, the Tempe Formation sits unconformably on poorly exposed Neoproterozoic sedimentary rocks (Loves Creek Formation, Bitter Springs Group); it is overlain in a structural conformity (but with a depositional disconformity) by the Illara Sandstone.

Horn Valley Siltstone
Sample HB17CJE608 was collected from a low ridge of outcrop within a valley formed over this more typically recessive unit. A thin horizon of sandstone crops out at the top of a series of low bench outcrops of calcareous sandstone, sandy limestone and limestone. The sample is a relatively clean, moderately sorted, fine- to medium-grained quartz sandstone. Beds are up to 20 cm in thickness.

Deception Formation
This sample from the Deception Formation comprises dark red-brown, fine-grained micaceous sandstone typical of this unit. Bedding is thin to very thin and planar in style; planar laminations is also commonly present. Some small scale cross-bedding is occasionally observed. The sample location was from outcrop in the bank of a creek. The Deception Formation has a fairly localised distribution. It was sampled in an area where the formations of the Pertaoorrta Group transition from dominantly calcareous (east) to dominantly siliciclastic (west).

Plain Creek Formation
The Plain Creek Formation (McNamara Group, Pma, e.g. Sweet, 1982, 1984; Rawlings et al., 2008) is characterised by micaceous siltstone, shales and sandstone ‘interbeds’, around 400-600m thick (but as much as 1000 m; e.g. Sweet, 1984; Rawlings et al., 2008). The Plain Creek Formation commonly outcrops as cycles of thin beds of fine-grained flaggy sandstones and laminated siltstones (see Rawlings et al., 2008). Current features, such as flute marks and tool marks are common (Rawlings et al., 2008). The Plain Creek Formation is considered a stratigraphic equivalent to the Riversleigh Formation (or Siltstone) of the McNamara Group in the Lawn Hill Platform region in Queensland. Although Sweet (1984) included a basal white massive ‘orthoquartzite’ within the Plain Creek Formation (his Pmas), Rawlings et al. (2008) subdivided the Plain Creek Formation recognising the basal quartzite as a separate, conformably underlying, mappable unit, the Shady Bore Quartzite. The upper contact with the overlying recessive Lawn Hill Formation is invariably concealed (Rawlings et al., 2008) but is ‘presumed to be concordant’. In regions where the Lawn Hill Formation is absent, the Plain Creek Formation is overlain, with a marked angular unconformity, by the Constance Sandstone (Rawlings et al., 2008). The sampled unit is medium-grained feldspathic micaceous sandstone comprised of well-sorted but sub-angular quartz and feldspar grains. Sandstone horizons display distinctive sedimentary pinch-and-swell features resulting in attenuation and dismemberment of the sandy layers. The sample outcrop locality hosts small crosscutting quartz-manganese oxides veinlets containing cryptomelane and pyrolucite. The sandstone also contains dispersed manganese oxide phases. Rawlings et al. (2008) noted that ‘thin veins’ of manganese oxides are common throughout the Plain Creek Formation in MOUNT DRUMMOND.

Widdallion Sandstone Member
The Widdallion Sandstone Member (Pmhw; Hutton et al., 1981; Sweet, 1984; Rawlings et al., 2008) is the uppermost unit in the McNamara Group exposed on MOUNT DRUMMOND, however the unit was first described in Queensland as a member within the Lawn Hill Formation on LAWN HILL (Sweet and Hutton, 1982). The lower contact of the Widdallion Sandstone Member with the Lawn Hill Formation is not exposed but is ‘presumed to be conformable’ (Rawlings et al., 2008). The upper contact with the overlying Playford Sandstone (Wangalinji Sandstone Member) is locally an angular unconformity, whereas elsewhere the contact is interpreted as a disconformity (Rawlings et al., 2008). The member varies in thickness from 50 m to as much as 370 m. The member is characterised by friable brown to purple lithic and micaceous fine- to coarse-grained sandstone and minor laminated siltstone and claystone. Bedding is medium to very thick (several metres) with abundant pebble lags and gritty lenses. Large low-angle trough cross bed sets are common, as are current lineations and ripple marks. At the sample locality, the Widdallion Sandstone Member is a friable texturally immature feldspathic and micaceous, sub-lithic poorly sorted, sub-angular medium- to coarse-grained sandstone. The unit is generally very poorly exposed except along the banks of incised creek beds. Individual beds are up to 10 m thick, and large trough cross beds (5-10 m scale) and soft sediment slumps are common.

Two component mixture modelling used to assist designation of analyses to constitute the weighted mean
Mount Bonner Sandstone
The sample was collected from a prominent rocky peninsular (Bonner Rocks) on the northeastern coastline of Arnhem Land, about 3 km northeast of Mount Bonner and about 32 km northwest of Gove airport. Sample GV16TJM004 was collected from the reference area for the Mount Bonner Sandstone, selected by Plumb and Roberts (1992); note that there is no type section for this unit. The Mount Bonner Sandstone is about 150 m thick, and comprises a localised up-to 50 m-thick basal conglomerate overlain by a fining-upwards succession of typically grey-white, silicified, fine- to medium- to very coarse-grained (locally pebbly) quartz sandstone. The sandstone is trough cross-bedded to occasional massive, and is medium- to thickly bedded. Sample GV16TJM004 is a white to grey, fine-grained silicified quartz sandstone from near the top of the Mount Bonner Sandstone. The Mount Bonner Sandstone is unconformable on most units of the Spencer Creek Group, but only the contact with the Yanungbi Volcanics is exposed. The basal contact is very irregular, apparently overlying a deeply incised palaeotopography. The formation is unconformably overlain by the Balbirini Dolostone (Nathan Group).
Kositcin, N., Munson, T.J., Whelan, J.A., 2017. Summary of results. Joint NTGS-GA geochronology project: greater McArthur Basin, July 2016-June 2017. Northern Territory Geological Survey Record, 2017-012, 64p.

Coast Range Sandstone
The sample was collected from well exposed relatively flat-lying exposures capping a plateau of the Coast Range, about 16 km northeast of the family outstation of Marrkalawa and about 18 km west-southwest of the eastern tip of Haddon Head, which extends into Blue Mud Bay. The type section, selected by Haines in Haines et al (1999), is positioned between 590500mE 8518000mN and 590200mE 8518000mN across the northern part of the Coast Range. The Coast Range Sandstone is a relatively thin unit of sandstone and minor conglomerate, with exposures restricted to northeastern BLUE MUD BAY. In the Coast Range area, the formation can be subdivided into three informal units: a lenticular basal conglomerate; a lenticular brown pebbly, coarse-grained sandstone/granule conglomerate; and a ubiquitous upper unit of medium- to thickly bedded, fine-, medium- and coarse-grained sandstone (Haines et al 1999). Sample BM16TJM029 was collected from the upper unit and is a grey-white, silicified fine-grained sandstone, with pink to light brown weathering surfaces in places

Jalma Formation
The sample was collected from well exposed, gently west-dipping exposures in a creek bed on the western flank of the Coast Range, about 12 km northeast of the family outstation of Marrkalawa and about 21 km southwest of the eastern tip of Haddon Head, which extends into Blue Mud Bay. The sample site is adjacent to the type section of the formation, selected by Haines in Haines et al (1999), which extends from 586500mE 8505100mN (base) northwestwards to 585800mE 8505500mN (top). The Jalma Formation is a succession of sandstone, mudstone and minor carbonate restricted to the western flank of the Coast Range and several small outcrops to the north. The formation is subdivided into a lower, moderately resistant ferruginous sandstone-dominated unit, comprising about two-thirds of the formation, and an upper, very recessive fine-grained unit (Haines et al 1999). Sample BM16TJM041 was collected from near the top of the lower unit and is partly weathered, light to dark grey, brown-weathering fine sandstone. Dark minerals in laminae give a finely spotted texture. The Jalma Formation is undated and the unit is ungrouped. It unconformably overlies the Coast Range Sandstone and locally the underlying Grindall Formation (Arnhem Province), where the unconformity cuts down to that level. The formation is overlain unconformably by the Mesoproterozoic Balbirini Dolostone (Nathan Group); the contact is generally obscured by younger cover, but there is regional evidence that it is truncated (Haines et al 1999).

Nagi Formation
The sample was collected from 10–15 m above the base of the Nagi Formation type section, which is located about 1 km south of Mount Birch in central Urapunga. The sample site is located towards the top of a steep scarp slope on the southern side of a wooded rocky ridge. Exposures consist of discontinuous benches and abundant blocky rubble of medium-bedded, faintly trough cross-bedded, fine- to medium-grained white sandstone. The sample is of a supermature fine-grained quartz sandstone, which consists of generally well-rounded quartz grains, minor (ca 5%) chert, and rare plagioclase, tourmaline and zircon in a quartz authigenic overgrowth cement that occludes porosity.
Kositcin, N., Munson, T.J., 2019. Summary of results. Joint NTGS-GA geochronology project: greater McArthur Basin, July 2017-August 2018. Northern Territory Geological Survey Record, 2019-002, 44p.

Kurbayia Metamorphic Complex
Kurbayia Migmatite
Variably banded stromatic migmatite (leucosome + melanosome) intruded by dykes/sills? of more granitic rock (possibly Kalkadoon Granodiorite?) in the Black Angel Gorge area.
Black Angel Gorge area
Lewis, C.J., Bultitude, R.J., Hutton, L.J., Waltenberg, K., Armstrong, R.A., Evans, N.J., 2018. Unravelling the pre-1860-1850 Ma 'basement' history of the Mount Isa Inlier. Abstract 142, Australian Geoscience Council Convention, 14-18 October 2018.. Australian Geoscience Council Convention, 142, 141p.

The Morstone 1 drillhole, north of the Camooweal to Burketown Road in western Queensland, was drilled by Amalgamated Petroleum in 1963 (Stewart and Hoyling, 1963) on the eastern edge of the South Nicholson Basin. The well penetrated 335 metres of Cambrian limestone overlying 427 metres of sandstone, siltstone and claystone. Stewart and Hoyling (1963) tentatively correlated the lower clastic sedimentary rocks with the (from top down) Paradise Creek Formation, Gunpowder Creek Formation and Myally Subgroup of the Mount Isa Province. The interval sampled for geochronology (538.10-538.25 m) correlates with the Gunpowder Creek Formation (as interpreted by Stewart and Hoyling, 1963), which is a succession of predominantly thin-bedded to laminated siltstone and shale, with minor sandstone, dolostone and chert (Southgate et al., 1999). The unit is interpreted to have been deposited between ca. 1694 Ma and ca. 1658 Ma, based on tuff crystallisation ages from the lower Gunpowder Formation and overlying Paradise Creek Formation, respectively (Page et al., 2000). Page et al. (2000) inferred a time break within the Gunpowder Creek Formation, based on the above age data and differences in stratigraphic character of the lower and upper Gunpowder Creek Formation. However, Withnall and Hutton (2013) suggested that the glauconitic sandstones and finer units described at 376-634 m within Morstone 1 may, instead, correlate with the Mullera Formation of the South Nicholson Group. The sampled unit comprises fine- to medium-grained grey sandstone with thin (typically <1 mm thick) discontinuous laminae of glauconite. No age data currently exists for the well. The sampled interval was targeted for detrital zircon geochronology to further examine the proposed stratigraphic affinities with the Gunpowder Creek Formation (Stewart and Hoyling, 1963), the Mullera Formation (South Nicholson Group, Withnall and Hutton, 2013) or with any other possible stratigraphic units.
Morstone 1

Drill hole GIDPDS5 was drilled by North Limited east of the Millungera Basin near Gidya Creek in November 1994 to investigate a gravity peak within a larger gravity high (Wightman, 1995). The solid geology interpretation shows this area as comprising a small granite intrusion tentatively assigned to the Williams Supersuite (Geological Survey of Queensland, 2018). The vertical hole intersected Wallumbilla Formation (Carpentaria Basin) to 174 m, below which metasedimentary basement rocks were encountered to the bottom of the hole at 342 m. The cored interval is from 188.4 m to T.D. and comprises a fairly monotonous sequence of blue-grey metasandstone. Grainsize is dominantly coarse throughout with only local fine sandstone or silty beds/interbeds and minor pebbly beds. Beds and a strong foliation defined by flattening of quartz grains are flat lying to shallowly dipping. The metasandstone has an overall mature composition and is dominated by quartz grains, and siliceous lithic fragments. The geochronology sample (3316537/DPMI177) is from 337-342 m and was selected to provide an age constraint for the relatively unknown basement assemblage beneath the Carpentaria Basin succession between Mount Isa and Georgetown.

Petermann Sandstone
The Petermann Sandstone has a fairly localised distribution. Sample HB17CJE605 was collected from an area where the formations of the Pertaoorrta Group (which includes the Petermann Sandstone) transition from dominantly calcareous (east) to dominantly siliciclastic (west). Sample HB17CJE605 is a dark red–brown micaceous, ubiquitously cross-bedded sandstone, typical of the Petermann Sandstone across its distribution. It is fine- to medium-grained, and generally poorly sorted. Bedding varies from 6 cm to 15 cm, and the cross-bed sets are of a similar size range. Cross-beds are shallow dipping trough structures.

Goyder Formation
Sample HB17CJE559 was collected from outcrop low on a gentle slope where the Goyder Formation is uncommonly thick and well preserved. Usually the formation outcrops as poorly exposed, thin-bedded, heavily weathered and ferruginised sandstone just below the base of the overlying ridge and cliff-forming Pacoota Sandstone. Sample HB17CJE559 is a fine- to medium-grained sandstone with bedding varying from 8 to 20 cm in thickness. Many bedding surfaces are ripple marked in various forms; shallow, small scale trough cross-bedding is common. Minor sole marking, current lineations, and clay galls are also observed.

Stretton Sandstone
This sample was collected from the base of the Stretton Sandstone in the type section in northwestern Mallapunyah. The sample site is at the base of a 15 m-high scarp of thinly bedded tabular sandstone, which is separated by a few metres of talus slope from the uppermost cherty beds of the Yalco Formation. The sample is of a fine-grained quartz sandstone, consisting of abundant, mostly rounded to sub-rounded quartz, and minor mica and feldspar grains in a siliceous cement.
Kositcin, N., Munson, T.J., 2019. Summary of results. Joint NTGS-GA geochronology project: greater McArthur Basin, July 2017-August 2018. Northern Territory Geological Survey Record, 2019-002, 44p.

Tooganinie Formation
The Tooganinie Formation (Smith 1964) is a thick succession of dolostone and interbedded dolomitic sandstone, siltstone and shale. Exposures are restricted to the Batten Fault Zone in the southern McArthur Basin. The Tooganinie Formation has conformable and gradational lower and upper contacts with the Tatoola Sandstone and Leila Sandstone respectively; it is from the medial Umbolooga Subgroup (lower McArthur Group). The analysed sample was collected from the medial – upper part of the Tooganinie Formation and is an estimated 120 m stratigraphically above the base of reference section 78/01 of Jackson et al (1987), in southwestern Glyde. The sample site is located near the crest of a broad, low, sparsely wooded ridge. Exposures are weathered, low and sparse within alluvium in the vicinity of this locality. The sample is a medium-grained, dolomitic quartz sandstone, containing abundant, mostly rounded quartz and rarer chert and zircon grains, and dolostone/dolomitic siltstone rip-up clasts, in a corrosive dolomitic cement that has partially replaced an earlier siliceous cement. The analysed sample was deposited in an energetic, shallow-water marine environment, possibly adjacent to a carbonate bank from which were derived the carbonate clasts.
Kositcin, N., Munson, T.J., 2019. Summary of results. Joint NTGS-GA geochronology project: greater McArthur Basin, July 2017-August 2018. Northern Territory Geological Survey Record, 2019-002, 44p.

Bowgan Sandstone
The Bowgan Sandstone (Rawlings et al., 2008), represents the basal unit of the South Nicholson Group in the Benmara region (northwest MOUNT DRUMMOND). The contact with the underlying Benmara Group is poorly exposed but is mostly likely a low-angle unconformity (Rawlings et al., 2008) although a layer-parallel faulted contact is also possible. The Crow Formation is thought to lie conformably on the Bowgan Sandstone, although the actual contact zone is recessive and field relationships are not well exposed (Rawlings et al., 2008). The Bowgan Sandstone is generally thin (<100 m, typically ca 10 m; Rawlings et al., 2008) and discontinuous (in places the overlying Crow Formation lies directly on Benmara Group). Rawlings et al. (2008) assume the Bowgan Sandstone is a correlative of the Playford Sandstone (which forms the base of the South Nicholson Group elsewhere), but this lateral correlation is not well established. At the sample location the Bowgan Sandstone forms mildly resistant strike ridges. Rawlings et al. (2008) describe the Bowgan Sandstone as a ferruginous lithic to sublithic fine- to coarse-grained sandstone, exhibiting massive to thick, gently west-dipping (ca 15º) beds with thin pebbly lags and minor 1 m scale cross-beds. Beds are upright and subtle bedforms are present and scattered rounded matrix-supported cobbles occur. A braided fluvial to shallow-marine depositional environment is inferred by Rawlings et al. (2008).

Crow Formation
The Crow Formation (Rawlings et al., 2008) is a largely recessive unit that outcrops poorly throughout the western two-thirds of MOUNT DRUMMOND. The Crow Formation is composed of up to 2500 m of interbedded siltstone, sandstone, shale and lesser conglomerate (Rawlings et al., 2008). Notably Rawlings et al. (2008) highlights the diversity of texturally immature lithological types in the Crow Formation, suggesting that the unit is a proximal facies unit related to derivation from adjacent tectonically uplifted terrains. No previous geochronology has been conducted on the Crow Formation and assumptions about the depositional age is entirely based on the assignment of the Crow Formation to the South Nicholson Group and subsequent correlation of the South Nicholson Group with the Roper Group in the McArthur Basin (ca 1500-1400 Ma). Rawlings et al. (2008) places a tentative correlation of the Crow Formation with the Mainoru Formation of the Roper Group, a unit which contain tuffs dated at ca 1492 Ma (Jackson et al., 1999) which is also briefly noted by Munson (2016). This sample was collected along the measured section described by Rawlings et al. (2008) in the Benmara region (northwest MOUNT DRUMMOND). At the measured section location, Rawlings et al. (2008) reports that the Crow Formation conformably overlies the Bowgan Sandstone; the upper contact with the Mittiebah Sandstone is also conformable. The sampled unit is a tan-coloured moderately-sorted feldspathic quartz ‘gritty’ sandstone, with parting lineations, large scalloped ripple marks (30-40 cm from crest to crest) and flute casts evident on bedding surfaces. Bedding dips moderately to the west (dipping 50º towards 286º).

Four component mixture modelling used to assist designation of analyses to constitute the weighted mean of youngest 18 analyses, other compoent analyses do not have weighted means calculated
The sample was collected from sparse poor rubbly exposure about 1 km south of Central Arnhem Road and about 24 km west of the turnoff to Gapuwiyak. Haines and Pietsch in Rawlings et al (1997) selected a small roadside quarry at 610200mE 8590000mN as a reference locality for this informal unit, but this area is no longer accessible. The Durabudboi beds are composed mainly of weathered and ferruginised, thinly bedded, laminated and flaggy mudstone, which was probably originally dolomitic, minor leached and silicified carbonate rock, which includes relict intraclastic, arenitic, stromatolitic and evaporitic fabrics, and rare fine-grained sandstone. Colour varies from pale purple to buff yellow and white, but exposed surfaces are often dark red due to ferruginisation (Rawlings et al 1997). Overall thickness is unknown, as only a few metres of incomplete section is exposed at most localities. Sample AB16TJM021 is a brown fine-grained silicified sandstone that might have originally been dolomitic.

The sample was collected from well exposed outcrops in a creek bed on a tributary of the Chambers River, about 10 km east-northeast of Beswick. The sample site is about 700 m northeast of the uppermost part of the type section of the formation, selected by Sweet in Abbott et al (2001), which extends from about 306200mE 8386800mN (base) northwestwards to 304900mE 8390700mN (top). The Chambers River Formation comprises mudrocks, siltstone and subordinate sandstone in varying proportions. In the vicinity of the type section, the upper part of the formation consists mainly of well exposed quartz-rich fine- to medium-grained sandstone, and more rarely exposed siltstone and quartz-poor claystone (Walpole et al 1968, Kruse et al 1994). Sample KA16TJM001B was collected from rubbly exposures of medium-bedded fine-grained sandstone near the top of Chambers River Formation, forming part of a northwest-dipping succession of medium-bedded sandstone and interbedded mudrocks that are well exposed in the vicinity of the sample site. The sample is of a grey-purple, purple to light brown-weathering fine-grained sandstone. The Chambers River Formation is the youngest-known component of the Mesoproterozoic Roper Group, as currently defined. However, its age and stratigraphic affinities have not been established with any certainty and are unclear.

Two component mixture modelling used to assist designation of analyses to constitute the weighted mean
The sample was collected from the medial part of the formation in the type section, selected by Sweet et al (1974), which extends from about 664930mE 8088212mN (base) southwestwards to about 664514mE 8087951mN (top) in the Farquharson Gap area, about 35 km northwest of Kalkarindji. The Farquharson Sandstone comprises tabular and blocky, thinly to thickly bedded, typically massive fine-grained sandstone with some interbeds of siltstone in the lower part. The sandstone is poorly sorted and contains planar-tabular and trough cross-beds, wave ripples and abundant rip-up mud flakes (Sweet et al 1974). Sample WH16TJM015 is from nearly flat-lying, thinly bedded exposures along the bed and banks of a small creek and is a grey-light brown, light brown-weathering, fine-grained sandstone with rip-up mud flake layers. The Farquharson Sandstone is part of the medial Limbunya Group, and is conformable with the underlying Kunja Siltstone and overlying Blue Hole Formation. The age of the formation is relatively well constrained by several SHRIMP U-Pb zircon ages from waterlain tuffs of 1635 ± 19 Ma for the underlying Kunja Siltstone (Fanning 1991), and 1636 ± 5 Ma and 1638 ± 9 Ma for the overlying Blue Hole Formation and Campbell Springs Dolostone respectively (Smith 2001). These dates demonstrate a broad equivalence with the McArthur Group, but are indistinguishable within analytical uncertainty and do not enable more detailed correlation at formation level.

Bethungra Formation
Pale olive-green, banded dacite featuring crystal fragments, interpreted as a volcaniclastic rock. In thin section, this sample is a banded, sericite-altered, moderately crystal-rich rhyolite containing 15% crystals (comprising 7% quartz, 5-7% plagioclase, and 3% ex-ferromagnesian minerals, with accessory zircon) in a granophyric to cryptocrystalline matrix. Quartz forms 0.25-1 mm subequant faceted and embayed crystals, as well as rounded and uncommon angular grains. Plagioclase forms 0.5-2.5 mm prisms and lath-shaped crystals, which are largely altered to sericite. A ferromagnesian phase (probably biotite) formed 0.2-0.8 mm blades that are completely altered to sericite and rutile. The unit is part of a package of sandstone, conglomerate, shale, rare felsic volcanic rocks and rare limestone in the NE corner of the Tarcutta 1:100 000 area. In aeromagnetic imagery, the unit forms part of an elongate fault-bounded block up to 2 km wide that extends NW and becomes contiguous with the geophysical domain of the Early Devonian Bethungra Formation (Warren et al., 1995; Eastlake, 2018). The succession is juxtaposed against the Silurian Bumbolee Creek Formation to the NE (Myers, 1982), and the 432.1 +/- 2.1 Ma Junawarra Volcanics to the SW (Eastlake, 2018; see also ERIVMAE1221.01). Stratigraphic control is provided by fish remains within the limestone horizons, which indicate a Pragian (mid-Early Devonian) age (Pickett et al., 1984). Felsic volcanic rocks within the succession encompass moderately crystal-rich, feldspar-quartz phyric coherent rhyolite, to juvenile, poorly-sorted, fine-sand to medium-pebble size rhyolitic breccia. Juvenile clasts in the breccia are closely packed, angular, and vary from jumbled to jigsaw-fit textures. The matrix consists of translucent microcrystalline silica (Eastlake, 2018). This rhyolitic volcaniclastic rock was targeted for U-Pb SHRIMP geochronology to compare isotopic dates from magmatic zircon with the biostratigraphic constraints.
In situ material excavated out of the batter in the SE corner of Blackball Hill quarry, about 650 m E of the intersection of Bethungra Road and Rays Road, and about 3.8 km N of Nangus.
Bodorkos, S., Eastlake, M.A.S., Waltenberg, K., Bull, K.F., Gilmore, P.J., Campbell, L.M., Trigg, S.J., Blevin, P.L., Deyssing, L., Williams, B.J., 2021. New U-Pb SHRIMP zircon ages from the Lachlan Orogen, New South Wales: East Riverina Project, July 2016-June 2020. Geoscience Australia. Record, 2021/08, 321p.

Leila Sandstone
This sample was collected from near the base of the Leila Sandstone in the type section in southwestern Glyde. It is a cross-bedded, fine-grained dolomitic quartz sandstone consisting of abundant subangular to rounded quartz, minor chert and rare zircon grains in a corrosive dolomitic cement. The sample site is a 2 m-thick bench of thinly bedded sandstone at the base of a scarp slope. Jackson et al (1987) suggested a shallow-marine environment of deposition with occasional emergence for the Leila Sandstone.

The Morstone 1 drillhole, north of the Camooweal to Burketown Road in western Queensland, was drilled by Amalgamated Petroleum in 1963 (Stewart and Hoyling, 1963) on the eastern edge of the South Nicholson Basin. The well penetrated 335 metres of Cambrian limestone overlying 427 metres of sandstone, siltstone and claystone. Stewart and Hoyling (1963) tentatively correlated the lower clastic sedimentary rocks with the (from top down) Paradise Creek Formation, Gunpowder Creek Formation and Myally Subgroup of the Mount Isa Province. The interval sampled for geochronology (737.80-738.00 m) correlates with the Myally Subgroup (as interpreted by Stewart and Hoyling, 1963),which comprises the Alsace Quartzite, Bortala Formation, Whitworth Quartzite and Lochness Formation, and together with the Eastern Creek Volcanics, make up the Myally Supersequence (Neumann et al., 2006). Maximum depositional ages indicate deposition occurred after ca. 1780 Ma and had ceased by ca. 1765 Ma (Neumann et al., 2006). As for GA SampleNo 2712850, an alternative correlation for the sequence intersected beneath Cambrian limestone in Morstone 1 is with the South Nicholson Group (Kruse, 2008; Withnall and Hutton, 2013). The sample comprises red-brown, well-sorted, medium- to coarse-grained sandstone. No age data currently exists on the well; this interval was targeted for geochronology to investigate if it belongs to the Myally Subgroup or the South Nicholson Group.
Morstone 1

Liddle Formation
The Liddle Formation is part of the Winnall Group. At its type section in HENBURY, the Liddle Formation overlies the Froud Formation and underlies the Puna Kura Kura Formation. Its maximum thickness in LAKE AMADEUS and BLOODS RANGE is estimated at 500 m. Donnellan and Normington (2017) divided the Liddle Formation into three informal lithofacies (lower, middle and upper). The lower lithofacies is cyclical with thinly, planar-parallel bedded sandstone overlain by medium to thickly bedded, low-angle cross-bedded sandstone; the middle lithofacies is bi-directionally cross-bedded sandstone; and the upper lithofacies is an 'event' facies comprising small-scale trough and festoon cross-bedded sandstone with ripple marks and weathered-out shale clasts. In BLOODS RANGE, the Liddle Formation is exposed in Souths Range, ~60 km NE of Kaltukatjara (Docker River). Here, the Liddle Formation consists of well-bedded, silicified, fine- to coarse-grained sandstone with occasional granule- to pebble-size chert clasts, which is correlated with the lower lithofacies at the type locality in HENBURY. Sample BR19CSV130 is a poorly-sorted, medium-grained sandstone with granule-size clasts; it was collected from the northern base of Souths Range. A precise depositional age for the Liddle Formation has not been determined. In HENBURY, the Winnall Group overlies the Cryogenian Inindia Beds, Aralka Formation or Pertatataka Formation, and underlies the Cambrian Pertaoorrta Group, suggesting an Ediacaran age for the Liddle Formation. LA-ICPMS U-Pb dating of detrital zircons from a sample of Liddle Formation in HENBURY yielded a maximum depositional age of 886 +/- 11 Ma (Normington et al 2018), which is significantly older than the Ediacaran age inferred from stratigraphic position. PSample BR19CSV130 was collected to constrain the age of deposition of the Liddle Formation and to determine if there are any lateral variations in provenance for the unit towards the west.

Liddle Formation
The Liddle Formation is part of the Winnall Group. At its type section in HENBURY, the Liddle Formation overlies the Froud Formation and underlies the Puna Kura Kura Formation. Its maximum thickness in LAKE AMADEUS and BLOODS RANGE is estimated at 500 m. Donnellan and Normington (2017) divided the Liddle Formation into three informal lithofacies (lower, middle and upper). The lower lithofacies is cyclical with thinly, planar-parallel bedded sandstone overlain by medium to thickly bedded, low-angle cross-bedded sandstone; the middle lithofacies is bi-directionally cross-bedded sandstone; and the upper lithofacies is an 'event' facies comprising small-scale trough and festoon cross-bedded sandstone with ripple marks and weathered-out shale clasts. Sample LA19CSV058 was collected from the base of a ridge in southeastern LAKE AMADEUS, ~85 km from Kings Canyon. This outcrop was previously assigned to the Inindia beds (Wells et al 1963) but lithological similarities with the Liddle Formation at its type locality suggest that the outcrop is Liddle Formation. It comprises medium-bedded, poorly-sorted, medium-grained sandstone with granule-size chert clasts. Lithological similarities between this site and Souths Range (BR19CSV130) suggest that LA19CSV058 is of the lower lithofacies. A precise depositional age for the Liddle Formation has not been determined. In HENBURY, the Winnall Group overlies the Cryogenian Inindia Beds, Aralka Formation or Pertatataka Formation, and underlies the Cambrian Pertaoorrta Group, suggesting an Ediacaran age for the Liddle Formation. LA-ICPMS U-Pb dating of detrital zircons from the Liddle Formation in HENBURY yielded a maximum depositional age of 886 +/- 11 Ma (Normington et al 2018), significantly older than the Ediacaran age inferred from stratigraphic position. Sample LA19CSV058 was collected to constrain the depositional age of the Liddle Formation and to determine if there are any lateral variations in provenance towards the west.

Tatoola Sandstone
The Tatoola Sandstone (Smith 1964) is a light coloured, predominantly sandstone unit, mainly consisting of a lower, fine-grained, thinly bedded facies and an upper, medium- to coarse-grained, more thickly bedded sandstone and dolostone facies. The analysed sample was collected from the base of the Tatoola Sandstone type section, which is located about 46 km southeast of Cape Crawford in northeastern Kilgour. The sample site is on a broad, low wooded ridge. Exposures are generally restricted to abundant tabular rubble and less common thin beds. The sample was collected from a dip slope interval of thinly bedded, planar laminated and ripple-marked, fine-grained sandstone. It is a fine-grained quartz-lithic sandstone, containing abundant mostly rounded quartz, lesser chert, and rare muscovite, zircon, glauconite and labile grains in a siliceous cement that has been partially replaced by Fe-oxides. A tuffaceous rock from the Tatoola Sandstone has been dated by SHRIMP U–Pb zircon at 1648 ± 3 Ma (Page et al 2000).

Baiguridji Formation
Sample 2709633 was collected from the east side of Bath Range about 11 km north-northeast of Mount Ranken in southeastern Koolatong. The top of the usually recessive formation is well exposed in this area where it forms steep 25–30 m-high scarps under a cap of Bath Range Formation. The exposed succession comprises thinly to thickly bedded, fine-grained, tabular sandstone, and silicified and leached carbonate rocks. Planar and wavy laminations, ‘pinch-and-swell’ bedding, small-scale hummocky cross-stratification, and minor soft-sediment deformation are present in places. The sample is a fine-grained quartz sandstone from the base of a scarp above a steep rubbly talus slope, on the southern bank of an unnamed east-flowing creek. The sandstone consists mostly of sub-angular to sub-rounded quartz grains, with minor muscovite, chert and other lithic grains, and rare zircon and feldspars in a siliceous cement.

Mount Birch Sandstone
The sample was collected from near the top of the Mount Birch Sandstone a few metres stratigraphically below the concealed contact with the overlying recessive Knuckey Formation, which is exposed in an excavation at this site. The sample site is located about 1 km SSW of Munbililla (Tomato Island) Campsite, in central Urapunga, in the vicinity of a landfill site adjacent to the Nathan River Road. The sample was collected from a steep dip slope on the northern side of a thickly wooded rocky ridge. Exposures of Mount Birch Sandstone at the sampling site consist of rare beds and abundant blocky rubble of trough cross-bedded, fine- to medium- to coarse-grained, cream to light brown sandstone with mudrock rip-up clasts and minor cobble conglomerate. The sample is of a mature, silicified, fine-grained quartz sandstone, consisting of 90–95% sub-angular to well-rounded quartz, 5–10% chert grains, and accessory zircon in a siliceous authigenic overgrowth cement.

Mittiebah Sandstone
Exploration drillhole CRDD001 was drilled by Teck Australia in October 2016, in southern MOUNT DRUMMOND. It was collared in Camooweal Dolostone, and intersected ~569 m of the Georgina Basin stratigraphy, including 467 m of Barkly Group and 101 m of underlying Helen Springs Volcanics, before terminating in "South Nicholson sandstones" (Teck Australia, 2017). The South Nicholson sandstones were tentatively logged as Mittiebah Sandstone. The well completion report (Teck Australia, 2017) emphasises the uncertainty of this interpretation as the prevalence of sandstone in the region, combined with the monotony of the drilled interval, hinders identification of the stratigraphic unit intercepted. Teck Australia (2017) reported that the sandstone below the Cambrian Helen Springs Volcanics, logged as Mittiebah Sandstone(?), is dominated by fine- to coarse-grained quartz and mica-rich +/- lithic sandstones. At 568-621 m, the unit is a micaceous siltstone to lithic-quartz sandstone, while at 621-738 m the unit changes in composition to an overall white fine- to medium-grained sandstone with rare angular glauconitic mud-clasts. The sampled interval (640-641 m) is a massively bedded, creamy white, weakly feldspathic, quartz sandstone, with bands of hematitic staining. In thin section, the sample predominantly comprises well-sorted, medium-sized, rounded to sub-round quartz grains and <10% feldspar grains (mostly altered to fine-grained intergrowths of white mica). Many quartz grains exhibit marked undulose extinction. Secondary quartz is abundant as both interstitial quartz cement and mantles or overgrowths on rounded quartz grains. Minor muscovite is locally present along grain boundaries.

In addition to GA SampleNo 2776714 (depth interval 368.2-369.2 m), a second sample collected from well NTGS02/1 was analysed for U-Pb detrital geochronology with the aim of investigating the variability of age spectra and maximum depositional age of the unit. The sample was collected over a depth interval of 344.80-346.22 m logged as undivided South Nicholson Group (Kruse, 2008; Kruse et al., 2010). The sample selected for geochronology is a cream coloured, medium-grained, silicified quartz-rich sandstone, with a minor lithic component. The interval is moderately- to well-sorted, with sub-round to round quartz grains.
NTGS02/1 Lake Sylvester

In MOUNT DRUMMOND, Rawlings et al. (2008) describe the Surprise Creek Formation as consisting of well-rounded pebble to boulder conglomerate (with rhyolite clasts near the base, presumably Top Rocky Rhyolite), interlayered with sub-lithic to quartz sandstone (displaying small scale trough beds and current lineations) up to 200 m in stratigraphic thickness. The stratigraphic affinity of the Surprise Creek Formation in MOUNT DRUMMOND is ‘unassigned’ (Rawlings et al., 2008). The depositional environment is probably a proximal braided fluvial system, with local alluvial fans (Rawlings et al., 2008). At the sample locality (immediately overlying the unconformable contact with the Top Rocky Rhyolite; Carrara Range Group, ca 1725 Ma) the Surprise Creek Formation is a matrix supported highly silicified, white to tan coloured medium-grained quartz sandstone comprised of well- to moderately-rounded quartz grains (a minor lithic component is present) with interstitial quartz cement. Iron oxides(?) and secondary muscovite are present along grain boundaries. Scattered pebbly lags of rounded quartz clasts are common and rare vesicular rhyolite clasts are present (presumably derived from the underlying Top Rocky Rhyolite).
adjacent to contact with Top Rocky Rhyolite

Shady Bore Quartzite
The Shady Bore Quartzite was first described in Queensland (LAWN HILL and CAMOOWEAL 250K mapsheets, e.g. Hutton et al., 1981), some 100 km east of occurrences in MOUNT DRUMMOND. Sweet et al. (1984) mapped a massive white fine-grained well-sorted quartzite at the base of the Plain Creek Formation, and correlated it with Queensland occurrences of the Shady Bore Quartzite, a correlation supported by later workers (McConachie and Krassay, 1997). Rawlings et al. (2008) formally recognised this basal quartzite as Shady Bore Quartzite. The Shady Bore Quartzite has conformable upper and lower contacts with the Plain Creek Formation and Brumby Formation, respectively. The Shady Bore Quartzite on MOUNT DRUMMOND in the Carrara Range region forms a resistant low ridge which is readily visible and traceable along strike in satellite and aerial imagery. The Shady Bore Quartzite is around 40-50 m thick (Rawlings et al., 2008). The sampled Shady Bore Quartzite is a clean white medium-grained quartz sandstone. Quartz grains are well-sorted, rounded to sub-angular, and mantled by interstitial quartz cement. Bedding is poorly defined. The original rounded grain boundaries of the quartz grains can be readily observed. Rare muscovite is present.

Lawn Hill Formation
Pale grey-green, fine- to medium-grained mica-quartz-feldspar (tuffaceous) sandstone.

Knuckey Formation
The analysed sample was collected from the lower half of the Knuckey Formation type section, which is located about 10 km south-southeast of Mount Vizard in southern Urapunga. The Knuckey Formation is estimated to be about 150 m thick in the type section (Abbott et al 2001); the sample site is estimated to be 30–40 m stratigraphically above the base of the formation. The sample site is located in the bed of an unnamed ephemeral creek; sparse exposures are confined to the creek bed, and consist of low pavements and tabular to blocky rubble of thinly bedded, ripple-marked, fine-grained, light brown sandstone with a surficial dark grey colour. The sample is of a slightly weathered, fine-grained quartz-lithic sandstone, consisting of about 85% poorly sorted, angular to sub-rounded, to rarely well-rounded quartz grains, up to about 15% lithic grains (claystone rip-up clasts and chert grains), minor elongate muscovite, very rare labile grains (plagioclase, amphibole), and accessory zircon. Claystone clasts and muscovite grains tend to be aligned with bedding. Grains and clasts are set in a discontinuous, siliceous, authigenic quartz overgrowth cement that has been partially replaced by iron oxides as a result of weathering.

Mount Birch Sandstone
The sample was collected from near the base of the Mount Birch Sandstone type section, which is located about 1 km south of Nagi Hill in southern Urapunga. The Mount Birch Sandstone is about 80 m thick in the type section. The sample site is located towards the top of a steep scarp slope on the eastern side of a thickly wooded rocky ridge. Exposures consist of extensive benches and abundant blocky rubble of medium- to thickly bedded, trough cross-bedded, medium- to coarse-grained, cream to light brown sandstone. It outcrops a few metres above a 5 m-thick basal conglomerate. The sample is of a slightly weathered, mature, medium-grained sandstone, consisting of about 90% sub-angular to well-rounded quartz, about 10% chert grains and accessory zircon in a siliceous authigenic overgrowth cement.

The sample was collected from the type section in Archies Creek, about 900 m west of its junction with the Kilgour River. The type section was selected by Jackson et al (1987) and extends along the creek banks from about 595679mE 8110285 mN (base) eastwards to about 595966mE 8110163mN (top). The Masterton Sandstone consists of thinly to medium-bedded fine- to coarse-grained quartz and lithic sandstone. A thin pebbly sandstone is at the base of the formation, whereas the topmost beds are transitional with the overlying Mallapunyah Formation and consist of dolomitic sandstone and siltstone with chertified stromatolites. Sedimentary structures include cross-laminations, planar cross-beds, herringbone cross-beds, isolated trough cross-beds, pebble bands, ripples, and desiccation features. Sample WW16TJM014 is a light purple- to brown-weathering, light- to medium-grey fine-grained sandstone from about the middle of the formation. The Masterton Sandstone is the basal formation of the McArthur Group and is unconformable on various units of the Tawallah Group, including the Gold Creek Volcanics, Wollogorang Formation, and Wununmantyala Sandstone. In most areas, the formation is has a gradational conformable contact with the overlying Mallapunyah Formation, but where this formation is absent, the Masterton Sandstone is unconformably overlain by the Karns Dolostone (Nathan Group).

Square Head Formation
Low rubbly outcrop on private property 'Hillcrest', about 600 m NNW of the homestead. The site is 3.5 km SSE of Beness Hill, and about 3 km WNW of Colinroobie. Rocks in this area belong to the Square Head Formation (Colquhoun et al., 2005) and lie within the Beness Syncline. Locally, strata dip 50 to the SE (Trigg, 2018). The rock sampled was described in the field as a weakly foliated sandstone. In thin section, however, this rock appears to be a foliated volcanogenic mudstone (K.F. Bull in Trigg, 2018) featuring 10% angular and irregularly distributed 0.1-0.3 mm quartz crystal fragments, possible lithic grains of siltstone and claystone up to sand-size, and subrounded tourmaline. The foliation is defined by wispy bands of sericite and iron oxide minerals, and some of the bands are kinked. Iron oxide minerals also form clusters and aggregates about the same size as the quartz crystal fragments, and these may have been former ferromagnesian crystals. The matrix is isotropic, and is interpreted as tuffaceous on the basis of its resemblance to recrystallised glass. However, no pyroclasts were recognised, and the presence of lithic grains and subrounded tourmaline grains indicates that the rock is at least in part detrital in origin. Age constraints for the Square Head Formation are limited. It unconformably overlies Early to Middle Ordovician metasedimentary rocks (Trigg, 2017) of the Abercrombie Formation of the Adaminaby Group (formerly the Wagga Group; Deyssing et al., 2018), and is in turn unconformably overlain by the Middle to Late Devonian Barrat Formation (Trigg, 2018). Based on regional correlations, Colquhoun et al. (2005) assigned a late Silurian to Early Devonian age to the Square Head Formation; however, this unit lacks fossils, and this possibly tuffaceous sandstone was targeted for U-Pb SHRIMP geochronology of detrital zircons in order to better constrain its depositional age.
Low rubbly outcrop on private property 'Hillcrest', about 600 m NNW of the homestead. The site is about 3.5 km SSE of Beness Hill, and about 3 km WNW of Colinroobie.

The sample was collected from the eastern coast of the Flinders Peninsula in northern Arnhem Land, about 42 km northeast of Gapuwiyak. Sample AB16TJM005 was collected from the reference section for the Darwarunga Sandstone, selected by Plumb and Roberts (1992); note that there is no type section for this unit. The Darwarunga Sandstone is a 350 m-thick, prominent ridge-forming unit which separates the more recessive Yarawoi and Ulunourwi formations in the medial Habgood Group. The formation is informally subdivided into two units; a lower, very resistant, thinly to medium-bedded, cross-bedded sandstone-dominated succession, and an upper more recessive succession of interbedded sandstone, dolomitic mudstone and minor dolostone. Sample AB16TJM005 is a grey-white, fine-grained silicified sandstone from the top of the lower unit

The sample was collected from the western limb of a south-plunging anticline in northern Arnhem Land, about 13 km northeast of Gapuwiyak. Sample AB16TJM012 was collected from the reference area for the Yarawoi Formation, selected by Plumb and Roberts (1992); note that there is no type section for this unit. The Yarawoi Formation is a 600-700 m-thick, incompletely exposed, mixed succession of dolomitic shale, dolostone and sandstone that is conformable between the Slippery Creek Siltstone (below) and ridge-forming Darwarunga Sandstone in the lower to medial Habgood Group. In the vicinity of the reference area, the formation is informally subdivided into upper and lower, poorly to not exposed, very recessive intervals, separated by a thin, more prominent, ridge-forming quartz sandstone (Plumb and Roberts 1992, Rawlings et al 1991). The lower interval contains dolostone, dolomitic shale, dolomitic sandstone, chert and stromatolitic chert; the medial ridge-forming interval is about 100 m thick and comprises medium- to thickly bedded, massive or cross-bedded, blocky, white to grey, fine- to medium-grained sandstone; the upper interval consists of dolostone interbedded with dolomitic shale and sandstone. Sample AB16TJM012 is a white to grey, fine-grained sandstone from the top of the medial ridge-forming sandstone interval.

Deep Bore Metamorphics
Sample HU17BLR1672 was collected from a grey-coloured gneiss in the Molyhil W-Mo deposit in central Jinka. The Molyhil pit exposes skarn mineralisation associated with metre- to decimetre-scale bodies and veins of variably deformed and altered Marshall Granite intruding calc-silicate rock of the Deep Bore Metamorphics and an unnamed grey-coloured gneiss. The grey-coloured gneiss is the dominant lithology in the pit; however, it is pervasively altered such that its protolith is uncertain. Sample HU17BLR1672 was collected from the grey coloured gneiss that crops out in the northeastern pit wall in order to identify the protolith. The sample is a strongly altered and weathered plagioclase-quartz-biotite-sillimanite-andalusite-ilmenite gneiss with a well-developed foliation defined by biotite and plagioclase. Plagioclase is subhedral to euhedral, medium- to coarse-grained (2-5 mm), and variably altered to sericite. Prismatic sillimanite ranges in length from 3-12 mm and is commonly fibrolitic. Minor andalusite is rarely poikiloblastic with inclusions of quartz and is interpreted to post-date sillimanite. Biotite up to 5 mm is interstitial between plagioclase crystals. Accessory ilmenite is up to 0.5 mm and occurs as inclusions in plagioclase and biotite.
Kositcin, N., McGloin, M.V., Reno, B.L., Weisheit, A., Beyer, E.E., 2018. Summary of results. Joint NTGS-GA geochronology project: Base metal and tungsten mineralisation, and skarn alteration in the Aileron Province, July 2017-June 2018. Northern Territory Geological Survey Record, 2018-009, 34p.

Hole SXDD001 was drilled by Anglo American between June and October 2008 (Kneeshaw & Haker, 2009; CR56771) to test a SQUID (Super conducting QUantum Interference Device) EM target. The drilling cost was subsidised by the Queensland Department of Mines and Energy Collaborative Drilling Initiative programme. The drill hole is located west of the Flinders River between Clean Skin and Sandy Creek bores, on Wondoola Station. The current basement geology interpretation shows this area as comprising either Mount Fort Constantine Volcanics or Corella Formation (Geological Survey of Queensland, 2018). The hole was orientated at 70 degrees towards 270 degrees and intersected metamorphic basement below the Mesozoic cover sequence at 474.5 m before terminating at 712 m. The upper part of the basement interval is dominated by strongly metasomatised and altered calc-silicate rocks, which are locally cut by pegmatite dykes that become thicker down the hole. A fault at ~667.5 m separates these rocks from an interval of strongly foliated biotite schist, psammite and foliated pegmatite. We sampled a quartzose metasandstone from this interval (sample 3316533/DPMI178b, 693.3-696.5 m) to place an age constraint on deposition of the basement rocks in this area. The sandstone is foliated and consists mainly of strained quartz and altered feldspars. Zircon grains are relatively large and rounded.

Bath Range Formation
The sample was collected from a reference section for the Bath Range Formation (Haines et al 1999), about 7 km northeast of the junction of Vaughton Creek and Rose River in south-central Parsons. The sample site is located on the bed and banks of a small shallow gully on the southern flanks of a broad, low, thickly wooded ridge. It is from near the top of the unit, but the stratigraphic position cannot be accurately determined due to discontinuous recessive exposures and low dips along this section. The sample was collected from a poorly exposed succession of weathered, thinly to medium-bedded fine-grained sandstone with occasional trough cross-beds and rare synaeresis cracks. It is a laminated, fine-grained, poorly sorted silty sandstone, consisting of abundant angular to subrounded quartz and minor chert grains, with rare muscovite, zircon and labile grains, in a porous, quartz-rich siltstone matrix.

Mount Philp Breccia
Polymictic, matrix-supported, magmatic–hydrothermal? breccia, consisting of randomly oriented, angular to rounded fragments and larger ‘rafts’ of country rocks dispersed in a pink to red or, more rarely grey, fine-grained matrix, is exposed at several localities in the southern part of the Mount Isa Inlier, mainly northeast and southeast of Duchess. The largest (ca. 14.5 km2) of these breccias is located ca. 45 km north-northeast of Duchess. The sample (2808850/BB5944) collected for dating is from the matrix of this body, which has a north-northeasterly elongation parallel to the regional structural trend of the enclosing Corella Formation. The matrix is non foliated and has not been recrystallised or deformed to any significant degree (except in and adjacent to faults and shear zones), therefore implying the breccia formed after the enclosing Corella Formation had been deformed and regionally metamorphosed to amphibolite grade. The sample was collected from an extensive pavement in the bed of the Malbon River. The breccia matrix at this locality is grey to pinkish grey, massive, and fine-grained except for the numerous and conspicuous dark green, euhedral–subhedral amphibole (tremolite–actinolite?) grains, which range from <1 cm up to ca. 5 cm in length (most <3 cm). A range of rock types is represented in the clasts, including coarse amphibolite (up to ca. 35 cm across), granite and pegmatite (up to ca. 1.5 m), and calc-silicate rocks (up to ca. 3 m across).
pavement in bed of Malbon River
Kositcin, N., Bultitude, R.J., Purdy, D.J., 2019. Summary of results. Joint GSQ-GA Geochronology Project: Mary Kathleen Domain, Mount Isa Inlier, 2018-2019. Queensland Geological Record, 2019/02, 81p.

Puna Kura Kura Formation
The Puna Kura Kura Formation is the uppermost unit in the Winnall Group. At the type section in HENBURY, the Puna Kura Kura Formation comprises well-sorted and well-rounded feldspathic sandstone (Donnellan and Normington 2017). Bedding is cyclic up-succession, varying from thin- to medium-bedded with tabular angular cross-beds, to massive to medium-bedded then predominantly thin-bedded sandstone. Weathered-out shale clasts are common in the thin- and medium-bedded units, particularly near the base of the formation, and are commonly associated with ripple marks. Within the Puna Kura Kura Formation, the Chookla Member is a poorly sorted, clast- to matrix-supported conglomerate with pebble-, cobble- and small boulder-size clasts of quartzite, vein quartz and minor basement rock (Normington et al 2018). In LAKE AMADEUS, the Puna Kura Kura Formation forms a ridge ~35 km SW of Kings Canyon. Sample LA19CSV060 collected at this location is a dark red, medium-bedded, poorly-sorted, medium-grained feldspathic sandstone. A precise depositional age for the Puna Kura Kura Formation has not been determined. In HENBURY, the Winnall Group overlies the Cryogenian Inindia Beds, Aralka Formation or Pertatataka Formation, and underlies the Cambrian Pertaoorrta Group. At the type locality, the Puna Kura Kura Formation unconformably overlies the Liddle Formation, and possibly correlates with the late Ediacaran Arumbera Sandstone of the Pertaoorrta Group. In HENBURY, LA-ICPMS U-Pb detrital zircon dating of the Puna Kura Kura Formation and the Chookla Member indicate maximum depositional ages of 959 +/- 7 Ma and 620 +/- 5 Ma respectively (Normington et al 2018). The former is significantly older than the Ediacaran age inferred from stratigraphic position, but the latter is consistent with an Ediacaran depositional age (Normington et al 2018). Sample LA19CSV060 was collected to constrain the age of deposition, and any lateral variations in provenance for the unit towards the west.

Liddle Formation
The Liddle Formation is part of the Winnall Group. At its type section in HENBURY, the Liddle Formation overlies the Froud Formation and underlies the Puna Kura Kura Formation. Its maximum thickness in LAKE AMADEUS and BLOODS RANGE is estimated at 500 m. Donnellan and Normington (2017) divided the Liddle Formation into three informal lithofacies (lower, middle and upper). The lower lithofacies is cyclical with thinly, planar-parallel bedded sandstone overlain by medium to thickly bedded, low-angle cross-bedded sandstone; the middle lithofacies is bi-directionally cross-bedded sandstone; and the upper lithofacies is an 'event' facies comprising small-scale trough and festoon cross-bedded sandstone with ripple marks and weathered-out shale clasts. Sample LA19CSV141 was collected from the top of the western part of Winnall Ridge, ~60 km SW of Kings Canyon. Outcrop generally consists of fine- to medium-grained, cross-bedded sandstone. The sample is a grey, medium-grained, cross-bedded sandstone. Abundant bi-directional cross-beds suggest correlation with middle lithofacies of the Liddle Formation at its type locality in HENBURY (Donnellan and Normington 2017). A precise depositional age for the Liddle Formation has not been determined. In HENBURY, the Winnall Group overlies the Cryogenian Inindia Beds, Aralka Formation or Pertatataka Formation, and underlies the Cambrian Pertaoorrta Group, suggesting an Ediacaran age for the Liddle Formation. LA-ICPMS U-Pb dating of detrital zircons from the Liddle Formation in HENBURY yielded a maximum depositional age of 886 +/- 11 Ma (Normington et al 2018), significantly older than the Ediacaran age inferred from stratigraphic position. Sample LA19CSV058 was collected to constrain the depositional age of the Liddle Formation and to determine if there are any lateral variations in provenance towards the west.

Shillinglaw Formation
The sample was collected from the lower part of the upper lithofacies in the type section of the Shillinglaw Formation. The sample locality is about 13.5 km west of Renner Springs in central Helen. The upper lithofacies in the type section is recessive and sparsely exposed as subtle benches and tabular rubble in low to moderate-relief undulose hills; it is estimated to be 300–400 m thick in this area. The sample was collected from a low, shallowly dipping (ca 5° NE) pavement of light brown- weathering, medium-grained grey-pink sandstone, which is estimated to be 60–90 m stratigraphically above the base of the lithofacies. The sample has a mature composition and contains 90–95% well-rounded to sub-rounded to rarely sub-angular quartz grains, 5–10% rounded chert grains, and accessory zircon. These are set in a well-developed siliceous, authigenic quartz overgrowth cement; a siliceous, drusy cavity-fill replaces earlier porosity in some places.
Tennant Creek Region

Carruthers Formation
The sample was collected from the uppermost ridge-forming sandstone lithofacies, from the nose of a north-plunging faulted anticline, which is located about 11 km west-southwest of Renner Springs in south-central Helen. The upper lithofacies is estimated to be approximately 120 m thick in this section where it is dominated by thinly to medium-bedded, fine- to medium-grained sandstone. The sample site is estimated to be 50–60 m stratigraphically below the top of the formation, and is on a ca 20° dip slope near the top of a spinifex-covered rocky ridge. Sandstone at the sample site consist of low pavements and tabular rubble of thinly bedded fine- to medium-grained, light brown-weathering, cream to light mauve sandstone. The sample is fine-grained and has a mature composition; it contains 90–95% mostly well-rounded to sub-angular quartz grains, 5–10% rounded chert grains, rare muscovite and glauconite, very rare amphibole and accessory zircon. These are set in a siliceous, authigenic quartz overgrowth cement that has been replaced by iron oxides (weathering) in some places.

This sample was collected from drillhole NTGS02/1, in the Georgina Basin (Kruse, 2008). The interval 342.9-371.2 m intersected pre-Georgina Basin rocks, comprising flat-lying, coarse-grained quartz sandstone with rare thin interbeds of pale green mudstone and multiple horizons of cross-beds and "bedding-parallel pebbles" near end of hole. Kruse et al. (2010) provisionally assigned this interval to the (undivided) South Nicholson Group. Most U-Pb zircon maximum depositional ages for the South Nicholson Group have been obtained from the eastern South Nicholson Basin, and span the range ca. 1750-1570 Ma (Jackson et al., 1999; Page et al., 2000; Carson et al., 2011; Magee et al., 2013). LA-ICP-MS detrital zircon U-Pb age data from three other undifferentiated South Nicholson Group sandstones (in drillholes AY06DD01, NTGS00-1 and NTGS01-1 in the SW South Nicholson Basin; Yang, 2019) yielded maximum depositional ages (based on each youngest single grain) of 1542 +/- 69 Ma, 1550 +/- 52 Ma and 1519 +/- 51 Ma respectively (2sigma; Yang, 2019). In addition, Anderson et al. (2019a, b) and Kositcin and Carson (2019) bracketed deposition of the South Nicholson Group between ca. 1483-1470 Ma and ca. 1266 Ma, based on SHRIMP U-Pb zircon and xenotime geochronology, indicating a temporal correlation with the Roper Group in the McArthur Basin. This sample was obtained from NTGS02/1 at a depth interval of 368.2-369.2 m. It is a cream to pink, fine- to medium-grained, moderately well-sorted quartz sandstone which contains cracks and lenses of cream coloured clay and minor red alteration halos. The aim is to establish the presence of South Nicholson Group beneath the Georgina Basin, west of all known exposures, and to enable stratigraphic correlations and provenance studies. Drillhole NTGS02/1 is located on the 2017 deep reflection seismic line (19GA-B1, Carr et al., 2019) and thus facilitates regional geological interpretations of units underlying the Georgina Basin.
NTGS02/1 Lake Sylvester

Pinkish-grey and black banded migmatitic gneiss, comprising Sampled interval is complex and heterogeneous but is representative of package as a whole. Strong fabric development and metamorphism. Sample taken from this interval because it incorporates previous samples within the same interval (2018339536 and 2018339537 [2786115]) which have visible zircon in thin section. The latter sample has yielded an in-situ SHRIMP U-Pb monazite date of c. 1844 Ma, interpreted to constrain the age of peak metamorphism. No lower contact (i.e. same rock continues). Upper contact is a hematitic, broken shear zone. Contact relationship left in core tray, but entire remaining (quarter) core taken. Some small representative pieces left for reference, including previous sample offcuts. Sampled for U-Pb zircon geochronology to constrain age of rock (detrital age spectrum, and maximum depositional age) and compare potential migmatitic/metamorphic ages to the in-situ U-Pb monazite metamorphic age of c. 1844 Ma previously obtained on sample 2018339537 [2786115] (168.89-169.04 m).
Cross, A.J., Clark, A.D., Schofield, A., Kositcin, N., 2020, New SHRIMP U-Pb zircon and monazite geochronology of the East Tennant region: a possible undercover extension of the Warramunga Province, Tennant Creek. IN: Czarnota, K., Roach, I., Abbott, S., Haynes, M., Kositcin, N., Ray, A. and Slatter, E. (eds.), Exploring for the Future: extended abstracts. Geoscience Australia. Record, 4.

Bangus Formation
Dark greenish-grey, foliated and metamorphosed, mafic-looking rock. In outcrop, the foliation is defined by elongate feldspar-rich lenses up to 1.5 x 8 mm, interspersed with medium-grained (0.5-3.0 mm) mafic porphyroclasts that comprise 15% of the rock. Euhedral amphibole is prominent in some porphyroclasts. In thin section, this deformed, poorly sorted mafic metasandstone contains relict detrital plagioclase (20%), ferromagnesian mineral grains (8%), and rare lithic clasts, in a dynamically recrystallised matrix. It is compositionally immature, and termed an arkose based on porphyroclast content. Plagioclase is the most abundant relict detrital component, and includes subangular to subrounded grains, as well as unmodified prismatic crystals. Brownish-green hornblende forms subangular to subrounded grains, some with simple twins. Epidote pseudomorphs replace subequant mineral grains less than 1.5 mm across, some of which preserve eight-sided cross sections, and may have been calcic pyroxene. Lithic fragments are commonly rounded. A continuous secondary foliation defined by fine-grained actinolite, chlorite, minor epidote and opaque oxide minerals wraps the porphyroclasts, and indicates that deformation occurred under greenschist facies conditions. Eastlake (2018) assigned these rocks to the mid-Silurian Bangus Formation (which includes the 'Bangus volcaniclastics' of Wyborn, 1996). W of Adelong, a metamorphic aureole in the Bangus Formation (Eastlake, 2020) reflects emplacement of the 432.0 +/- 1.9 Ma Wondalga Granodiorite (ERIVMAE1820.01), ostensibly imposing a minimum age on the Bangus Formation. The compositional immaturity of the Bangus Formation implies a proximal source region of intermediate composition. One candidate is the 432.1 +/- 2.1 Ma Junawarra Volcanics (ERIVMAE1221.01) which abuts the Bangus Formation to the NE; another is the Nacka Nacka Metabasic Igneous Complex, for which Glen (2013) cited an unpublished U-Pb LA-ICPMS zircon date of 438 +/- 3 Ma.
Water-worn pavements on E bank of Nacki Creek, about 20 m N of the bridge linking private properties 'Bangadang' and 'Mount Adrah'. The site is about 200 m NNW of the homestead on 'Bangadang', and 2.6 km NNE of the intersection of the access road with the Snowy Mountains Highway.

Bethungra Formation
Mauve to purplish-brown, crystal-poor rhyolite containing about 10% sand-sized feldspar and quartz crystals and fragments, interpreted as a volcaniclastic rock. The matrix is aphanitic and locally displays weak banding. In thin section, this sample is an extremely altered ignimbrite. Crystals and crystal fragments constitute 7% of the rock, and comprise quartz, K-feldspar and plagioclase in subequal abundance. Some crystals are broken, but many are not. K-feldspar is altered to brown clay minerals, and plagioclase to sericite. Quartz is variably embayed. Rare ferromagnesian minerals are less than 1 mm and altered to iron oxide minerals, but rare pseudomorphs with prismatic- and diamond-shaped outlines suggests the primary phase was amphibole. The unit is part of a package of sandstone, conglomerate, shale, rare felsic volcanic rocks and rare limestone in the NE corner of the Tarcutta 1:100 000 area. In aeromagnetic imagery, the package is part of an elongate fault-bounded block up to 2 km wide that extends NW until it becomes contiguous with the geophysical domain of the Early Devonian Bethungra Formation (Warren et al., 1995; Eastlake, 2018). Stratigraphic control is provided by the limestone horizons, where fish remains indicate a Pragian (mid-Early Devonian) age (Pickett et al., 1984). Felsic volcanic rocks encompass moderately crystal-rich, feldspar-quartz phyric coherent rhyolite, to juvenile, poorly-sorted, fine-sand to medium-pebble size rhyolitic breccia. Juvenile clasts in the breccia are closely packed, angular, and vary from jumbled to jigsaw-fit textures. The matrix consists of translucent microcrystalline silica (Eastlake, 2018). This rock was targeted for U-Pb SHRIMP geochronology to compare isotopic dates from magmatic zircon with the biostratigraphic constraints. A similar sample from the same unit, collected at Blackball Hill quarry 13 km to the NW, yielded a maximum age of 416.6 +/- 2.3 Ma for deposition (ERIVMAE1821.01).
Outcrop at the top of an embankment on the W side of a S-draining gully on private property 'Bangawalla', about 100 m W of Tumblong Reserve Road, and 1.7 km N of its intersection with the Old Hume Highway, about 3 km WNW of the locality of Tumblong.

pelitic and psammitic sedimentary rocks 74240

Acacia Sandstone Member
MCLARTY HILLS_136069.1
Canning Region
Wingate, MTD 2007, 136069: quartz sandstone, Looma 1; Geochronology Record 656: Geological Survey of Western Australia, 5p.

The Liddle Formation is part of the Winnall Group (formerly Winnall beds of Ranford et al 1965, redefined by Donnellan and Normington 2017). The formation is exposed in generally northwest-striking ridges in the central and western parts of the Amadeus Basin. At its type section in HENBURY, the Liddle Formation is overlain by the Puna Kura Kura Formation, the uppermost part of the Winnall Group. The Liddle Formation is probably late Ediacaran based on its stratigraphic position (Donnellan and Normington 2017). A previous sample of the Liddle Formation from BLOODS RANGE produced a detrital zircon maximum depositional age of 696 +/- 13 Ma (Beyer et al., 2020). Sample BR19VJN037 is a thick-bedded, medium-grained sandstone collected from a small hill ~20 km southwest of Souths Range. It is laminated, and displays minor cross-stratification.
Kositcin, N., Verdel, C., Normington, V.J., Simmons, J.M., 2021. Summary of results. Joint NTGS-GA geochronology project: western Amadeus Basin, July-August 2020. Northern Territory Geological Survey Record, 2021-002, 25p.

Carnarvon Region

Waddikee Rocks gneiss
granitic gneiss

Warrow Quartzite

The sample was taken from very-fined-grained sandstone-siltstone beds in overall mudstone package, containing distinct graded bedding in beds up to 5 cm thick. This sample was collected to provide a maximum depositional age of an unnamed silty mudstone unit within the Georgetown Inlier. Dating these rocks was thought to provide a maximum depositional age of the upper stratigraphy within the Georgetown Inlier. The sample was collected from the A2 Prospect, near Croydon, by David Huston (Geoscience Australia).

Biscay Formation
GORDON DOWNS_206185.1
Lu, Y, Wingate, MTD, Maidment, DW and Hollis, JA 2017, 206185: feldspathic metasandstone, Duncan Highway; Geochronology Record 1388: Geological Survey of Western Australia, 5p.

This sample was collected from the northern part of the Marimo–Staveley Domain in the Slaty Creek area where slices of Answer Slate (dominantly carbonaceous cleaved mudstone) alternate with Staveley Formation (typically calcareous sandstone and siltstone passing into calc-silicate granofels). Some slices of Roxmere Quartzite (mostly very thick bedded, amalgamated lithic sublabile sandstone) also occur. The outcrop sampled consists of well-sorted, very thick-bedded, medium- to coarse-grained, quartzofeldspathic sandstone to granule conglomerate. The beds are mostly massive, but rare crossbedding is present. In thin section, the sample consists of a mosaic of interlocking quartz and subordinate feldspar grains 0.05–0.25 mm and accessory opaque oxides grains. The absence of mica indicates that the sandstone was originally well sorted with no clay matrix. The rocks are currently mapped within a less carbonaceous subunit Answer Slates as depicted on the Marraba 1:100 000 Geological map (Withnall et al., 2015). That subunit is described as “brown phyllite or fine-grained mica schist and graphitic slate” on the map legend, and because such massive, coarse-grained sandstone as observed in 2017 at this site and several other sites are not typical of either the Staveley Formation or Answer Slate in general, we speculated that they might represent slices of Roxmere Quartzite. Common outcrops of ribbon quartz suggest that unmapped faults transect the unit.
Kositcin, N., Lewis, C.J., Withnall, I.W., Slade, A.P., Sargent, S., Hutton, L.J., 2023. Summary of results. Joint GSQ-GA Geochronology Project: Mount Isa region, 2017-2018. Geoscience Australia. Record, 2023/32, 97p.

NELSON, D. R., 2001, 169118: metasandstone, Fandango Prospect; in Compilation of geochronology data, 2000: Western Australia Geological Survey, Record 2001/2, p. 189-193.

Carson Volcanics
Lu, Y, Wingate, MTD, Kirkland, CL, Maidment, DW, Phillips, C and Hollis, JA 2016, 206165: quartz-feldspar arenite, Teronis Gorge; Geochronology Record 1344: Geological Survey of Western Australia, 6p.

Quartzite

Sixty-two analyses were undertaken on 62 zircon grains. One analysis with a common 206Pb content higher than an arbitrary value of 0.5% was considered unreliable, and was removed from further consideration. The remaining 61 analyses are characterised by a wide range of U contents (49-786 ppm), Th contents (35-555 ppm) and Th/U (0.26-2.22). The analyses record 207Pb/206Pb ages between ~3428 Ma and ~1288 Ma, with dominant age clusters at ~1780 Ma and ~1680 Ma, and smaller peaks at ~1380 Ma and at ~1310 Ma. The youngest individual age (from 079.62.1.1) forms part of this youngest cluster, and the weighted mean age for this group is 1309 +/- 10 Ma (95% confidence; n = 10; MSWD = 1.2; probability of fit = 0.29). This weighted mean age is used to define the maximum depositional age for this sample. The weighted mean 207Pb/206Pb age of 1309 +/- 10 Ma (95% confidence) obtained from the youngest cluster of 10 analyses is used to define the maximum age for deposition of this sandstone.
?Lefroy Formation
GSWA Empress 1A
Korsch, R.J., Blewett, R.S., Pawley, M.J., Carr, L.K., Hocking, R.M., Neumann, N.L., Smithies, R.H., Quentin de Gromard, R., Howard, H.M., Kennett, B.L.N., Aitken, A.R.A., Holzschuh, J., Duan, J., Goodwin, J., Jones, T., Gessner, K., Gorczyk, W., 2013. Geological setting and interpretation of the southwest half of deep seismic reflection line 11GA-YO1: Yamarna Terrane of the Yilgarn Craton and the western Officer Basin. In: Neumann, N.L. (ed.) Yilgarn Craton-Officer Basin-Musgrave Province Seismic and MT Workshop. Geoscience Australia. Record, 2013/28, 24-50.

Macquarie University
Age is the youngest significant peak. Three clusters were identified in the youngest sub-population (~ 435, ~ 445 and ~ 455 Ma).
Trigalong Formation
Tilhac 2019 paraphrased "The sample is a meta-Sandstone with two main morphological zircon populations. (1) Euhedral to subhedral crystals with elongations ranging from 1:2 to 1:4. (2) Mostly stubby, rounded crystals. Some inclusions in both populations. Mostly pale yellow. Very dominantly oscillatory zoned, some core-rim and diffuse features, especially in the rounded population; a few sector zoned.
Tilhac, R. (2019). Zircon U-Pb dating: TerraneChron report to the Geological Survey o fNew South Wales (TC-182). CCFS and GEMOC Macquarie University. Geological Survey of New South Wales, Maitland. File GS2019/0446.

130 analyses give a prominent complex peak at ~1780Ma & ~1695 & 1860Ma peaks. 2 isolated grains younger than 1590Ma are not considered further, and youngest 10 grains define a population with a weighted mean 207Pb/206Pb age of 1616 ? 16 Ma
Tidna Sandstone
LAWN HILL_ISSNG_047

Bluish grey fine to medium grained quartzose-feldspathic sandstone, thin to thickly bedded, laminated in parts. Cross-cut by small granite veins in places. Dating Objective: Maximum age of deposition.
Lewis, C.J., Withnall, I.W., Hutton, L.J., Bultitude, R.J., Slade, A.P., Sargent, S., 2020. Summary of results. Joint GSQ-GA geochronology project: Mount Isa region, 2016-2017. Queensland Geological Record, 2020/01, 71p.

Age taken from GSNSW's MinView. Not directly reported in Meffre et al 2007
Adaminaby Group
Quartz-rich sandstone
Meffre S., Scott R.J., Glen R.A. & Squire R.J. (2007) Re-evaluation of contact relationship between Ordovician volcanic belts and the quartz-rich turbidites of the Lachlan Orogen., Australian Journal of Earth Sciences 54, 363-383.

MacDougall Formation
Kirkland, CL, Wingate, MTD, Smithies, RH, Howard, HM and Quentin De Gromard, R 2014, 201307: metasandstone, Yulun-Kudara Waterhole; Geochronology Record 1222: Geological Survey of Western Australia, 4p.

Nelson, DR 2002, 154880: sandstone, Pirrilyungka Outstation; Geochronology Record 259: Geological Survey of Western Australia, 4p.

psammite (metasandstone) (mt)

gneiss
Kirkland, CL, Bodorkos, S and Wingate, MTD 2009, 183596: laminated paragneiss, Mount Fanny; Geochronology Record 758: Geological Survey of Western Australia, 5p.

A more conservative estimate of the maximum depositional age can be based on the weighted mean 207Pb*/206Pb* date of 579 +/- 4 Ma, MSWD = 0.76. N = five youngest analyses
Wilson Cliffs Sandstone
Wingate, MTD and Haines, PW 2009, 135964: sandstone, Wilson Cliffs 1; Geochronology Record 779: Geological Survey of Western Australia, 5p.

Group S comprises 50 analyses (Table 1), which yield 207Pb*/206Pb* dates of 3176-2382 Ma. A more conservative estimate of the maximum depositional age can be based on a weighted mean 207Pb*/206Pb* age of 2453 +/- 13 Ma (MSWD = 1.7) for the youngest coherent group of six analyses in Group S.
Beasley River Quartzite
Ashburton Region
Wingate, MTD, Lu, Y, Sircombe, K, Kirkland, CL and Johnson, SP 2017, 203710: quartzite, Miningee Well; Geochronology Record 1355: Geological Survey of Western Australia, 5p.

Strelley Pool Formation
MARBLE BAR_178043.1
Nelson, DR 2005, 178043: lithic-quartz sandstone, Strelley Pool; Geochronology Record 565: Geological Survey of Western Australia, 5p.

Subunit/q
The sample was collected from a lens, up to ca. 5 m thick, of pale brown to pale reddish brown, medium- to thick-bedded, medium-grained, even-grained, feldspathic quartzite in an assemblage of mainly muscovite schist and micaceous quartzite. The assemblage dips gently to the east and is cut by a steeply dipping–subvertical, northerly trending foliation. The feldspathic quartzite is relatively resistant to erosion and forms a prominent ridge with a narrow crest ca. 2.7 km east of Duchess.
Prominent ridge on northern side of main Duchess-Cloncurry road, ~2.7 km east of Duchess.
Kositcin, N., Bultitude, R.J., Purdy, D.J., 2019. Summary of results. Joint GSQ-GA Geochronology Project: Mary Kathleen Domain, Mount Isa Inlier, 2018-2019. Queensland Geological Record, 2019/02, 81p.

Sericite overprinted, muscovite-biotite-opaques quartzite, collected for U-Pb geochronology. In thin section, this sample displays an inequigranular granoblastic metamorphic texture, with indistinct foliation defined by widely spaced white mica aggregates and trails. Quartz dominates the rock, forming small to large anhedral grains ~0.1-1.0 mm in size. Larger grains display equant anhedral shapes that are reminiscent of primary clastic particles. Smaller grains form microgranular mosaics around the grain margins, and appear to represent recrystallisation mosaics. White mica occurs in two textural types: i) Some forms well-shaped larger plates ~0.4-1.0 mm long scattered throughout the rock. A weak preferred orientation defines a structure of unknown origin, either a metamorphic foliation or possibly a primary layering. ii) Small flakes of white mica are present throughout the rock. Some occur as small dense replacements of anhedral plagioclase grains. Some small anhedral relict plagioclase grains are preserved in these sites. These plagioclase grains have suffered partial to complete replacement by fine-grained white mica. Much of the fine-grained white mica also occurs as diffuse concentrations in ragged to elongated wispy patches up to several millimetres in size whose preferred orientation defines another structure, discordant to the weak alignment of the larger muscovite plates. This structure appears to be of retrogressive metamorphic origin. Biotite occurs in trace amount as small pleochroic brown to very pale yellow flakes that tend to be concentrated in local small aggregates. Opaques occur in minor amount as small blocky grains ~0.1-0.2 mm in size that are disseminated sparsely throughout the rock. Zircon occurs in significant amount for an accessory phase.

Strongly foliated, fine- to medium-grained metasandstone with abundant chlorite and muscovite. The sample comprises 10-15% grains of strained quartz and lesser sericitized plagioclase about 0.5 mm in diameter in a matrix of anhedral granular quartz, plagioclase, pale orange-brown biotite, muscovite and opaque minerals £0.05 mm. Scattered grains of anhedral to subhedral zircon are evident. A weak schistosity defined by seams of muscovite and biotite, some of which are crenulated.
Bodorkos, S., Sheppard, S., Saroa, D., Tsiperau, C.U., Sircombe, K.N., 2013. New SHRIMP U-Pb zircon ages from the Wau-Bulolo region, Papua New Guinea: July 2012-June 2013. Geoscience Australia. Record, 2013/25, 56p.

Nelson, DR 2002, 154881: sandstone, Pirrilyungka Outstation; Geochronology Record 260: Geological Survey of Western Australia, 4p.

Fine silty sandstone. Dwyer et al 2018 paraphrased: "Sample RTD7 is a metasedimentary rock obtained from within the magnetic anomaly zone and interpreted to be interbedded with the Louth Volcanics...(it) is a poorly outcropping metasedimentary rock isolated by Quaternary floodplain deposits. It was originally assigned as a possible Cobar Group metasediment by Loudon, Menzies, and Wallis (1965), with the rocks within the outcrop described as ‘contorted quartzite, sandstone, phyllite and slate.’ The RDT 7 outcrop, located within a prominent magnetic feature that is related to the Louth Volcanics, is subvertically bedded, contains a strong cleavage and is likely to be part of the Louth Volcanics package. Tuffs and intrusive calc-alkaline dolerites exist within drill holes MINOL33, MINOL30 and MINOL21, which are located within the geophysical anomaly associated with the Louth Volcanics. In associated tuffs, sedimentary rocks and field samples, bedding parallel and axial planar fabrics were observed (MINOL21-05, MINOL30-04, MINOL33-06, RDT7)."

Hannover South 1

metafelsic volcanic rock (mf)
Wingate, MTD, Bodorkos, S and Van Kranendonk, MJ 2009, 180095: felsic volcaniclastic metasandstone, Pioneer Mine; Geochronology Record 812: Geological Survey of Western Australia, 5p.

interlayered pelitic and psammitic schist, gneiss and quartzite 74415
Eranondoo Hill

Durba Sandstone
Wingate, MTD and Bodorkos, S 2007, 181126: quartz sandstone, Durba Spring; Geochronology Record 681: Geological Survey of Western Australia, 5p.

Considered to represent a depositional age; Simple zoned euhedral crystals; 11 grains gave the above age; one zircon gave ca 1225Ma
Silver Hills Volcanics
EMERALD_SAMPLE 2
Anakie Region
Henderson, R.A., Davis, B.K., Fanning, C.M., 1998. Stratigraphy, age relationships and tectonic setting of rift-phase infill in the Drummond Basin, central Queensland. Australian Journal of Earth Sciences, 45(4), 579-595.

Data migrated from OZCHRON1. Original comment: This is a maximum depositional age for the sediment, although not precise. Other detrital ages are 1750 and 1774 Ma
Staveley Formation

K-Ar split analysis: K: AAS or AES and Ar: isotope-dilution mass spectrometry
Stratigraphic age: near top of Upper Devonian. Appears to be an excellent date.
Lake Mountain Rhyodacite
Lake Mountain Rhyodacite / Cerberean Volcanics
2 miles east of Rubicon Power Station, Snobs Creek, Warburton, Victoria, Australia
Evernden, J.F., Curtis, G.H., Obradovich, J.D., Kistler, R., 1961. On the evaluation of glauconite and illite for dating sedimentary rocks by the Potassium-Argon method. Geochimica et Cosmochimica Acta, 23, 78-99.

Mosquito Creek Formation
Nelson, DR 2004, 169200: coarse lithic quartz sandstone, Branchies Well; Geochronology Record 94: Geological Survey of Western Australia, 6p.

Sundown Group
This sample of Sundown Group was collected from Dense Camp Creek, approximately 17 km north of the township of Silverton. The sample is a sillimanite-rich psammitic horizon with a pervasive S2 foliation that appears to record earlier deformation fabrics than the overlying Paragon Group east of the sample location. The lithology shows evidence of extensive partial melting, with peritectic garnet-bearing leucosomes developed, and some muscovite-rich retrogression associated with a nearby shear zone (200 m away). The sample preserves evidence for at least three deformations: 1) bedding parallel S1 defined by biotite and sillimanite, 2) isoclinal folding and development of a composite S1/S2 defined by sillimanite and biotite, and 3) upright to inclined folding (F3) and spaced cleavage development.
Kositcin, N., Fitzherbert, J.A., Main, P.T., Waltenberg, K., 2018. New SHRIMP U-Pb zircon provenance and in situ monazite metamorphic ages from the Mount Robe Sub-block, Broken Hill, New South Wales: July 2015-June 2017. Geoscience Australia. Record, 2018/50, 63p.

alt. max dep age: 923+/- 12 Ma. MSWD=0.73. N= 4 youngest
Group S comprises 51 analyses (Table 1), which yield 207-corrected 238U/206Pb* and 207Pb*/206Pb* dates of 2767-933 Ma. A more conservative estimate of the maximum depositional age can be based on the weighted mean 207-corrected date of 923 +/- 12 Ma (MSWD = 0.73) for the four youngest analyses in Group S.
Wingate, MTD, Kirkland, CL and Haines, PW 2014, 199420: sandstone, Mu Hills; Geochronology Record 1193: Geological Survey of Western Australia, 5p.

Macquarie University
The youngest concordant grain (of 59 analyses) is Early Ordovician (478 +/- 5 Ma) with a corresponding peak at 475 Ma and is thus of no assistance in establishing a stratigraphic age.
Mundoonen Sandstone
Glen et al 2016 paraprashed: "This sample is extracted from the Mundoonen Sandstone. The Mundoonen Sandstone lies 52 km north of Canberra, lacks fossils, but lies above a latest Ordovician black shale and is faulted below Late Silurian volcanics (Sherwin, 2012). It consists of thick- and thin-bedded, coarse- to fine-grained sublithic to quartz-rich turbidites. Scattered grit-size quartz grains with angular crystal faces are probably volcanic. Scattered clasts of chert, phyllite and mudstone (Sherwin, 2012) were probably recycled from Early-Middle Ordovician turbidites. "
Glen, R. A., Belousova, E. &, Griffin, W. L. (2016). Different styles of modern and ancient non-collisional orogens and implications for crustal growth: a Gondwanaland perspective., Canadian Journal of Earth Sciences 53(11), 1372-1415.

There are no recorded Early Carboniferous ages in the region that would possibly correlate with this younger modelled age group. Assuming a Gaussian distribution for this estimated max dep age means a 28.1% probability that the 'true' model age is older than the 354 Ma boundary (10.6% for a 362 Ma boundary).
Rosemeath Formation
Sircombe & McQueen 2000 paraphrased: This sample was taken from coarse sandstones from near the top of the Rosemeath Formation showing prominent cross-bedding.
Endeavour
Sircombe, K. N .& McQueen, K .G. (2000). Zircon dating of Devonian-Carboniferous rocks from the Bombala area, New South Wales. Australian Journal of Earth Sciences 47, pp.1041-1051.

Burrell Creek Formation
Matrix-supported cobble conglomerate Sample of the former Noltenius Formation.
Chilling Creek

metasandstone (mt)
Kirkland, CL, Bodorkos, S, Wingate, MTD and Smithies, RH 2009, 185592: banded quartz-rich psammite, Latitude Hill; Geochronology Record 763: Geological Survey of Western Australia, 5p.

At the Rover 12 prospect, multiple layers of quartz-feldspar-chlorite rock occur within a sequence of metasedimentary quartz-chlorite schist and chert. In drill core the quartzofeldspathic rock is interlayered on the centimetre-scale with metasedimentary schist, occasionally showing irregular contacts with the schist and containing angular clasts of metasedimentary rock to ca. 9 cm in length. Both the schist and quartzofeldspathic rock contain a strong foliation that is sub-parallel to layering in the sampled drill core. In thin section the quartzofeldspathic rock shows numerous irregular 1-2 mm grains of quartz and feldspar set in a foliated chlorite-quartz matrix. The irregular grain shapes and the fine-scale interlayering with metasedimentary schist suggest that the quartzofeldspathic layers are immature, weakly metamorphosed volcaniclastic rocks. If the rock is indeed volcaniclastic in origin, the large angular metasedimentary fragments might represent rip-up clasts rather than magmatic xenoliths.
Rover 12
Maidment, D.W., Huston, D.L., Donnellan, N., Lambeck, A., 2013. Constraints on the timing of the Tennant Event and associated Au-Cu-Bi mineralisation in the Tennant Region, Northern Territory. Precambrian Research, 237, 51-63.

Kilbrechin Conglomerate Member
Sircombe & McQueen 2000 paraphrased: This sample is from the Kilbrechin Conglomerate Member, West of Bibbenluke, is a dipping conglomeratic unit near the base of the Rosemeath Formation. The base of the sequence is well defined by a pebble-cobble conglomerate, overlain by coarse grit and sandstone with less prominent, red and drab-coloured shale and siltstone units. The sequence here is at least 250m thick.
Kilbrechin
Sircombe, K. N .& McQueen, K .G. (2000). Zircon dating of Devonian-Carboniferous rocks from the Bombala area, New South Wales. Australian Journal of Earth Sciences 47, pp.1041-1051.

conservative alternative max depositional age 207Pb/206Pb: 1983 +/- 9 Ma. MSWD = 1.6. N = 12 youngest
Marboo Formation
LENNARD RIVER_206102.1
King Leopold Region
Kirkland, CL, Wingate, MTD, Tyler, IM, Hollis, J and Bodorkos, S 2013, 206102: sandstone, Richenda River; Geochronology Record 1135: Geological Survey of Western Australia, 5p.

Townsend Quartzite
Wingate, MTD, Lu, Y, Kirkland, CL, Haines, PW and Werner, M 2017, 195237: lithic sandstone, Townsend Ridges; Geochronology Record 1372: Geological Survey of Western Australia, 5p.

Bumbarlow 1

Papulankutja Supersuite
Kirkland, CL, Wingate, MTD, Smithies, RH and Evins, PM 2012, 194768: migmatitic paragneiss, Mount Scott; Geochronology Record 1028: Geological Survey of Western Australia, 5p.

Lu, Y, Wingate, MTD, Kirkland, CL, Maidment, DW, Phillips, C and Hollis, JA 2016, 206172: quartz-feldspar arenite, Chamberlain River; Geochronology Record 1345: Geological Survey of Western Australia, 6p.

MacDougall Formation
Lu, Y, Wingate, MTD, Quentin de Gromard, R, Howard, HM and Smithies, RH 2017, 208501: psammitic gneiss, Yulun-Kudara Waterhole; Geochronology Record 1410: Geological Survey of Western Australia, 6p.

This sample is from diamond drillcore obtained from Thomson Resources Ltd. drillhole F03D02 (downhole depth 481.4-482 m), drilled in 2011. This drillhole is located ~30 km west of the Cuttaburra mineral prospect, and between the Cuttaburra and F1 prospects.This drillhole contains predominantly pelitic and psammitic rocks with abundant quartz veins, and was sampled for geochronology as representative of the regional metasedimentary basement rocks which are intruded by mineralised granites at the Cuttaburra prospect. The sampled sandstone is comprised of rounded to sub-angular quartz grains within a fine-grained matrix of quartz, feldspar and sericite. The age of the youngest detrital zircons from this sample will provide a maximum age constraint on the timing of deposition of this sedimentary rock. The detrital zircon age spectrum will also be of interest for comparison with age spectra from other regional metasedimentary rocks of the southern Thomson and northern Lachlan Orogens.
Armistead, S.E., Fraser, G.L., 2015. New SHRIMP U-Pb zircon ages from the Cuttaburra and F1 prospects, southern Thomson Orogen, New South Wales. Geoscience Australia. Record, 2015/20, 39p.

Leucogranite; predominantly leucosome from migmatite.

Cooma Metamorphic Complex
Williams 2001 paraphrased: "Samples of the Cooma Complex were collected along an approximately east-west transect extending westwards. Biotite zone metasediment sample 95-32 was taken from a road cut where slaty metapelites with metapsammitic interbeds up to ~0.5 m wide outcrop in isoclinal folds with near-vertical axial planes. The sampled unit was a 0.1 m layer of semipelite, selected because comparison of zircon provenance between low-grade metasediment and the granodiorite required a sample of a ‘fertile’ lithology that might possibly yield a low-temperature partial melt. The rock is predominantly recrystallised granular quartz, with fine flakes of biotite defining the schistosity. Zircon from the biotite schist has a wide range of grainsize (30-250 um), colour (colourless to pale-pink to purple to brown), clarity, and shape (sharply euhedral whole grains to angular fragments to strongly rounded remnants). Such variation is to be expected in a physically and chemically resistant detrital mineral derived from a range of sources of different ages. Strongly rounded grains dominate the population, their frosted surfaces, characteristic of brittle grains worn by abrasion during sediment transport and reworking, visible under an optical microscope. Even the ‘euhedral’ grains are damaged, most obviously at the corners of the crystals and along the edges where faces meet. Such damage is most evident in secondary electron images, and is visible in cathodoluminescence images as microindentations around the edge of most rounded grains. Except for the near-euhedral grains, internal zoning is truncated at the broken or worn grain margins."
Williams, I. S. (2001). Response of detrital zircon and monazite, and their U-Pb isotopic systems, to regional metamorphism and host-rock partial melting, Cooma complex, southeastern Australia. Australian Journal of Earth Sciences 48, pp.557-580.

Omar 1

Lu, Y, Wingate, MTD, Kirkland, CL, Maidment, DW, Phillips, C and Hollis, JA 2016, 206106: pelitic migmatite, Sydney Harbour Yard; Geochronology Record 1340: Geological Survey of Western Australia, 6p.

Murphy Metamorphics
The Murphy Metamorphics is a poorly exposed low-grade metasedimentary unit forming part of a Paleoproterozoic basement complex, the Murphy Province, which is largely exposed within CALVERT HILLS (e.g. Ahmad and Wygralak, 1989). The unit consists of greenschist-facies shales, schists, meta-siltstones, meta-arenites, meta-greywackes, meta-volcanics and rare banded ironstone that is considered to have once represented a succession of turbidites prior to metamorphism (e.g. Ahmad and Wygralak, 1989). Sample 2786176 was collected in a small region of good exposure of Murphy Metamorphics, around 250 m north of the faulted southern margin of the Murphy Province (the extension of the east-west trending Fish River Fault system), where the basement is faulted against the Paleoproterozoic Tawallah and Fickling Groups. The sample is a well-foliated two mica, quartz schist with discontinuous lenses of recrystallised ‘sugary’ textured pegmatite and sandstone. The well-developed foliation observed at this locality, dips very steeply to the north and to the south (between 75-90º), striking approximately east-west and is sub-parallel to the bounding fault system.

coarse-grained metasandstone

104 analyses exhibit several prominent peaks at ~1752Ma with subordinate peaks at ~1864 & 2525 Ma. Determining a youngest population is difficult. A weighted mean of the youngest three grains gives 1600 ? 21 Ma, (MSWD 0.65
Burangoo Sandstone
LAWN HILL_ISSNG_053

Hussar Formation
NELSON, D. R., 2004, 154666: arenite, Empress 1A; Geochronology dataset 52; in Compilation of geochronology data, June 2006 update: Western Australia Geological Survey.

This sample is a feldspathic sandstone from Polygonum DD IN6 570.6 - 572.5 m

Hermit Creek Metamorphics
schist

University of Queensland
Combined detrital zircon ages of sedimentary samples MG-14-11, MG-14-12, MG-14-15, MG-14-18: 288.5 +- 2.1 Ma (MSWD = 0.21, n = 33)
Giro beds
White et al 2016 paraphrased: "The Giro Damictite is a massive pebbly mudstone/fine-grained siltstone (or diamictite) with uncommon massive, bedded or turbidite sandstones, siltstones, and pebble conglomerates. Sheared serpentinite clastswere observed within. Zircons with
White L., Rosenbaum G., Allen C. & Shaanan U. (2016) Supporting information for orocline-driven transtensional basins: insights from the Lower Permian Manning Basin (eastern Australia)., Tectonics 35, 690-703.

Nombiginni Volcanics
Rhyolite adjacent to quarry (I-type).
Downes P., Blevin P., Armstrong R., Simpson C., Sherwin L., Tilley D. & Burton G. (2016) Outcomes of the Nymagee mineral system study - an improved understanding of the timing of events and prospectivity of the central Lachlan Orogen., Quarterly Notes of the Geological Survey of New South Wales 147.

Metasandstone

Wanna Formation
Wingate, MTD, Kirkland, CL, Haines PW and Hocking, RM 2013, 199423: sandstone, Empress 1; Geochronology Record 1112: Geological Survey of Western Australia, 6p.

Regionally, the lowermost part of the Corella Formation (PLkc1) in the Mary Kathleen Domain is described as laminated calcareous metasiltstone and fine-grained feldspathic sandstone, limestone and siltstone, passing into calcareous scapolitic granofels and calc-silicate (hornblende-diopside) granofels. The sample was collected from an outcrop of thin- to medium-bedded, fine-grained laminated metasandstone interbedded with fine-grained scapolitic calc-silicate rocks that occur along a low ridge in the westernmost part of the Corella Formation type section about 150 m above the base and the contact with the underlying Ballara Quartzite. The site is about 50 m north of the former Cloncurry–Mount Isa road (now used as a station track on Corella Park Station) and is about 17.5 km north of the former Mary Kathleen uranium mine. In thin section, the sample consists of ~25% bluish green, subelongate and partly aligned grains of hornblende up to 0.5 mm in a granular mosaic of quartz and untwinned feldspar in subequal proportions and generally 0.05–0.1 mm. Opaque grains (~5%) and accessory titanite are also present. Bands of alteration up to 5 mm wide contain turbid feldspar and minor epidote. The sample was collected to provide a MDA and Zr spectra to be used as a control for regional comparison.
Kositcin, N., Lewis, C.J., Withnall, I.W., Slade, A.P., Sargent, S., Hutton, L.J., 2023. Summary of results. Joint GSQ-GA Geochronology Project: Mount Isa region, 2017-2018. Geoscience Australia. Record, 2023/32, 97p.

Halls Reward Metamorphics
The Halls Reward Metamorphics are considered part of the Thomson Orogen and are the easternmost unit in the Greenvale Province. They comprise amphibolite facies mica schist, quartzite, biotite-muscovite gneiss and mafic and ultramafic units (Fergusson et al., 2013). This sample of Halls Reward Metamorphics is a quartzose meta-arenite with thin micaceous horizons collected from a cutting along the old Greenvale railway line ~4.8 km north-northwest of Greenvale.
Kositcin, N., Lisitsin, V., Bultitude, R.J., Purdy, D.J., Brown, D.D., von Gnielinski, F.E., Dhnaram, C., 2016. Summary of results - Joint GSQ-GA geochronology project: Thomson Orogen, Mossman Orogen and Cape York, 2015-2016. Queensland Geological Record, 2016/09, 102p.

Tempe Formation
The Tempe Formation of the Pertaoorrta Group (Ranford et al 1965) is confined to the central-west of the Amadeus Basin (Carmichael sub-basin). It is poorly exposed (Wells et al 1970, Bradshaw 1991) in strike valleys in the Gardiner Range, Walter Creek, Petermann Creek, and Parana Hill anticlines (HENBURY). The formation averages ~150 m in thickness and is a predominantly recessive unit dominated by shale and siltstone, with lesser dolostone, sandy dolostone, calcareous sandstone, and locally glauconitic sandstone or dolostone. Bradshaw (1991) interpreted the formation as a nearshore to shallow water shelf succession containing offshore, shoreface, tidal flat, and bay and lagoon sediments. The upper part of the formation contains brachiopods, trilobites and gastropods, which indicate an early Middle Cambrian age (Wells et al 1970, Shergold 1986). A previous detrital zircon sample of sandstone from the Tempe Formation produced a maximum depositional age of 518 +/- 8 Ma (Kositcin et al 2018). This sample (LA19CSV027) of the Tempe Formation is a red, well-sorted, fine-to medium-grained sandstone collected from a small ridge ~25 km south-southeast of Kings Canyon.
Kositcin, N., Verdel, C., Normington, V.J., Simmons, J.M., 2021. Summary of results. Joint NTGS-GA geochronology project: western Amadeus Basin, July-August 2020. Northern Territory Geological Survey Record, 2021-002, 25p.

Macquarie University
Age is the youngest significant peak. Concordia age 456.0 +- 6.3. Two clusters were identified in the youngest sub-populations (~ 455 and ~ 475 Ma). The most significant age peak identified is ~ 455 Ma.
Combaning Formation
Tilhac 2019 paraphrased "The sample is a meta-conglomerate with mostly stubby zircon grains and fragments, suhedral to anhedral and commonly rounded, equant to weakly elongated, some with inclusions. Wich are mostly orange, ranging from 80 um to 350 um. They have mix of different features. Oscillatory zoned and diffuse features, some sector zoned, laminated, and more complex features.
Tilhac, R. (2019). Zircon U-Pb dating: TerraneChron report to the Geological Survey o fNew South Wales (TC-182). CCFS and GEMOC Macquarie University. Geological Survey of New South Wales, Maitland. File GS2019/0446.

Yilgatherra Formation
Nelson, DR 2004, 169093: sandstone, Cundarra Bore; Geochronology Record 87: Geological Survey of Western Australia, 5p.

Telfer Member
Telfer West Dome
Nelson, DR 2000, 137655: metasandstone, Telfer West Dome; Geochronology Record 418: Geological Survey of Western Australia, 5p.

Euro Basalt
MARBLE BAR_168999.1
Nelson, DR 2004, 168999: quartzite, Pethernurrina Spring; Geochronology Record 59: Geological Survey of Western Australia, 5p.

Lalla Rookh Sandstone
Lalla Rookh Well
Nelson, DR 2000, 142951: sandstone, Lalla Rookh Well; Geochronology Record 301: Geological Survey of Western Australia, 5p.

Gorge Creek Group
volcaniclastic sediment
Nelson, DR 1998, 127330: volcaniclastic sedimentary rock, Cleaverville; Geochronology Record 442: Geological Survey of Western Australia, 4p.

Gardiner Sandstone
GORDON DOWNS_213019.1
Lu, Y, Wingate, MTD, Morin-Ka, S and Beardsmore, TJ 2017, 213019: quartz arenite, Kundat Djaru; Geochronology Record 1398: Geological Survey of Western Australia, 6p.

Nelson, DR 2004, 169013: metasandstone, Punduna Pool; Geochronology Record 138: Geological Survey of Western Australia, 5p.

laser ablation: New Wave ESI 193 nm laser
Chinese Academy of Geological Sciences
Fairbridge Volcanics
Zhang et al 2019 paraphrased "The Fairbridge Volcanics are dominated by volcanic breccia, conglomerate and volcanic rocks, which are intercalated with finer volcaniclastic sandstones, volcanic sandstones and minor cherty siltstones. The lowest-preserved stratigraphic levels are dominated by poorly-sorted volcanic derived conglomerate. Most clasts are basaltic to andesitic, ranging in size 0.2-8 cm. Samples of this unit display dislocations in feldspars, undulose extinction in rare quartz and extensive sericitic alteration. In sample 16FV01-1,most of the extracted zircons are round, clear and small to medium in size (70-30 um by 100-50 um), and a few of them are yellow in colour with larger sizes. In CL images, well preserved entire zircons show concentric oscillatory zoning and a few of them show recrystallisation patches. The larger zircons are grain fragments. Four small grains show intense oscillatory zoning, some larger sizes of fragments show wider bands, and the remaining have no zoning features."
Zhang, Q., Buckman, S., Bennett, V. & Nutman, A. (2019). Inception and early evolution of the Ordovician Macquarie Arc of Eastern Gondwana margin: zircon U-Pb-Hf evidence from the Molong Volcanic Belt, Lachlan Orogen. Lithos 326-327, pp.513-528.

Fairbridge Volcanics
Zhang et al 2019 paraphrased "The Fairbridge Volcanics are dominated by volcanic breccia, conglomerate and volcanic rocks, which are intercalated with finer volcaniclastic sandstones, volcanic sandstones and minor cherty siltstones. The lowest-preserved stratigraphic levels are dominated by poorly-sorted volcanic derived conglomerate. Most clasts are basaltic to andesitic, ranging in size 0.2-8 cm. Samples of this unit display dislocations in feldspars, undulose extinction in rare quartz and extensive sericitic alteration. In 16FV01Sa, 12 zircons were analysed, and most are small (50-70 um) and clean, with a few big dark rounded grains of 100 um."
Zhang, Q., Buckman, S., Bennett, V. & Nutman, A. (2019). Inception and early evolution of the Ordovician Macquarie Arc of Eastern Gondwana margin: zircon U-Pb-Hf evidence from the Molong Volcanic Belt, Lachlan Orogen. Lithos 326-327, pp.513-528.

10 grains form a non-Gaussian distribu-tion in which two age components of 440.1 +/- 5.3 Ma and 469.4 +/-4.7 Ma (2sigma) were resolved by mixture modelling in Isoplot
Fairbridge Volcanics
Zhang et al 2019 paraphrased "The Fairbridge Volcanics are dominated by volcanic breccia, conglomerate and volcanic rocks, which are intercalated with finer volcaniclastic sandstones, volcanic sandstones and minor cherty siltstones. The lowest-preserved stratigraphic levels are dominated by poorly-sorted volcanic derived conglomerate. Most clasts are basaltic to andesitic, ranging in size 0.2-8 cm. Samples of this unit display dislocations in feldspars, undulose extinction in rare quartz and extensive sericitic alteration. In sample 16FV01,most of the extracted zircons are round, clear and small to medium in size (70-30 um by 100-50 um), and a few of them are yellow in colour with larger sizes. In CL images, well preserved entire zircons show concentric oscillatory zoning and a few of them show recrystallisation patches. The larger zircons are grain fragments. Four small grains show intense oscillatory zoning, some larger sizes of fragments show wider bands, and the remaining have no zoning features."
Zhang, Q., Buckman, S., Bennett, V. & Nutman, A. (2019). Inception and early evolution of the Ordovician Macquarie Arc of Eastern Gondwana margin: zircon U-Pb-Hf evidence from the Molong Volcanic Belt, Lachlan Orogen. Lithos 326-327, pp.513-528.

The metasandstone sample was taken from the downhole interval 51–52.6 m in drillhole 17GRDD001 at the Grapple Prospect; it was selected for geochronology to determine the maximum depositional age of the metasedimentary succession hosting mineralisation at the Grapple prospect. The metasandstone is weakly foliated and is subarkose, containing medium- to coarse-grained, poorly-sorted, sub-angular to sub-rounded quartz and feldspar. The dominant mineral is quartz, with grain size ranging from 20 μm to 1 mm. Feldspar (K-feldspar and plagioclase) comprises 10–20% of the rock and ranges up to 1 mm in size. Micas (biotite and muscovite) constitute ~5 vol% of the rock; trace to minor opaque oxide minerals and zircon are also identified.
Kositcin, N., McGloin, M.V., Reno, B.L., Beyer, E.E., 2019. Summary of results. Joint NTGS-GA geochronology project: Cu-Au-Ag-Zn mineralisation in MOUNT RENNIE, Aileron and Warumpi provinces, March-September 2018. Northern Territory Geological Survey Record, 2019-011, 24p.

Euro Basalt
Nelson, DR 2005, 178042: altered volcaniclastic sandstone, Table Top Well; Geochronology Record 564: Geological Survey of Western Australia, 4p.

The Liddle Formation is part of the Winnall Group (formerly Winnall beds of Ranford et al 1965, redefined by Donnellan and Normington 2017). The formation is exposed in generally northwest-striking ridges in the central and western parts of the Amadeus Basin. At its type-section in HENBURY, the Liddle Formation is overlain by the Puna Kura Kura Formation, the uppermost part of the Winnall Group. The Liddle Formation is probably late Ediacaran based on its stratigraphic position (Donnellan and Normington 2017). A previous sample of the Liddle Formation from BLOODS RANGE produced a detrital zircon maximum depositional age of 696 +/- 13 Ma (Beyer et al 2020). Sample BR19CSV097 is a well sorted, medium-grained sandstone collected from Mt. Unapproachable, a small ridge within Lake Neale.

metarhyolite (mfr)
Wingate, MTD, Bodorkos, S and Van Kranendonk, MJ 2009, 180039: felsic volcaniclastic rock, Wodgina; Geochronology Record 806: Geological Survey of Western Australia, 4p.

MacDougall Formation
Kirkland, CL, Wingate, MTD, Quentin De Gromard, R, Howard, HM and Smithies, RH 2014, 205194: psammitic gneiss, Mitika Homestead; Geochronology Record 1203: Geological Survey of Western Australia, 5p.

DIXON RANGE_206126.1
Wingate, MTD, Kirkland, CL, Hollis, J and Phillips, C 2015, 206126: metasandstone, Dry Creek mine; Geochronology Record 1241: Geological Survey of Western Australia, 6p.

Wingate, MTD and Haines, PW 2009, 135965: phyllitic metasandstone, Acacia 2; Geochronology Record 780: Geological Survey of Western Australia, 5p.

gneiss
Bodorkos, S, Wingate, MTD and Kirkland, CL 2008, 174748: migmatitic metasandstone, Mount Fanny; Geochronology Record 720: Geological Survey of Western Australia, 7p.

67 analyses of 67 zircons, which yield 207Pb*/206Pb* and 238U/206Pb* dates of 2978-503 Ma.
Anderson Formation
Wingate, MTD and Haines, PW 2009, 135966: sandstone, Yulleroo 1; Geochronology Record 781: Geological Survey of Western Australia, 5p

age of the volcanic component in the Mitchell Formation
Mitchell Formation
Zhang et al 2019 paraphrased "The sample is from volcanic-derived conglomerate in the Mitchell Formation with clasts that are predominantly sub-angular to sub-rounded basalt and andesite (60-70%), feldspar fragments (10-15%), minor sandstone and chert fragments, with abundant calcite and sericite alteration. The Mitchell Formation is characterised by low yields of zircons from the volcaniclastic rock samples which reflects the predominantly basaltic nature of the source rocks. Their lack of significant rounding or weathering indicates proximal sources in a submarine environment (Morgan and Scott in Meakin et al., 1999)."

The sample was collected towards the easternmost and upper part of the Corella Formation type section within subdivision PLkc3a . Regionally, the subunit is described as calc-silicate granofels and impure marble with common metasiltstone interbeds (Withnall et al., 2015). The sampled outcrop consists of thin to medium interbeds of fine-grained calc-silicate-bearing, laminated meta-sandstone or metasiltstone showing lenticular spots of scapolite. In thin section, the sample consists mostly of a granular mosaic of subequant grains of quartz and untwinned feldspar <0.1 mm with aligned reddish brown biotite. Some layers have up to 30% subhedral poikiloblastic grains of weakly birefringent garnet (grossular or andradite) up to 0.2 mm. Aggregates of highly birefringent scapolite up to 5 mm are intergrown with poikiloblastic diopside and contain inclusions of garnet. The site is about 130 m north of the former Cloncurry–Mount Isa road (now used as a station track on Corella Park Station) and is about 22.5 km north-northeast of the former Mary Kathleen uranium mine. The sample was collected to provide a maximum depositional age and Zr spectra to be used as a control for regional comparison and correlation.
Kositcin, N., Lewis, C.J., Withnall, I.W., Slade, A.P., Sargent, S., Hutton, L.J., 2023. Summary of results. Joint GSQ-GA Geochronology Project: Mount Isa region, 2017-2018. Geoscience Australia. Record, 2023/32, 97p.

Considered to represent a depositional age; 14 analyses produced one discordant result attributed to Pb loss; grains have rounded terminations, but show magmatic zoning and internal cavities consistent with entrapment of vapour phases during rapid cooling
Silver Hills Volcanics
CLERMONT_SAMPLE 7
Drummond Region
Henderson, R.A., Davis, B.K., Fanning, C.M., 1998. Stratigraphy, age relationships and tectonic setting of rift-phase infill in the Drummond Basin, central Queensland. Australian Journal of Earth Sciences, 45(4), 579-595.

A more conservative estimate of the maximum depositional age can be based on the weighted mean 207Pb*/206Pb* date of 553 +/- 26 Ma (MSWD = 2.60) for the three youngest analyses
Goldwyer Formation
Wingate, MTD and Haines, PW 2009, 135963: sandstone, Wilson Cliffs 1; Geochronology Record 778: Geological Survey of Western Australia, 5p.

laser ablation: GeoLas 193nm ArF laser ablation system
James Cook University
Youngest detrital zircon population from a combination of four samples (053_SH_AK, 073_SH_NW, 031_SH_HA, 007_SH_BU) from Early Permian Nambucca block.
Shaanan et al 2015 paraphrased "The sample was extracted from a slate at North Armidale Road. Zircon crystals range from elongate euhedral to abraded and well-rounded morphologies. Their maximum length is 325 um, and the mean apparent elongated axis is 108 um. Under cathodoluminescence, most crystals exhibit well-defined oscillatory zoning, and some contain convolute zoning or absence of zoning
Shaanan, U., Rosenbaum, G. & Wormald, R. (2015). Provenance of the Early Permian Nambucca block (eastern Australia) and implication for the role of trench retreat in accretionary orogens. Geological Society of America Bulletin 127, pp.1052-1063.

Age populations of 600-505 Ma, 700-600 Ma and 1250-950 Ma are distinguishable from 95 concordant analyses (from a total of 100). This is the youngest population mean age.
Noonthorangee Formation
Johnson et al 2016 paraphrased: "The sample was collected fromthe Noonthorangee Formation of the Ponto Group, which is located in the hangingwall of the Koonenberry Fault. Quartz is the dominant mineral in this sample, with minor abundances of detrital muscovite, plagioclase and alkali feldspar. Quartz grains are characterised by the development of subgrain boundaries, which reflects the higher-grade of metamorphism and strain attained by these rocks. Oscillatory zoning is dominant in the majority of the detrital zircon grains extracted from this sample."
Johnson, E. L., Phillips, G. & Allen, C. M. (2016). Ediacaran-Cambrian basin evolution in the Koonenberry Belt (eastern Australia): implications for the geodynamics of the Delamerian Orogen. Gondwana Research 37, pp.266-284.

Hannover South 1
Lech, M.E., Lewis, C.J., White, L.T., Abbott, S.T., 2018. Triassic provenance analysis of the Roebuck Basin, North West Shelf of Australia. ASEG/SEG Conference Papers, 2018(1), 6p.

Telfer Member
Nelson, DR 2001, 137657: metasandstone, Telfer West Dome; Geochronology Record 419: Geological Survey of Western Australia, 4p.

Sixty-six analyses were undertaken on 66 zircon grains, and the analyses are characterised by a wide range of U contents (56-629 ppm), Th contents (50-574 ppm) and Th/U (0.15-1.88). The analyses record 207Pb/206Pb ages between ~2630 Ma and ~1285 Ma, with dominant age clusters at ~1800 Ma, at ~1750 Ma and at ~1670 Ma, as well as 29 analyses with ages between ~1438 Ma and the youngest individual age (from 080.14.1.1) at ~1285 Ma. The MSWD value of 5.9 for the weighted mean 207Pb/206Pb age of the post-1440 Ma cluster (n = 29) indicates that it is not a single population. Mixture modelling of this cluster assuming the presence of three resolvable age components yields a youngest modelled age of 1313 +/- 11 Ma (2sigma; fraction = 0.30). Alternatively, using the MSWD as a guide for the youngest statistically coherent group provides a weighted mean age of 1313 +/- 13 Ma (95% confidence) for the youngest 9 analyses in this cluster (MSWD = 1.8; probability of fit = 0.069). Given that these two age calculations are within error of each other, the weighted mean age is used to define the maximum depositional age for this sample.The weighted mean 207Pb/206Pb age of 1313 +/- 13 Ma (95% confidence) obtained from the youngest 9 analyses is used to define the maximum age for deposition of the sandstone.
fine grained silty sandstone
GSWA Empress 1A
Korsch, R.J., Blewett, R.S., Pawley, M.J., Carr, L.K., Hocking, R.M., Neumann, N.L., Smithies, R.H., Quentin de Gromard, R., Howard, H.M., Kennett, B.L.N., Aitken, A.R.A., Holzschuh, J., Duan, J., Goodwin, J., Jones, T., Gessner, K., Gorczyk, W., 2013. Geological setting and interpretation of the southwest half of deep seismic reflection line 11GA-YO1: Yamarna Terrane of the Yilgarn Craton and the western Officer Basin. In: Neumann, N.L. (ed.) Yilgarn Craton-Officer Basin-Musgrave Province Seismic and MT Workshop. Geoscience Australia. Record, 2013/28, 24-50.

Partially consolidated medium-grained sand to gravel. Pale grey to white. Within Madura Fm shales. Contains wood.
Jagodzinski, E.A., Bodorkos, S., Crowley, J.L., Pawley, M.J., Wise, T.W., 2019. PACE Copper Coompana Drilling Project: U-Pb dating of basement and cover rocks. Geological Survey of South Australia. Report Book, 2018/00028, 211p.

A small population of ages is located on the shoulder of the dominant 700-500 Ma population; mean age.
Morden Formation
Johnson et al 2016 paraphrased: "The sample is from the Morden Formation of the Kayrunnera Group, which represents the stratigraphically lowest exposed unit of the Kayrunnera Basin. Grains of subangular quartz and feldspar that are embedded in calcite cement comprise the majority of the sample; matrix material is largely absent. The angular nature of the framework grains indicates that the sediments were not extensively reworked, and are probably not far traveled. The dominance of quartz and the minor fractions of feldspar in samples KB22a, KB21 and KB23 from the Kayrunnera Group indicate that the contributing sediments were probably derived from a cratonic source. Grains of detrital zircon extracted from the sample are well rounded and have low aspect ratios. Oscillatory zoning and complex heterogeneous textures are pronounced in the majority of grains."
Johnson, E. L., Phillips, G. & Allen, C. M. (2016). Ediacaran-Cambrian basin evolution in the Koonenberry Belt (eastern Australia): implications for the geodynamics of the Delamerian Orogen. Gondwana Research 37, pp.266-284.

187 concordant results define a broad distribution of ages between 1550 Ma and 900 Ma. This is the youngest population's mean age.
Kara Formation
Johnson et al 2016 paraphrased: "Samples KB07 and KB08 are from the Kara Formation that consists of finely laminated siltstone and sandstone with minor chert and limestone (Mills, 1992). U-Pb dating of zircon taken from a horizon of alkali rhyolite that is conformable with bedding in the Kara Formation. The sample was collected from just below the contact with the overlying Nundora Formation of the Teltawongee Group. Bedding in formations is parallel, and the contact is considered to be structurally concordant. Texturally, the samples are angular to sub-rounded quartz that lies in a fine-grained matrix of quartz and white mica. The samples contain very little lithic material or feldspar and plot within the craton interior field of the tectonic discrimination plot. Grains of detrital zircon extracted from the samples are generally fragmented, variably rounded and have oscillatory zoning."
Johnson, E. L., Phillips, G. & Allen, C. M. (2016). Ediacaran-Cambrian basin evolution in the Koonenberry Belt (eastern Australia): implications for the geodynamics of the Delamerian Orogen. Gondwana Research 37, pp.266-284.

A more conservative estimate of the maximum depositional age can be based on the weighted mean 207Pb*/206Pb* date of 1097 +/- 22 Ma (MSWD = 2.0) for the 10 youngest analyses
Sir Frederick Conglomerate
Wingate, MTD, Kirkland, CL and Haines, PW 2014, 199418: sandstone, Mu Hills; Geochronology Record 1191: Geological Survey of Western Australia, 6p.

Considered to represent a depositional age; 9 analyses gave the above age; one discordant analysis gave ca 1690Ma; 2 others were also discordant and thought to have lost radiogenic Pb
Silver Hills Volcanics
CLERMONT_SAMPLE 5
Drummond Region
Henderson, R.A., Davis, B.K., Fanning, C.M., 1998. Stratigraphy, age relationships and tectonic setting of rift-phase infill in the Drummond Basin, central Queensland. Australian Journal of Earth Sciences, 45(4), 579-595.

Bodorkos, S., Cawood, P.A., Oliver, N.H.S., Nemchin, A.A., 2000. Rapidity of orogenesis in the Paleoproterozoic Halls Creek Orogen, northern Australia; evidence from SHRIMP zircon data, CL zircon images, and mixture modeling studies. American Journal of Science, 300(1), 60-82.

alt. conservative maximum age of deposition: 1872 +/- 5 Ma. MSWD = 1.47. N=25 youngest
A more conservative estimate of the maximum age of deposition is provided by the weighted mean 207Pb*/206Pb* date of 1872 +/- 5 Ma (MSWD = 1.47) for the 25 youngest analyses in Groups Y and S. However, the date of 1838 +/- 15 Ma (1 sigma) is consistent with the previous estimate of 1840-1830 Ma for deposition of the Lander Rock Formation (Scrimgeour, 2006).
Kirkland, CL, Wingate, MTD, Spaggiari, CV and Tyler, IM 2009, 184363: metasandstone, Mount Tietkens; Geochronology Record 821: Geological Survey of Western Australia, 5p.

Wirku Metamorphics
Kirkland, CL, Bodorkos, S, Wingate, MTD, Smithies, RH and Evins, PM 2009, 185508: felsic paragneiss, Mount Aloysius; Geochronology Record 767: Geological Survey of Western Australia, 5p.

McFadden Formation
Wingate, MTD and Bodorkos, S 2007, 181127: quartz sandstone, Durba Hills; Geochronology Record 682: Geological Survey of Western Australia, 7p.

Group S comprises 59 analyses (Table 1), which yield 207Pb*/206Pb* dates of 2958-1126 Ma. A more conservative estimate of the maximum depositional age can be based on the concordia age of 1163 +/- 13 Ma (MSWD = 2.4) for the youngest coherent group of six analyses in Group S.
Karukali Quartzite
Wingate, MTD, Lu, Y, Quentin de Gromard, R, Howard, HM and Haines, PW 2017, 208466: quartzite, Mount Deering; Geochronology Record 1437: Geological Survey of Western Australia, 7p.

Of the 98 detrital zircons analysed, 81 concordant results were obtained. This is the mean of the youngest population.
Bilpa Conglomerate
Johnson et al 2016 paraphrased: " The sample was collected from the Bilpa Conglomerate, which is the basal unit of the Mutawintji Group. The sample is dominated by metamorphic and mafic lithic fragments along with coarse, angular clasts of quartz and alkali feldspar. The lithic and clast contents of this sample are consistent with its derivation from an orogenic source. Detrital zircon extracted from the sample are rounded, fragmented, and often exhibits faint oscillatory zoning. The identification of heterogeneous and patchy textures combined with inherited cores with metamorphic rims indicates a complex history for some of the grains."

Ooloo Hill Formation
The drill core contains basaltic lavas with minor tuff intercalated with the siliciclastic-epiclastic sedimentary succession. Sample R1837679 is a sandstone-greywacke from a ~30 m interval of sandstone, arkose, greywacke and conglomerate (pebble clasts are mostly weathered basalt) that separates basaltic lavas at the base of the drillhole and the top of the unit.
Sheard, M.J., White, M.R., Stoian, L., Jagodzinski, E.A., 2012. Explanatory notes for Marree, South Australia 1:250 000 geological map, sheet SH54-5. Geological Survey of South Australia. Report Book, 2012/00004, 231p.; Wade, C.E., Reid, A.J., Jagodzinski, E.A., Sheard, M.J., 2023. Mid-Devonian basaltic magmatism and associated sedimentation: the Ooloo Hill Formation, central-eastern South Australia. Australian Journal of Earth Sciences, 70, 22p.

University of Queensland
Combined detrital zircon ages of sedimentary samples MG-14-11, MG-14-12, MG-14-15, MG-14-18: 288.5 +- 2.1 Ma (MSWD = 0.21, n = 33)
Giro beds
eastern basin clastic sample, Charity Creek beds (equiv)
White et al 2016 paraphrased: "Charity Creek Beds comprise massive pebbly mudstones and diamictites commonly interbedded with massive sandstone horizons harboring thin siltstone and mudstone laminations. This unit is possibly correlative to the Giro Diamictite of the western part of the [Manning] basin (Jenkins, 1992). Zircons with preference for the larger, more euhedral crystals to encourage a robust youngest population constraint."
White L., Rosenbaum G., Allen C. & Shaanan U. (2016) Supporting information for orocline-driven transtensional basins: insights from the Lower Permian Manning Basin (eastern Australia)., Tectonics 35, 690-703.

Anderson, J.R., Lewis, C.J., Jarrett, A.J.M., Carr, L.K., Henson, P.A., Carson, C.J., Southby, C., Munson, T.J., 2019. New SHRIMP U-Pb zircon ages from the South Nicholson Basin, Mount Isa Province and Georgina Basin, Northern Territory and Queensland: July 2017-June 2018. Geoscience Australia. Record, 2019/10, 101p.; Carson, C.J., Kositcin, N., Anderson, J.R., Henson, P.A., 2023, A revised Proterozoic tectono-stratigraphy of the South Nicholson region, Northern Territory, Australia - insights from SHRIMP U-Pb detrital zircon geochronology. Australian Journal of Earth Sciences, in press.

Lupton Formation
NELSON, D. R., 1999, 154109: quartz-carbonate diamictite, Empress 1A; Geochronology dataset 71; in Compilation of geochronology data, June 2006 update: Western Australia Geological Survey.

A more conservative estimate of the maximum depositional age can be based on the weighted mean 207-corrected 238U/206Pb* date of 1012 +/- 26 Ma (MSWD = 1.7) for the nine youngest analyses
Maurice Formation
Wingate, MTD, Kirkland, CL and Haines, PW 2014, 199414: sandstone, Sir Frederick Range; Geochronology Record 1190: Geological Survey of Western Australia, 6p.

Youngest zircon is c. 301 Ma. This contrasts with known deposition age of the sediment being early Permian.
Cardarie Sandstone Member
Grant Gp, Carolyn Formation Ngumban Claystone Member 1st resistant sandy bed with pebbles-boulders

The youngest population of ages defines a mean age.
Wonnaminta Formation
Johnson et al 2016 paraphrased: "Samples KB12 and KB14 are from the Wonnaminta Formation of the Teltawongee Group and were collected in close proximity to a faulted contact with the older Kara Formation. The samples dominantly consist of angular to subangular quartz with moderate proportions of detrital white mica, minor K-feldspar and plagioclase. The Wonnaminta Formation is characterised by repetitive sequences of immature sandstone (up to 3m thick in places) overlain by an upward fining sequence of fine sandstone, siltstone and mudstone (Mills, 1992). In places, the finer-grain lithologies are absent, which results in an amalgamation of coarse-grained sandstone horizons that give the appearance of an extremely thick (~10 m), monotonous package of immature sandstone (Mills, 1992). Grains of detrital zircon from samples KB12 and KB14 are invariably rounded, and contain internal grain morphologies that range from faint oscillatory zoning to homogeneous textures with sector zoning."

Concordant U-Pb ages (149 from 197 analyses) dominantly cluster around 750-500 Ma, with substantial populations in the ranges of 950-750 Ma and 1400-950 Ma.
Wonnaminta Formation
Johnson et al 2016 paraphrased: "Samples KB12 and KB14 are from the Wonnaminta Formation of the Teltawongee Group and were collected in close proximity to a faulted contact with the older Kara Formation. The samples dominantly consist of angular to subangular quartz with moderate proportions of detrital white mica, minor K-feldspar and plagioclase. The Wonnaminta Formation is characterised by repetitive sequences of immature sandstone (up to 3m thick in places) overlain by an upward fining sequence of fine sandstone, siltstone and mudstone (Mills, 1992). In places, the finer-grain lithologies are absent, which results in an amalgamation of coarse-grained sandstone horizons that give the appearance of an extremely thick (~10 m), monotonous package of immature sandstone (Mills, 1992). Grains of detrital zircon from samples KB12 and KB14 are invariably rounded, and contain internal grain morphologies that range from faint oscillatory zoning to homogeneous textures with sector zoning."

New Hope Sandstone Member
The sample is a coarse-grained felspathic sandstone collected from southeast of the Mount Cobalt mine in the upper part of a succession mapped as New Hope Sandstone Member. The member consists of prominent beds of brown to cream or pink, massive to locally graded, medium to very thick-bedded, coarse-grained feldspathic sandstone with subordinate interbeds of more micaceous metasandstone and pelitic mica schist. The succession at the sample site is overturned, and youngs to the west. It is overlain by the upper part of the Starcross Formation, which is the parent unit of the New Hope Sandstone Member. In thin section, the sample consists of a mosaic of quartz and subordinate feldspar and minor muscovite. The grainsize distribution shows bimodality with coarser grains 0.5–2 mm in a finer matrix 0.5–0.2 mm, but the low abundance of muscovite indicates that there was little clay in the protolith. Four samples of the New Hope Sandstone Member have been dated previously. One located east of the Kuridala smelter site (Geochron Delivery, sample 1925991/2005169048) gave a maximum depositional age of 1676 ± 4 Ma (Withnall, 2019). Another from the Tip Top mine area (Geochron Delivery, sample 1925942/2006169014) yielded an interpreted maximum deposition age of 1674 ± 9 Ma (Withnall, 2019). A quartzo-feldspathic sandstone sample from northeast of Mount Cobalt (sample 1925943/2006169015) yielded a maximum depositional age of 1693 ± 9 Ma (recalculated to 1691 ± 9 Ma, Withnall, 2019). Lewis et al. (2020) determined a maximum depositional age of 1662 ± 22 Ma for the New Hope Sandstone Member (2614024/SSMI-139) south of Mount Dore. This sample from near the top of the member was collected to further constrain the age of the unit and that of the Starcross Formation and lower part of the Kuridala Group.

The date of 3464 +/- 3 Ma indicated by the weighted mean 207Pb/206Pb ratio of the 14 concordant analyses of Group 1 may be interpreted as the age of igneous crystallization of the felsic volcanic precursor to the schist
quartz-sericite schist
Nelson, DR 2002, 169008: quartz-sericite schist, Coongan Belt Well; Geochronology Record 171: Geological Survey of Western Australia, 4p.

Zircon Description The sample is from BMR drillcore Hay River 2 which penetrated basement below the Erromanga basin. There is no nearby exposure of basement for context but aeromagnetics suggest continuity with the Arunta region. Zircons in the sample have rounded, pitted and broken external forms truncating internal zoning, consistent with a mature detrital zircon suite (Fig. 1). Internal zoning patterns are highly variable. A random split of grains not sorted for quality contained a high proportion of excessively cracked and physically soft grains (topographic lows in polishing) indicating risk of a high proportion of isotopic discordance. Accordingly analysis was restricted to non-magnetic grains of higher quality. U-Pb Isotopic Results A total of 79 individual analyses was collected. Of these, 6 are more than 10% discordant and are not considered further. Seven analyses have age errors greater than ± 60 Ma (2¿) from a combination of low U contents and high common Pb, and these are not considered useful age measurements. The remaining 64 analyses of 63 grains provide a useful detrital zircon age spectrum (Fig. 2). The detrital ages are dominated by two major groupings (Fig. 3) at ca. 1770-2000 Ma (30 grains, 47% of the data) and ca. 2400-2550 Ma (26 grains, 41% of data). Outside these groups there are two grains at ca. 2150 Ma and a thin scatter of earlier Archaean ages in the range ca. 2600-2950 Ma. Detail of the youngest end of the spectrum is provided in Figure 4. The age of the youngest individual grain 22 has been reproduced twice with a mean of 1773 ± 25 Ma (2¿), the relatively large uncertainty reflecting a U content below 75 ppm. A second grain 68 has a similar age of 1785 ± 30 Ma (2¿) and is statistically coherent with grain 22 (MSWD 1.6). The next-oldest grain 59 has a clearly resolved age of 1826 ± 14 Ma (2¿). Thus the youngest statistically definable group comprises two grains 22 and 68 which have a joint mean age of 1777 ± 19 Ma (2¿) and this provides an estimate of the maximum deposition age of the sediment.
Unnamed Metasedimentary Rock, Bmr Hay River-2
quartz gneiss

The date of 1334 +/- 6 Ma represents the maximum age of deposition, assuming that the protolith of this rock is sedimentary. If the protolith of this rock is an intrusion, then the dominant age cluster at c. 1333 Ma could be interpreted as the time of magmatic crystallization.
Wirku Metamorphics
Kirkland, CL, Wingate, MTD and Evins, PM 2011, 190245: migmatitic quartzofeldspathic gneiss, Kampurarr Pirti; Geochronology Record 932: Geological Survey of Western Australia, 4p.

Seventy-three analyses were undertaken on 73 zircon grains. Four analyses greater than 10% discordant and 2 analyses with a common 206Pb content higher than an arbitrary value of 0.5% are considered unreliable, and were removed from further consideration. The remaining 67 analyses are characterised by a wide range of U contents (61-849 ppm), Th contents (46-706 ppm) and Th/U (0.15-1.83). The analyses record 207Pb/206Pb ages between ~2721 Ma and ~1255 Ma, with dominant age clusters at ~1780 Ma, at ~1670 Ma and at ~1310 Ma. The youngest individual age (from 078.4.1.1) forms part of this youngest cluster, and the weighted mean age for this group is 1308 +/- 8 Ma (95% confidence; n = 21; MSWD = 1.3; probability of fit = 0.19). This weighted mean age is used to define the maximum depositional age for this sample. The weighted mean 207Pb/206Pb age of 1308 +/- 8 Ma (yielded by the youngest 21 analyses) is used to define the maximum age for deposition of the sandstone.
From ?Mesoproterozoic unit 2
WMC NJD 1
Korsch, R.J., Blewett, R.S., Pawley, M.J., Carr, L.K., Hocking, R.M., Neumann, N.L., Smithies, R.H., Quentin de Gromard, R., Howard, H.M., Kennett, B.L.N., Aitken, A.R.A., Holzschuh, J., Duan, J., Goodwin, J., Jones, T., Gessner, K., Gorczyk, W., 2013. Geological setting and interpretation of the southwest half of deep seismic reflection line 11GA-YO1: Yamarna Terrane of the Yilgarn Craton and the western Officer Basin. In: Neumann, N.L. (ed.) Yilgarn Craton-Officer Basin-Musgrave Province Seismic and MT Workshop. Geoscience Australia. Record, 2013/28, 24-50.

The weighted mean 206Pb-238U date indicated by this group is 725 +/- 11 Ma (chi-squared = 1.23. N = 11).
Kanpa Formation
NELSON, D. R., 2004, 154667: sandstone, Empress 1A; Geochronology dataset 258; in Compilation of geochronology data, June 2006 update: Western Australia Geological Survey.

Mosquito Creek Formation
Nelson, DR 2004, 169194: coarse lithic-quartz sandstone, Blue Spec mine; Geochronology Record 47: Geological Survey of Western Australia, 5p.

Dean Quartzite
Wingate, MTD, Kirkland, CL and Haines, PW 2015, 199404: sandstone, Robert Range; Geochronology Record 1256: Geological Survey of Western Australia, 6p.

Lansdowne Arkose
LENNARD RIVER_182106.1
Kirkland, CL, Wingate, MTD and Tyler, IM 2010, 182106: feldspathic sandstone, Mount Vincent; Geochronology Record 887: Geological Survey of Western Australia, 5p.

Pooranoo Metamorphics
WINNING POOL_208371.1
Wingate, MTD, Kirkland, CL, Korhonen, FJ and Johnson, SP 2017, 208371: quartzite, Emu Creek Bore; Geochronology Record 1359: Geological Survey of Western Australia, 6p.

Not explicitly stated what the age is interp'd as.
Chalmers Formation
2km south-south-east of Mount Chalmers, ROCKHAMPTON MGA 259425 7419479
Murray, C.G., Blake, P.R., Crouch, S.B.S., Hayward, M.A., Robertson, A.D.C., Simpson, G.A., 2012. Geology of the Yarrol Province central coastal Queensland. Queensland Geology, 13, 675pp.

autolithic quartz-tourmaline mudstone
Curran Curran rockhole
NELSON, D. R., 1999, 118580: autolithic quartz-tourmaline mudstone, Curran Curran rockhole; in Compilation of geochronology data, 1998: Western Australia Geological Survey, Record 1999/2, p. 185-189.

Wirku Metamorphics
Kirkland, CL, Wingate, MTD, Bodorkos, S and Smithies, RH 2011, 184150: metasandstone, Kampurarr Pirti; Geochronology Record 940: Geological Survey of Western Australia, 5p.

Mosquito Creek Formation
Nelson, DR 2005, 178010: lithic-quartz sandstone, Mount Olive; Geochronology Record 549: Geological Survey of Western Australia, 5p.

3602 +/-5 Ma. MSWD = 1.78. N = 24 variably discordant analysis
Corboy Formation
PORT HEADLAND_BEDOUT ISLAND_142836.1
Nelson, DR 1998, 142836: volcaniclastic sedimentary rock, Gorge Creek; Geochronology Record 393: Geological Survey of Western Australia, 4p.

DIXON RANGE_206131.1
Lu, Y, Wingate, MTD, Kirkland, CL, Maidment, DW, Phillips, C and Hollis, JA 2016, 206131: migmatitic pelitic gneiss, Six Mile Bore; Geochronology Record 1342: Geological Survey of Western Australia, 5p.

A more conservative estimate of the maximum depositional age is provided by the weighted mean 207Pb*/206Pb* date of 1179 +/- 5 Ma. MSWD = 0.99. N= 30 youngest for the 30 youngest analyses
Kirkland, CL, Wingate, MTD, Quentin De Gromard, R and Howard, HM 2014, 194806: metasandstone, Mitika Homestead; Geochronology Record 1198: Geological Survey of Western Australia, 6p.

Detrital provenance spectrum between ca 1847-3100 Ma
Halls Creek Group
meta siltstone

Thomas No. 1 was drilled in 1981 by Argonaut International Corporation under a farm-in agreement with Beach Petroleum N.L. and North Broken Hill Ltd. Thomas No. 1 was intended as an on-structure test of basal Cretaceous, Jurassic, Triassic and possibly Permian reservoirs (Wiltshire, 1982). The primary target was the Pedirka Basin early Jurassic and middle Triassic sandstone and shale sequence that had been first recognized at Poolowanna No. 1, where it contained oil shows. Lesser objectives were the basal Cretaceous Cadna-Owie Formation of the Eromanga Basin, known to contain oil and gas reservoir and source rocks in the region of the Cooper Basin, and rocks of the early Permian Pedirka Basin sequence, thought to underlie the Mesozoic units at Thomas 1 (Wiltshire, 1982). In Thomas 1, 157 m of indurated, hard, steeply-dipping, silty, dolomitic and calcareous fine sandstone, with quartz veins and quartzite intervals, was intersected below the Pedirka/Eromanga basins successions (Wiltshire, 1982). These sedimentary rocks were interpreted to represent low energy, shallow shelf environments, and were considered to be correlatives of late Neoproterozoic or early Cambrian successions of the Amadeus and Georgina basins (Edgoose and Munson, 2013). The sample comprises chips of calcareous sandstone collected over the interval 2578–2608 metres. A maximum depositional age for this sample will place a constraint on the age of pre-Pedirka Basin sediments in the Simpson Desert region.
Thomas 1
Kositcin, N., Verdel, C., Edgoose, C., 2023. Summary of results. Joint NTGS-GA geochronology project: western Warburton Basin, March 2022-February 2023. Northern Territory Geological Survey Record, 2023-006, 16pp.

Alt. max deposit age 207Pb/206Pb: 3502 +/- 4 Ma. MSWD = 1.13. N=330 are interpreted as detrital zircons
Salt Well Member
PORT HEDLAND_BEDOUT ISLAND_178020.1
Nelson, DR 2005, 178020: pebble conglomerate, Mount Grant; Geochronology Record 553: Geological Survey of Western Australia, 5p.

Immediately above the unconformity the basal Mount Thomas Quartzite of the Reynolds Range Group is a cross-bedded sandstone with quartz cement, in which heavy-mineral bands are preserved. It is interpreted as an intertidal-zone shallow-water sediment. A very large quantity of detrital zircon data was obtained for this sample. The spectrum is very similar to that in sandstone immediately below the unconformity, with a presence of 8 analyses in the age range 1785-1820 Ma that includes duplicate analyses of some grains. The youngest replicated individual grain age is 1785 ± 16 Ma (2¿) and the youngest coherent group of grains is 1798 ± 12 Ma. The remaining data are distributed across several groupings in the age range 1840-2700

sandstone (st)
Wingate, MTD, Bodorkos, S and Kirkland, CL 2008, 178852: sandstone, Palm Spring; Geochronology Record 744: Geological Survey of Western Australia, 5p.

Nelson, DR 2004, 169187: coarse lithic-quartz sandstone, Blue Spec mine; Geochronology Record 93: Geological Survey of Western Australia, 6p.

Beasley River Quartzite
Nelson, DR 2004, 169084: ferrigenous sandstone, Miringee Well; Geochronology Record 43: Geological Survey of Western Australia, 5p.

Nelson, DR 2004, 169094: quartz-plagioclase-biotitesillimanite gneiss, Woorkailjia Pool; Geochronology Record 88: Geological Survey of Western Australia, 6p.

Metasiltstone

Albarta Metamorphics
psammitic metasedimentary rock

Hardey Formation
MOUNT BRUCE_195895.1
Wingate, MTD, Lu, Y, Kirkland, CL and Johnson, SP 2017, 195895: sandstone, Moona Well; Geochronology Record 1363: Geological Survey of Western Australia, 6p.

A more conservative estimate of the maximum age of deposition: 1179 +/- 13 Ma. MSWD = 1.8. N = 17 youngest analyses
Kirkland, CL, Wingate, MTD, Quentin De Gromard, R, Howard, HM and Smithies, RH 2014, 208414: quartzite, Mitika Homestead; Geochronology Record 1205: Geological Survey of Western Australia, 6p.

meta-arkose with graded bedding
Bodorkos, S, Love, GJ, Nelson, DR and Wingate, MTD 2006, 178747: metamorphosed feldspathic sandstone, North East Bore; Geochronology Record 643: Geological Survey of Western Australia, 4p.

Group Y comprises one analysis, which yields a 207Pb*/206Pb* date of 1071 +/- 18 Ma (1 sigma). Group S comprises 48 analyses, which yield 207Pb*/ 206Pb* dates of 2870-1075 Ma. A more conservative estimate of the maximum depositional age can be based on the weighted mean 207Pb*/206Pb* date of 1105 +/- 24 Ma (MSWD = 2.2) for the youngest eight analyses in Groups Y and S.
Wankari Volcanics
Wingate, MTD, Lu, Y, Quentin de Gromard, R, Howard, HM and Haines, PW 2017, 208498: quartzite, Dean Creek; Geochronology Record 1440: Geological Survey of Western Australia, 6p.

meta sandstone
Bodorkos, S, Love, GJ, Nelson, DR and Wingate, MTD 2006, 178746: metamorphosed quartz sandstone, Chubba Well; Geochronology Record 642: Geological Survey of Western Australia, 4p.

A more conservative estimate of the maximum depositional age can be based on the weighted mean 207Pb*/206Pb* date of 1147 +/- 13 Ma (MSWD = 0.73) for the 17 youngest
Dixon Range beds
Wingate, MTD, Kirkland, CL and Haines, PW 2015, 199408: sandstone, Dixon Range; Geochronology Record 1258: Geological Survey of Western Australia, 5p.

lithic quartz sandstone
Nelson, DR 2002, 169061: lithic quartz sandstone, Yangibana Yard; Geochronology Record 135: Geological Survey of Western Australia, 4p.

Possible very thin felsic tuff layers (although thin-section seems to suggest quartz-only) within siltstone.
Wonominta Region
Black, L.P., 2007. SHRIMP U-Pb zircon ages obtained during 2006/07 for NSW Geological Survey projects. Geological Survey of New South Wales Report GS, 2007/298, 84p.

Tollis Formation
Sample appears to have black tuff shards.
Katherine Gorge Road

basal quartzite, Bimba Formation, Ameroo Hill
The quartzite forms prominent rib along a ridge crest east of the low saddle at Ameroo Hill. The sample was collected to determine the depositional age of the Bimba Formation, and the age of an early migmatisation event, the latter to test the hypothesis of high-grade deformation pre-dating the Olarian Orogeny (Gibson and Nutman 2004). In thin section, this sample displays an inequigranular granoblastic metamorphic texture. Quartz dominates the rock, occurring as equant anhedral grains mostly ~0.4-1.0 mm in size. All display weak shadowy strain extinction. The size and shape of the quartz grains allows the interpretation that primary quartz particles have suffered grain boundary migration and suturing during metamorphism. K-feldspar is moderately abundant, forming smaller anhedral grains and aggregates ~0.2-0.4 in size. They lie in granoblastic equilibrium texture with the quartz, and occupy interstices between the larger quartz grains. Some of the K-feldspar grains display the combined albite-pericline twinning (‘tartan’ twinning) that is characteristic of microcline. Rare twinned plagioclase grains are identified in contact with K-feldspar grains. Muscovite occurs in minor amount as large platy flakes up to ~1 mm in size. They lack a preferred orientation. Opaques occur in significant amount for an accessory phase. They form small equant crystals mostly ~0.1-0.2 mm in size, disseminated uniformly throughout the rock. Their size and shape suggest they are ?magnetite. Biotite occurs in minor amount as small pleochroic brown flakes ~0.2-0.4 mm long. They are sparsely distributed through the rock. Tourmaline occurs in trace amount as pleochroic green grains. Rutile is uncommon, forming small granules in small loose aggregates that possibly represent severely modified precursor Fe-Ti oxide grains (? ilmenite). Zircon occurs in significant amount for an accessory phase.

Reddish poorly sorted lithified layer near top of red bed sandstone sequence.
Jagodzinski, E.A., Bodorkos, S., Crowley, J.L., Pawley, M.J., Wise, T.W., 2019. PACE Copper Coompana Drilling Project: U-Pb dating of basement and cover rocks. Geological Survey of South Australia. Report Book, 2018/00028, 211p.

An alternative interpretation is that the concordant 207Pb*/206Pb* date of 2988 +/- 5 Ma (1sigma) for the single analysis in Group Y represents a maximum age of igneous crystallization of the felsic volcanic eruptive component of this rock.
Metarhyolite
Wingate, MTD, Bodorkos, S and Van Kranendonk, MJ 2009, 180048: felsic metavolcanic rock, Cattle Well; Geochronology Record 807: Geological Survey of Western Australia, 4p.

Monotonous medium-grained sandstone towards base of red bed sequence.

Ooloo Hill Formation
The drillhole penetrates only sediments, comprising laminated to massive, greyish to tan hued shales and thick, dark brownish-grey siltstone that is either well laminated or massive. These fine-grained sediments contain well preserved small-scale slump structures, slump breccias, cross bedding, ripple marks, small scour-and-fill structures, and fine lamellae. There are also pale hued sandstone beds and lamellae intercalated within the shales and siltstones. Sample R1837680 is selected from near the base of the drill core and consists of sandstone with less shale and siltstone thin bands, slumps and lamellae.
Sheard, M.J., White, M.R., Stoian, L., Jagodzinski, E.A., 2012. Explanatory notes for Marree, South Australia 1:250 000 geological map, sheet SH54-5. Geological Survey of South Australia. Report Book, 2012/00004, 231p.; Wade, C.E., Reid, A.J., Jagodzinski, E.A., Sheard, M.J., 2023. Mid-Devonian basaltic magmatism and associated sedimentation: the Ooloo Hill Formation, central-eastern South Australia. Australian Journal of Earth Sciences, 70, 22p.

Drummond Formation
This sample of Drummond Formation is a thickly bedded pale cream-coloured, well-sorted quartz sandstone with minor opaques (possibly ilmenite). The outcrop is highly fractured resulting in a coarse blocky appearance, with iron straining along joints. The sample location is at the crest of an upright open east-west trending anticline, roughly 1km north of the east-west trending Littles Range Fault. The outcrop comprises ripple marked pale-white well-sorted medium-grained quartz sandstone, thinly to moderately bedded (10-50 cm), interlayered with argillaceous layers.

Kirkland, CL, Wingate, MTD, Hollis, J and Phillips, C 2015, 206119: metasandstone, Bullman Copper prospect; Geochronology Record 1239: Geological Survey of Western Australia, 6p.

medium-grained sandstone

alt. max dep age: 1876 +/- 4 Ma. MSWD=1.2. N=34
Marboo Formation
Kirkland, CL, Wingate, MTD, Hollis, J and Phillips, C 2014, 206154: pelitic migmatite, Paperbark Bore; Geochronology Record 1204: Geological Survey of Western Australia, 6p.

the ages of detrital components within sediments that have been reworked into this rock.
Marboo Formation
LENNARD RIVER_212344.1
Lu, Y, Wingate, MTD, Kirkland, CL, Maidment, DW, Phillips, C and Hollis, JA 2016, 212344: pelitic schist, Napier Creek; Geochronology Record 1348: Geological Survey of Western Australia, 6p.

This sample was collected from a conspicuous line of outcrops near Black Rock Dam about 14 km southwest of Selwyn on the southern side of the Selwyn–Chatsworth Road. They consist of banded, very fine-grained, dark grey calcareous metasandstone or calc-silicate mapped as Staveley Formation. In thin section, the sample consists of ~40% very fine-grained (<0.05 mm) quartz and feldspar, ~20% calcite to 0.5 mm and ~25% subparallel flakes of biotite to 0.1 mm defining a foliation. In addition, larger flakes of muscovite to 0.5 mm lie across the foliation. Lenticular aggregates up to 5 mm long of coarser calcite and muscovite (~0.5 mm) are oblique to the foliation. This sample of Staveley Formation was selected to provide an additional maximum depositional age constraint for the formation.

Maximum depositional age is a weighted average age c. 294 Ma. Contrasts with known deposition age of the sediment being early Permian.
Poole Sandstone
basal Poole Sandstone fS, lowest bench in Poole Ss

Maximum depositional age is a weighted average age c. 251 Ma. Contrasts with known deposition age of the sediment being late Permian.
Cherrabun Member
Hardman Fm fine S

There is only a minor difference between the younger MIX component and the pooled age suggesting that the inclusion of analyses from type C zircon has little effect on the ages of the two components present in the post-1900 Ma data set from metapelite 95SB11. Mixture 'MIX' Model-derived age component, weighted mean 207Pb/206Pb: Age:1867 +/-4Ma. N= 19. Conf.= 95%.
DIXON RANGE_95SB11
Bodorkos, S., Oliver, N.H.S., Cawood, P.A., 1999. Thermal evolution of the central Halls Creek Orogen, northern Australia. Australian Journal of Earth Sciences, 46(3), 453-465.; Bodorkos, S., Cawood, P.A., Oliver, N.H.S., Nemchin, A.A., 2000. Rapidity of orogenesis in the Paleoproterozoic Halls Creek Orogen, northern Australia; evidence from SHRIMP zircon data, CL zircon images, and mixture modeling studies. American Journal of Science, 300(1), 60-82.

A total of 88 analyses were collected from 88 zircon crystals. Four analyses have excessively high or low 206Pbc (> 0.90% or < -1.50%). Another ten analyses yield individual 207Pb/206Pb dates that are older than 1400 Ma, but are more than 10% discordant. Another analysis gave a spurious result from isotopic mixing across internal domains, resulting in heterogeneous Pb ratios. These 15 analyses are interpreted as unreliable and are not considered further. The remaining 73 analyses are characterised by low to moderate U contents (31-811 ppm, median 154 ppm), a wide range of Th/U (0.03-2.20, median 0.58), and low 206Pbc (maximum 0.60%, median 0.01%). The 73 accepted analyses are divided into five groups: Group 1 consists of the three youngest zircons that combine to yield 238U/206Pb weighted mean age of 513 +/- 24 Ma (95% confidence; MSWD = 0.09; Pequiv = 0.91); Group 2 consists of 24 analyses from 24 zircons with individual 238U/206Pb dates between c. 615 Ma and 530 Ma; Group 3 consists of 36 analyses from 36 zircons with individual 238U/206Pb dates between c. 1235 Ma and 895 Ma; Group 4 consists of three analyses from three zircons with individual 207Pb/206Pb dates between c. 2000 Ma and 1410 Ma; and Group 5 consists of seven analyses from seven zircons with individual 207Pb/206Pb dates pre-2000 Ma.The 238U/206Pb weighted mean age of 513 +/- 24 Ma (95% confidence; n = 3) is interpreted as a maximum depositional age for the 1100 m interval of the Lesueur Sandstone (Yalgorup Member). This age is considerably older than the biostratigraphically (S. speciosus to M. crenulatus Zones) assigned Late Triassic depositional age of this unit.

Stairway Sandstone
The Stairway Sandstone of the Larapinta Group consists predominantly of sandstone with lesser siltstone and limestone (Edgoose 2013). Fossils constrain the age of the Stairway Sandstone to the Middle Ordovician (467-458 Ma). The top of the formation is well constrained by its transitional contact with the Stokes Siltstone, which is early Gisbornian (460-456 Ma; Gibb et al 2009). The age of the formation is therefore most likely Darriwilian (467-458 Ma; Edgoose 2013 and references therein). A previous detrital zircon sample of the Stairway Sandstone from the adjacent HENBURY mapsheet produced a maximum depositional age of 514 +/- 6 Ma (Normington et al 2018). This sample (LA19VJN121) is a moderately sorted, fine-grained sandstone collected from a ridge 100 km west-southwest of Kings Canyon.

quartz-muscovite-biotite-plagioclase- epidote schist
Nelson, DR 2002, 169056: quartz-muscovite-biotite-plagioclase- epidote schist, Fraser Prospect; Geochronology Record 129: Geological Survey of Western Australia, 4p.

age of a detrital component within sediments that have been reworked into this rock.
Mount Joseph Migmatite
Lu, Y, Wingate, MTD and Hollis, JA 2017, 212317: pelitic migmatite, Mount Joseph; Geochronology Record 1389: Geological Survey of Western Australia, 4p.

Kulail Sandstone
Wingate, MTD, Kirkland, CL and Haines, PW 2015, 199407: sandstone, Robert Range; Geochronology Record 1257: Geological Survey of Western Australia, 6p.

This sample is a siliceous metasediment, collected from Polygonum DD 95 SR1 303-307.7 m. The drill core rock sample is composed mostly of fine-grained even-grained translucent pale grey rock. Scattered irregularly through the rock are dark greenish black diffuse patches, commonly with relatively coarse-grained yellowish ragged sulphide grains. In thin section, this sample displays a massive, even-grained granoblastic metamorphic texture with very little or no evident retrogressive alteration. Quartz dominates the rock, occurring as small equant anhedral grains ~0.2-0.4 mm in size. They form a more or less equigranular sutured granoblastic mosaic throughout the rock. Feldspar (plagioclase) occurs in minor amount forming small albite-twinned anhedral grains that tend to form interstices between slightly larger quartz grains. Muscovite occurs mostly as small but well-crystallised ragged flakes ~0.1-0.2 mm in size. A weak preferred orientation defines a weak foliation. Larger flakes up to ~0.4 mm long are intimately intergrown with chalcopyrite, magnetite, hematite and chlorite in coarser-grained patches. Magnetite is disseminated sparsely throughout the rock as small equant crystals of subhedral cubic morphology. Their average size is ~0.2 mm. Chalcopyrite is present in minor amounts. In places it forms relatively large ragged patches up to ~ 2mm in size, and these tend to be intergrown with similarly coarser-grained muscovite and hematite. Chalcopyrite also occurs as tiny ragged grains sparsely and irregularly disseminated through the rock, in places in granoblastic relationship with principal metamorphic minerals (i.e. quartz, muscovite, magnetite). Chlorite is present in minor amount, forming fine-grained pleochroic green aggregates intimately intergrown with coarser-grained chalcopyrite, hematite, muscovite and magnetite. Pyrite and rutile are rare.

metasandstone (mt)

Whim Creek Group
Whim Creek
Nelson, DR 2000, 142949: metasandstone, Whim Creek; Geochronology Record 299: Geological Survey of Western Australia, 5p.

The Crow Formation (Rawlings et al., 2008) is a largely recessive unit that outcrops poorly throughout the western two-thirds of MOUNT DRUMMOND. The Crow Formation is composed of up to 2500 m of interbedded siltstone, sandstone, shale and lesser conglomerate (Rawlings et al., 2008). This sampled unit also represents an ‘unnamed’ unit (Psos) as mapped on MOUNT DRUMMOND (Rawlings et al., 2008). This sample was collected immediately south of unnamed subunit GA 2786168, 400 m to the north. The structural and stratigraphic relationships between the two sample sites are unclear due to Cainozoic cover. There are considerable lithological differences between these two adjacent Crow Formation subunits and this sample was collected to test the stratigraphic integrity between the two. Sample GA 2786181 is a poorly outcropping, thinly- to medium-bedded silicified purplish-quartz sandstone, in contrast to the texturally immature highly feldspathic micaceous sandstone of GA 2786168.

Nelson, DR 2004, 169199: coarse lithic-quartz sandstone, Branchies Well; Geochronology Record 48: Geological Survey of Western Australia, 5p.

The Liddle Formation is part of the Winnall Group (formerly Winnall beds of Ranford et al 1965, redefined by Donnellan and Normington 2017). The formation is exposed in generally northwest-striking ridges in the central and western parts of the Amadeus Basin. At its type-section in HENBURY, the Liddle Formation is overlain by the Puna Kura Kura Formation, the uppermost part of the Winnall Group. The Liddle Formation is probably late Ediacaran based on its stratigraphic position (Donnellan and Normington 2017). A previous sample of the Liddle Formation from BLOODS RANGE produced a detrital zircon maximum depositional age of 696 +/- 13 Ma (Beyer et al 2020). Sample LA19CSV152 is a light-grey to white, well-sorted, fine-grained sandstone with distinctive festoon cross-stratification collected from a long, prominent ridge ~40 km east of Winnall Ridge.

A more conservative estimate of the maximum depositional age can be based on the weighted mean 238U/206Pb* date of 522 +/- 13 Ma MSWD = 0.07. N = three youngest analyses.
Worral Formation
Wingate, MTD and Haines, PW 2009, 135967: mudstone, Sahara 1; Geochronology Record 782: Geological Survey of Western Australia, 5p.

The sample selected for geochronology is from a coal exploration hole (OR17) drilled by Utah Development Company in 1976 (Murray, 1979). This hole is located ~25 km northwest of the nearest known outcrop of Sefton Metamorphics and intersected schist at 133 metres, which is overlain by Jurassic sedimentary rocks of the Carpentaria Basin. The rock sampled from drill core is a medium-grained biotite-garnet schist characterised by steeply dipping bands of biotite-muscovite-rutile and quartz-muscovite. At least two deformations are recognised; one parallel to bedding and another at a low angle to the first. The unit sits unconformably below the Carboniferous-Triassic Olive River Basin, and is likely to be a northern continuation of the Sefton Metamorphics.

Sandstone

A more conservative estimate of the maximum age of deposition: 1180 +/- 8 Ma. MSWD = 1.5. N =27 youngest analyses
Kirkland, CL, Wingate, MTD, Quentin De Gromard, R and Smithies, RH 2014, 201311: metasandstone, Yulun-Kudara Waterhole; Geochronology Record 1202: Geological Survey of Western Australia, 5p.

Wire Creek Sandstone
The Wire Creek Sandstone (Sweet, 1981; Grimes and Sweet, 1979; Ahmad and Wygralak, 1989) outcrops along the southeastern margin of the Murphy Province in CALVERT HILLS. The type locality and formal description of the unit are from the Hedleys Creek 100K mapsheet in Queensland (Sweet, 1981). The unit is broadly characterised as a coarse-grained, gritty quartz sandstone, occasionally cross-bedded, with pebble lags and local cobble to boulder conglomerate lenses, containing rounded clasts of predominantly white vein quartz, quartzite, felsic volcanics and rarely, granite (presumably underlying basement Nicholson Granite) up to 30 cm in diameter (Sweet, 1981). The lithofacies of the Wire Creek Sandstone is consistent with a braided stream and/or alluvial fan depositional environment (Ahmad and Wygralak, 1989). At the sample location, the Wire Creek Sandstone is a massively bedded, gritty feldspathic quartz sandstone. In thin section, sample 2786185 is a well- to moderately well-sorted sandstone. Quartz grain boundaries are irregular, serrated and/or cuspate, forming an interlocking pattern with adjacent grains, suggesting post-deposition grain boundary migration due to diagenetic dissolution and re-precipitation processes. Undulose extinction in quartz grains is common. Feldspar (ca 5-10 modal %) is typically microcline (exhibiting tartan or cross-hatched twinning) and have a subhedral tabular habit. Rare mica (muscovite?) and tourmaline are present as small isolated flakes.

NELSON, D. R., 2002, 169119: metasandstone, Fandango Prospect; in Compilation of geochronology data, 2001: Western Australia Geological Survey, Record 2002/2, p. 80-83.

youngest significant peak not affected by Pb loss
Age is the youngest significant peak. Concordia age 425.5 +/- 5.6 Ma. Age distribution and increasingly discordant analyses towards young ages suggest that this sample experienced Pb loss probably during a recent metamorphic event. The population least affected consists of analyses between 396-454 Ma (most significant age peak is ~ 425 Ma). More reliable estimate of the zircons age prior to the disturbance of the U-Pb system is given by an intercept of the Concordia. Results interpreted by R. Tilhac
Tilhac 2019 paraphrased "The sample is a meta-sandstone, which has colourless to pale yellow stubby zircon crystals and broken fragments, equant to weakly elongated, euhedral to subhedral, with abundant inclusions. With a mix of different features: mostly oscillatory zoned, some sector zoning and diffuse features, a few core-rim features.
Tilhac, R. (2019). Zircon U-Pb dating: TerraneChron report to the Geological Survey o fNew South Wales (TC-182). CCFS and GEMOC Macquarie University. Geological Survey of New South Wales, Maitland. File GS2019/0446.

Gator Sandstone
The Gator Sandstone is conformable on the Mitchiebo Volcanics, and is unconformably overlain by the Top Rocky Rhyolite. Thicknesses range between 100 m and 700 m. Rawlings et al. (2008) described the Gator Sandstone as a fine- to coarse-grained quartz to sub-lithic sandstone, with pebble lags. Trough cross-beds symmetrical ripple marks, desiccation cracks and mud rip-up clasts are common. The depositional environment is interpreted as moderate to high energy braided fluvial to supratidal (Rawlings et al., 2008). Deposition is bracketed (Rawlings et al., 2008) between the underlying Murphy Province basement (>1845 Ma, Page et al., 2000) and the overlying Top Rocky Rhyolite (1725 Ma, Page et al., 2000). At the sample locality, the Gator Sandstone is a pale cream to white, well-sorted silicified quartz sandstone, with ferruginous and minor purple staining along fractures, joints and on bedding surfaces. Asymmetrical ripple marks, bed load casts and other bedforms are common. Bedding is typically poorly defined, usually massive, forming blocky rubbly outcrop.

Alroy Formation
This sample is a fine-grained, foliated and laminated biotite-feldspar-quartz phyllite. The recrystallised assemblage is dominated by fine-grained, granoblastic feldspar, quartz, biotite and a small amount of white mica. Granoblastic feldspar appears to be a dominant constituent, and fine-grained, granoblastic quartz is abundant in the groundmass. There are a few larger aggregates of quartz and feldspar, suggesting that they are relict clasts from the sedimentary or volcaniclastic protolith. Mica is represented by biotite and white mica, showing simultaneous mineral growth. At least two generations of mica are present. Accessory phases include zircon, sub-euhedral apatite and dark green tourmaline. Crenulation cleavage is weakly defined, and the unit is cut by calcite veins.

The sample is a fine- to medium-grained garnet amphibolite, with a radiating texture comprising actinolite and minor amounts of albite and epidote. The dominant rock-forming mineral is amphibole, which occurs as radiating acicular and euhedral prismatic actinolite crystals, up to 600 microns long. There was some minor replacement of amphibole by chlorite. Garnet occurs as separate porphyroblasts and as aggregates, and has been partially replaced by both biotite and limonite around the rims and in fractures. The rock groundmass comprises very fine-grained granoblastic quartz and feldspar, likely to be albite. Trace amount of white mica and epidote are present. The opaque minerals appear to be hematite and sulphides. Crosscutting veins are zoned comprising epidote, limonite, aragonite, iron oxides needles and quartz.

This sample is a fine-grained metapelite, comprising a thinly interlaminated phyllite and carbonaceous metasiltstone. The lamination is plane-parallel, with lamellae thicknesses of 0.01-3 mm. The mica-rich phyllite layers contain little carbonaceous material (1-5%), while the quartz-feldspathic metasiltstone layers are carbon-rich, comprising up to 30% carbonaceous grains. Most of the rock is fine-grained, with a few quartz and feldspar porphyroblasts. Quartz and feldspar are the dominant minerals. Prevailing in the phyllite layers, sericite/muscovite showed at least two generations of growth. Pyrite occurs as both sub-euhedral grains and aggregates of anhedral grains, up to 5 mm across, in association with granoblastic chlorite-K-feldspar-quartz veins, while the fine-grained groundmass contains scattered smaller pyrite grains, up to 10 micron in diameter. K-feldspar-chlorite-pyrite-quartz lenses, veins and bands, up to 2 mm thick, cross-cut the unit.

two other grains dated (218.52, 218.29 Ma) interpreted as containing inherited or detrital components

Northeast Tasmania Region
Yim, W.W.-S., Gleadow, A.J.W., Van Moort, J.C., 1985. Fission track dating of alluvial zircons and heavy mineral provenance in Northeast Tasmania. Journal of the Geological Society, 142(2), 351-356p.

(VT1)zircons were first dated by ion microprobe using the SHRIMP II at Curtin University, Perth, or a Cameca ims 1270 at the Swedish Museum of Natural History, Stockholm; pooled weighted average. Detrital suite
Violet Town Volcanics
Kemp, A.I.S., Hawkesworth, C.J., Paterson, B.A., Foster, G.L., Kinny, P.D., Whitehouse, M.J., Maas, R., EIMF, 2008. Exploring the plutonic-volcanic link: a zircon U-Pb, Lu-Hf and O isotope study of paired volcanic and granitic units from southeastern Australia. Transactions of the Royal Society of Edinburgh: Earth Sciences, 97(4), 337-355.

(VT3)=87Sr/86Sr (t) 0·70832 to 0·71109; ENd(t) - 4·2 to -4·8; zircons were first dated by ion microprobe using the SHRIMP II at Curtin University, Perth, or a Cameca ims 1270 at the Swedish Museum of Natural History, Stockholm; pooled weighted average
Violet Town Volcanics
Kemp, A.I.S., Hawkesworth, C.J., Paterson, B.A., Foster, G.L., Kinny, P.D., Whitehouse, M.J., Maas, R., EIMF, 2008. Exploring the plutonic-volcanic link: a zircon U-Pb, Lu-Hf and O isotope study of paired volcanic and granitic units from southeastern Australia. Transactions of the Royal Society of Edinburgh: Earth Sciences, 97(4), 337-355.

Stony Head Sandstone
Lefroy Sandstone
Ridgers, B., 2017. Pb isotopic characterisation of ore deposits and prospects from northeast Tasmania. University of Tasmania, Hobart., BSc Hons thesis, 93pp.

The Simpson 1 well was drilled by Central Petroleum Ltd in 2008 in the Pedirka Basin, Northern Territory. Simpson 1 was drilled to test the Algebuckina, Poolowanna, Tirrawarra, Purni, and Crown Point formations, as well as the uppermost part of the Warburton Basin. The primary objective of the well was the Poolowanna Formation, whilst the Cadna-owie Formation and Algebuckina Sandstone were secondary targets (Central Petroleum, 2009). The well reached a total depth of 2165 m in the Warburton Basin (Central Petroleum, 2009). The sample comprises chips collected over the interval 2142–2165 metres depth. From 2142 m cuttings were described as light grey to greenish grey, fine- to medium-grained, moderately to poorly sorted sandstone. The sandstone is silificied and contains minor white kaolin and chloritic matrix, rare silicified siltstone lithic grains and occasional mica flakes (Central Petroleum, 2009). Below 2151 m, 30–50% shale was present in the samples. The shale is described as mid to dark red-brown, occasionally pale yellow-brown, micromicaceous, and sub-phyllitic (Central Petroleum, 2009). The 2142–2165 m interval marks the top of the Warburton Basin succession, and is in sharp contact with overlying well sorted Permian sandstone of the Pedirka Basin (Central Petroleum, 2009; Edgoose and Munson, 2013). The sample was selected to place constraints on the depositional age of this part of the Warburton Basin.
Simpson 1
Kositcin, N., Verdel, C., Edgoose, C., 2023. Summary of results. Joint NTGS-GA geochronology project: western Warburton Basin, March 2022-February 2023. Northern Territory Geological Survey Record, 2023-006, 16pp.

Two dominant populations span age ranges of 700-515 Ma and 1150-900 Ma (94 concordant results from 100 analyses). Mean age.
Bunker Creek Formation
Johnson et al 2016 paraphrased: "The sample is from the Bunker Creek Formation of the Teltawongee Group, and was sampled from a monotonous package of immature sandstone. The sample contains a high proportion of angular quartz and detrital mica, and to a lesser extent, feldspar and tourmaline. The Bunker Creek Formation is characterised by repetitive sequences of immature sandstone (up to 3 m thick in places) overlain by an upward fining sequence of fine sandstone, siltstone and mudstone (Mills, 1992). In places, the finer-grain lithologies are absent, which results in an amalgamation of coarse-grained sandstone horizons that give the appearance of an extremely thick (~10 m), monotonous package of immature sandstone (Mills, 1992). Zircons from the sample are rounded and have low aspect ratios. Internal grain textures are characterised by faint oscillatory to homogeneous zoning. Heterogeneous textures consisting of patchy sub-domains potentially indicate a complex metamorphic history for some of the grains. The presence of older cores with younger rims also indicates multiple phases of zircon crystallisation."

laser ablation: GeoLas 193nm ArF laser ablation system
James Cook University
Youngest detrital zircon population from a combination of two samples (066_SH_DE, 019_SH_SM) from Early Permian Nambucca block.
Shaanan et al 2015 paraphrased "The sample was extracted from a slate at Billybyang Creek Road. Zircon crystals range from elongate euhedral to abraded and well-rounded morphologies. Their maximum length is 325 um, and the mean apparent elongated axis is 108 um. Under cathodoluminescence, most crystals exhibit well-defined oscillatory zoning, and some contain convolute zoning or absence of zoning
Shaanan, U., Rosenbaum, G. & Wormald, R. (2015). Provenance of the Early Permian Nambucca block (eastern Australia) and implication for the role of trench retreat in accretionary orogens. Geological Society of America Bulletin 127, pp.1052-1063.

University of Melbourne
Local mine grid: 8149.805N 1938.237E; laserprobe; single-step laser ablation; unexpected old and scattering ages.. Samples Fosterville giving anomalously old apparent ages due to incorporation of detrital mica grains that were not reset during mineralising process (from Fu, 2007)
Phoenix ore zone
BENDIGO_SPD 221_FV
MacCulloch, J., 2005, 40Ar/39Ar constraints on the timing of gold mineralisation in the Fosterville, Nagambie and Walhalla deposits. B.Sc (Hons) thesis, Monash University, Melbourne (unpubl.), 80pp.

Local mine grid: 8149.805N 1938.237E; laserprobe; single-step laser ablation for total fusion age; unexpected old and scattering ages.. Samples Fosterville giving anomalously old apparent ages due to incorporation of detrital mica grains that were not reset during mineralising process (from Fu, 2007)
Phoenix ore zone
BENDIGO_SPD 221_FV
MacCulloch, J., 2005, 40Ar/39Ar constraints on the timing of gold mineralisation in the Fosterville, Nagambie and Walhalla deposits. B.Sc (Hons) thesis, Monash University, Melbourne (unpubl.), 80pp.

Local mine grid: 8149.805N 1938.237E; laserprobe; single-step laser ablation;. Samples Fosterville giving anomalously old apparent ages due to incorporation of detrital mica grains that were not reset during mineralising process (from Fu, 2007)
Phoenix ore zone
BENDIGO_SPD 221_FV
MacCulloch, J., 2005, 40Ar/39Ar constraints on the timing of gold mineralisation in the Fosterville, Nagambie and Walhalla deposits. B.Sc (Hons) thesis, Monash University, Melbourne (unpubl.), 80pp.

Out of 99 analyses, 66 concordant results were obtained, with the majority of ages falling in the range of 650-450 Ma. This is the youngest population.
Boshy Formation
Johnson et al 2016 paraphrased: "The sample is from the Boshy Formation, which conformably sits atop of the basally located Morden Formation. The sample is well-sorted and is composed of sub-rounded grains of quartz. The dominance of quartz and the minor fractions of feldspar in samples KB22a, KB21 and KB23 from the Kayrunnera Group indicate that the contributing sediments were probably derived from a cratonic source. Sample KB23 contains detrital zircon grains that dominantly have euhedral morphologies with oscillatory zoning."

laser ablation: GeoLas 193nm ArF laser ablation system
James Cook University
Youngest detrital zircon population from a combination of two samples (066_SH_DE, 019_SH_SM) from Early Permian Nambucca block.
Shaanan et al 2015 paraphrased "The sample was extracted from a Lithic sandstone at Smokey Cape. Zircon crystals range from elongate euhedral to abraded and well-rounded morphologies. Their maximum length is 325 um, and the mean apparent elongated axis is 108 um. Under cathodoluminescence, most crystals exhibit well-defined oscillatory zoning, and some contain convolute zoning or absence of zoning
Shaanan, U., Rosenbaum, G. & Wormald, R. (2015). Provenance of the Early Permian Nambucca block (eastern Australia) and implication for the role of trench retreat in accretionary orogens. Geological Society of America Bulletin 127, pp.1052-1063.

Tarran Volcanics
Felsic A-type porphyritic dyke member
Downes P., Blevin P., Armstrong R., Simpson C., Sherwin L., Tilley D. & Burton G. (2016) Outcomes of the Nymagee mineral system study - an improved understanding of the timing of events and prospectivity of the central Lachlan Orogen., Quarterly Notes of the Geological Survey of New South Wales 147.

Youngest detrital zircon population from a combination of four samples (053_SH_AK, 073_SH_NW, 031_SH_HA, 007_SH_BU) from Early Permian Nambucca block.
Shaanan et al 2015 paraphrased "The sample was extracted from a slate at Bundagen Headlands. Zircon crystals range from elongate euhedral to abraded and well-rounded morphologies. Their maximum length is 325 um, and the mean apparent elongated axis is 108 um. Under cathodoluminescence, most crystals exhibit well-defined oscillatory zoning, and some contain convolute zoning or absence of zoning

Booda Formation
Hack et al 2018 paraphrased: "This sample was collected from outcrop at the southern end of the Oxley Ranges, about 40km east of Bourke. The outcrop is well-exposed, moderately weathered and weakly foliated. The unit is unconformably overlain by an outlier of Mulga Downs Group (Fraser et al., 2014). Microstructures include a well-developed tectonic foliation defined by muscovite. A much weaker foliation is defined by the alignment of small mica plates (up to ~10 mm). Zircon grains are 50-200 um for the long axis and are commonly sub-angular to sub-rounded with minor euhedral grains present. Grains are commonly pale brown with generally poor grain condition with fractures and inclusions being common. Internal zoning is variable from oscillatory through to patchy and convoluted."

sheared felsic intrusive 82180
This sample is a well-laminated, fine- to medium-grained metasedimentary psammopelitic rock, with individual laminations ranging from quartz-feldspar- to biotite-rich layers. Compositional lamination is well preserved and on the scale of <0.5 mm to several millimetres in thickness. Relict grading is present in individual beds, although the detrital grain texture has been partially destroyed by recrystallisation. The rock-forming minerals are feldspar, quartz and biotite, with smaller amounts of tourmaline, rutile and zircon. The dominant mineral component is feldspar, with sub-euhedral, tabular and lath-shaped grains up to 300 microns long. The feldspar has been intensively altered by sericite. Biotite-rich lamellae comprise sub-euhedral biotite, minor quartz and metamorphic K-feldspar. Porphyroclastic and lepidoblastic biotite is also present in feldspar-quartz-rich layers. The biotite has been partially replaced by chlorite and contains abundant rutile inclusions. Some calcite veining was associated with biotite-rich lamellae. Accessory phases include tourmaline, zircon and an opaque mineral that appears to be pyrite.

This sample is a medium-grained, lepidogranoblastic sillimanite-bearing white mica-biotite schist. A well-developed foliation is defined mainly by biotite and by elongated quartz and feldspar grains. The rock-forming assemblage includes quartz, feldspar, biotite, muscovite and trace amounts of sillimanite (fibrolite) and chlorite. The metamorphic, sub-euhedral to anhedral feldspar displays zoning, with clear rims and cores, contains inclusions of apatite and fluids, and has been altered by sericite. Elongated biotite has been partially replaced by chlorite. Porphyroblastic white mica has overprinted the biotite and feldspar. White mica and large quartz grains enclose fibrous aggregates of sillimanite. Accessory phases include zircon, apatite and rutile inclusions in biotite. The unit is crosscut by K-feldspar (adularia?)-calcite veins up to 300 microns wide.

Youngest detrital zircon population from a combination of four (053_SH_AK, 073_SH_NW, 031_SH_HA, 007_SH_BU) samples from Early Permian Nambucca block.
Shaanan et al 2015 paraphrased "The sample was extracted from a microconglomerate at Korogoro/Hat Head. Zircon crystals range from elongate euhedral to abraded and well-rounded morphologies. Their maximum length is 325 um, and the mean apparent elongated axis is 108 um. Under cathodoluminescence, most crystals exhibit well-defined oscillatory zoning, and some contain convolute zoning or absence of zoning

Booda Formation
Abdullah et al 2020 paraphrased "Sample 17-ST-02 is a mature, well-sorted coarse-grained (50-100 um) metasiltstone from the Booda Formation. The sample contains pressure solution seams (comprising goethite and ilmenite) that define a dominant foliation. The majority of quartz grains exhibit undulose extinction and serrated boundaries that likely formed by grain boundary migration."

87Sr/86Sr (t) 0·71154; ENd(t) n/a; zircons were first dated by ion microprobe using the SHRIMP II at Curtin University, Perth, or a Cameca ims 1270 at the Swedish Museum of Natural History, Stockholm; pooled weighted average
Bulla Granodiorite
Kemp, A.I.S., Hawkesworth, C.J., Paterson, B.A., Foster, G.L., Kinny, P.D., Whitehouse, M.J., Maas, R., EIMF, 2008. Exploring the plutonic-volcanic link: a zircon U-Pb, Lu-Hf and O isotope study of paired volcanic and granitic units from southeastern Australia. Transactions of the Royal Society of Edinburgh: Earth Sciences, 97(4), 337-355.

Norton Gully Sandstone
on Old Fumina Road, Neerim North
Morand, V.J., Fanning, C.M., 2006. SHRIMP zircon dating results for various rocks from Victoria, 2006. Geological Survey of Victoria Technical Record, 2006/2, 70p.

maximum deposition age for the protolith to the metamorphic rocks
Nine grains: 318-309 Ma from three rocks (W0500, W0501a and W0601a) are the best estimate of the maximum deposition age for the protolith to the metamorphic rocks. The youngest grain is 309 +/- 5 Ma.
Girrakool beds
Craven and Daczko 2017 paraphrased "Sample W0601a is a weakly metamorphosed sublitharenite (Folk, 1980) from an outcrop composed of a steeply dipping, weakly foliated sequence of metamorphosed feldspathic and lithic sandstones interbedded with mudstones. The sample is immature, moderately sorted and fine-grained. It consists of variably metamorphosed very angular, microcrystalline lithic volcanic grains (150-200 um), plagioclase, potassium feldspar, quartz, and minor calcite and opaque minerals (10-100 um) in a very fine-grained matrix that includes feldspars, biotite, muscovite, chlorite, zircon and ilmenite (Danis, Daczko, Lackie, & Craven, 2010)."
Craven, S. J., & Daczko, N. R. (2017). The Keepit arc: Provenance of sedimentary rocks in the central Tablelands Complex, southern New England Orogen, Australia, as recorded by detrital zircon. Australian Journal of Earth Sciences, 64(3), 401-418.

Abdullah et al 2020 paraphrased "Fine-grained metasandstone to metasiltstone. Sample 17-ST-01, from a unit informally known as the Brewarrina siltstone, is a fine-grained metasandstone to metasiltstone, poorly sorted, subrounded, undulose extinction, bulge recrystallisation. Is the host rock for the Brewarrina Granite. The dominant foliation is defined by aligned muscovite grains. Small quartz grains typically display undulose extinction, and larger grains exhibit polycrystalline grain boundary migration. The range of grainsizes is 50-200 um. Evidence of serrated edges indicates bulge recrystallisation."

University of Hiroshima
unknowns were calibrated using measurements of the Temora 2 reference material (U¿Pb ages concordant at 417 Ma); HQ9 range 535+/-34 2sigma, 499+/- 17 95% CL), 496+/- 32 2sigma, 495+/-19 95% cl, 495+/-34 2sigma; . Error is 2 standard deviations.
Pinnak Sandstone
Pinnak Sandstone / Howqua River sandstone
Fergusson, C.L., Nutman, A.P., Kamiichi, T., Hidaka, H., 2013. Evolution of a Cambrian active continental margin: The Delamerian-Lachlan connection in southeastern Australia from a zircon perspective. Gondwana Research, 24, 1051-1066.

The main population of zircon dates is in the range 650-500 Ma. This is the youngest population's mean age.
Williams Creek Conglomerate
Johnson et al 2016 paraphrased: "The sample was taken from the (basal) Williams Creek Conglomerate of the Kayrunnera Group. The conglomerate is poorly sorted and polymict, comprising of angular to sub-rounded pebbles of pelite, psammite and granitic material, along with poorly sorted, sub-angular to rounded granules of quartz. A strong foliation defined by an alignment of white mica is also present. The dominance of quartz and the minor fractions of feldspar in samples KB22a, KB21 and KB23 from the Kayrunnera Group indicate that the contributing sediments were probably derived from a cratonic source. Detrital zircon grains from sample KB22a are generally well rounded and exhibit oscillatory zoning."

Youngest detrital zircon population from a combination of four samples (053_SH_AK, 073_SH_NW, 031_SH_HA, 007_SH_BU) from Early Permian Nambucca block.
Shaanan et al 2015 paraphrased "The sample was extracted from a slate at Armidale Kempsy Road. Zircon crystals range from elongate euhedral to abraded and well-rounded morphologies. Their maximum length is 325 um, and the mean apparent elongated axis is 108 um. Under cathodoluminescence, most crystals exhibit well-defined oscillatory zoning, and some contain convolute zoning or absence of zoning

Bowry Formation
"Western Wall Banded Schist"
Cumming, G., Bottrill, R., Halpin, J.A., Mulder, J.A., Calver, C., Meffre, S., 2021. Geochronology of Meso-Neoproterozoic units near Savage River, Western Tasmania. Geological Survey of Tasmania. Technical Report, TR24, 35pp.

Keith Schist
Cumming, G., Bottrill, R., Halpin, J.A., Mulder, J.A., Calver, C., Meffre, S., 2021. Geochronology of Meso-Neoproterozoic units near Savage River, Western Tasmania. Geological Survey of Tasmania. Technical Report, TR24, 35pp.

Timbs Group
"Armstrong Creek Schist"
Cumming, G., Bottrill, R., Halpin, J.A., Mulder, J.A., Calver, C., Meffre, S., 2021. Geochronology of Meso-Neoproterozoic units near Savage River, Western Tasmania. Geological Survey of Tasmania. Technical Report, TR24, 35pp.

Keith Schist
banded quartzite and phyllite

This sample of Answer Slate was collected in the northern part of the Marimo–Staveley Domain about 4 km south of sample 2678686/ASMI0134 east of the road to Top Camp. The Marimo–Staveley Domain is a folded thrust-belt consisting of alternating slices of Answer Slate (dominantly carbonaceous cleaved mudstone) and Staveley Formation (typically calcareous sandstone and siltstone passing into calc-silicate granofels). Some slices of Roxmere Quartzite (mostly very thick bedded, amalgamated lithic sublabile sandstone) also occur. The outcrop sampled consists of medium to thick-bedded, fine-grained quartz sandstone, intercalated with grey slate or cleaved siltstone with planar laminae and local flaser bedding. Apart from the presence of sandstone, the outcrops were noted as being more typical of the Answer Slate. In thin section, the sample consists of a mosaic of interlocking quartz and subordinate feldspar, mostly 0.05–0.1 mm, but local grains are up to 1 mm. A foliation defined by anastomosing films of brown iron oxide and very fine-grained muscovite is evident.

Pinkish grey fine to very coarse; thick to very thickly bedded; quartz-feldspathic sandstone, micaceous in parts. Graded bedding observed in outcrop possible indicating the sequence is overturned. Dating Objective: Maximum age of deposition
Lewis, C.J., Withnall, I.W., Hutton, L.J., Bultitude, R.J., Slade, A.P., Sargent, S., 2020. Summary of results. Joint GSQ-GA geochronology project: Mount Isa region, 2016-2017. Queensland Geological Record, 2020/01, 71p.

Green-grey claystone. Anderson et al 2019: "The sample was collected over a depth interval of 85.27-85.37 m, from undivided Constance Sandstone as interpreted by Dorrins et al. (1983). The sample is 10 cm thick and was taken from a ~50 cm interval of green-grey claystone and siltstone, with very fine- to medium-grained sandstone lenses. Sandstone lenses within the sampled interval are dominated by rounded, well sorted quartz and lesser feldspar grains. The sampled core was targeted on the possibility that it might contain some tuffaceous input."

Boora Boora Bore
Nelson, DR 2000, 152956: metasandstone, Boora Boora Bore; Geochronology Record 251: Geological Survey of Western Australia, 5p.

para gneiss
Reid, A., Jagodzinski, E.A., 2017. Project PGC03-02: Geochronology of drillhole TB02, Toby and Frew Creek IOCG-U exploration project of Metallica Minerals Ltd. IN Jagodzinski, E.A. and Reid, A.J. (eds) PACE Geochronology: Results of collaborative geochronology projects 2013-15. Geological Survey of South Australia. Report Book, 2015/00003, 29-68.; Reid, A.J., Jagodzinski, E.A., Wade, C.E., Payne, J.L., Jourdan, F., 2017. Recognition of c. 1780 Ma magmatism and metamorphism in the buried northeastern Gawler Craton: Correlations with events of the Aileron Province. Precambrian Research, 302, 198-220.

This sample was collected from Dense Camp Creek, approximately 17 km north of the township of Silverton. The sample is a cordierite andalusite/sillimanite granofels overprinted by a biotite-sillimanite foliation. The sample comprises a granoblastic quartz + biotite rich matrix studded with abundant circular cordierite poikiloblasts up to 0.6 mm and lesser andalusite (chiastolite) poikiloblasts of a similar size. Bedding features are locally evident within the cordierite poikiloblasts, along with randomly oriented biotite. Coarse porphyroblasts/poikiloblasts are enveloped by intergrown S1 sillimanite (fibrolite) and red-brown biotite. Rutile is abundant, particularly in association with biotite at andalusite porphyroblast margins. Cordierite and sillimanite poikiloblasts are strongly sericitised and andalusite porphyroblasts are partially pseudomorphed by coarse-grained muscovite. Graphite and locally tourmaline are abundant throughout.
Kositcin, N., Fitzherbert, J.A., Main, P.T., Waltenberg, K., 2018. New SHRIMP U-Pb zircon provenance and in situ monazite metamorphic ages from the Mount Robe Sub-block, Broken Hill, New South Wales: July 2015-June 2017. Geoscience Australia. Record, 2018/50, 63p.

Napier Complex
pink gneiss
Enderby Land. Zircon Point, Field Islands
Harley, S.L., Black, L.P., 1997. A revised Archaean chronology for the Napier Complex, Enderby Land, from SHRIMP ion-microprobe studies. Antarctic Science, 9(1), 74-91.

Crimson Creek Formation
Mulder, J.A., Everard, J.L., Cumming, G., Meffre, S., Bottrill, R.S., Merdith, A.S., Halpin, J.A., McNeill, A.W., Cawood, P.A., 2020. Neoproterozoic opening of the Pacific Ocean recorded by multi-stage rifting in Tasmania, Australia. Earth Science Reviews, 201, 103041.

leucocratic gneiss

Date in Prot. Compilation of unknown origin. This reference uses unpublished data from D. Maidment
Stubbins Formation
Bagas, L., Bierlein, F.P., English, L., Anderson, J.A.C., Maidment, D.W., Huston, D.L., 2008. An example of a Palaeoproterozoic back-arc basin: petrology and geochemistry of the ca.1864Ma Stubbins Formation as an aid towards an improved understanding of the Granites-Tanami Orogen, Western Australia. Precambrian Research, 166(1-4), 168-184.

Youngest zircon is c. 512 Ma. This contrasts with known deposition age of the sediment being early Cretaceous.
Broome Sandstone
orange fSU and silty fSL, clay ripups, cut and fill, parallel bedding, ripples, thin crossbeds, minor vertical burrows; sample ~ 2 m above dinoturbation

Omar 1
Lech, M.E., Lewis, C.J., White, L.T., Abbott, S.T., 2018. Triassic provenance analysis of the Roebuck Basin, North West Shelf of Australia. ASEG/SEG Conference Papers, 2018(1), 6p.

Cowrie Siltstone

Doherty Formation
Sampled psammitic bed from calc-silicate package. Psammites are internally bedded on cm scale and possibly graded, and interbedded with calcareous beds upto ~10cm thick.

Mount McGrath Formation
MOUNT BRUCE_169082.1
Nelson, DR 2004, 169082: sandstone, Meteorite Bore; Geochronology Record 42: Geological Survey of Western Australia, 5p.

Success Creek Group
Mulder, J.A., Everard, J.L., Cumming, G., Meffre, S., Bottrill, R.S., Merdith, A.S., Halpin, J.A., McNeill, A.W., Cawood, P.A., 2020. Neoproterozoic opening of the Pacific Ocean recorded by multi-stage rifting in Tasmania, Australia. Earth Science Reviews, 201, 103041.

Sixty-six analyses were undertaken on 66 zircon grains. Two analyses with common 206Pb contents higher than an arbitrary value of 0.5% were considered unreliable, and were removed from further consideration. The remaining 64 analyses are characterised by a wide range of U contents (25-522 ppm), Th contents (15-822 ppm) and Th/U (0.26-1.91). The analyses record 207Pb/206Pb ages between ~2982 Ma and ~1692 Ma, with a large number of ages ranging between ~2750 and ~2600 Ma, and smaller age clusters at ~2000 Ma and ~1790 Ma. The youngest individual age (from 081.46.1.1) forms part of this youngest cluster, but the MSWD value of 1.7 and probability of fit (= 0.039) derived for the weighted mean age of this entire group (n = 17) indicates that it is not a single population. Excluding the oldest age provides a weighted mean 207Pb/206Pb age of 1790 +/- 12 Ma (95% confidence) for the remaining 16 analyses in this cluster (MSWD = 1.5; probability of fit = 0.10), which is used to define the maximum depositional age for this sample.The weighted mean 207Pb/206Pb age of 1790 +/- 12 Ma (95% confidence) obtained from the youngest 16 analyses is used to define the maximum age for deposition of this sandstone.
Kanpa 1A

The weighted mean 207Pb/206Pb date for this group is 889 +/- 107 Ma. MSWD=1.84. N=8
NELSON, D. R., 2002, 169117: metasandstone, Desert Queens Bath; in Compilation of geochronology data, 2001: Western Australia Geological Survey, Record 2002/2, p. 75-79.

Victory Springs Formation
fine-grained micaceous quartzwacke sandstone

Victory Springs Formation
"quartz schist"

SOUTHERN CROSS_205918.1

Wings Sandstone

Pedder River Siltstone

Bernafai Volcanics
fine-grained, lithic rich volcaniclastic sandstone is moderately sorted, consisting of wispy chlorite, rounded to angular grains of quartz and Fe-Ti magnetite crystals

Donaldson Formation

Alt. max deposit ages 207Pb/206Pb: 3476 +/- 6 Ma. MSWD = 1.22. N=18 and 3425 +/- 9 Ma. MSWD=0.23. N=9 are interpreted as detrital zircons
Salt Well Member
Nelson, DR 2005, 178019: coarse sandstone, Mount Grant; Geochronology Record 552: Geological Survey of Western Australia, 5p.

Site 1P
Sutherland, F.L., Hendry, D.F., Barron, B.J., Matthews, W.L., Hollis, J.D., 1996. An unusual Tasmanian Tertiary basalt sequence, near Boat Harbour, northwest Tasmania. Records of the Australian Museum, 48(2), 131-161.

Site 1C
Sutherland, F.L., Hendry, D.F., Barron, B.J., Matthews, W.L., Hollis, J.D., 1996. An unusual Tasmanian Tertiary basalt sequence, near Boat Harbour, northwest Tasmania. Records of the Australian Museum, 48(2), 131-161.

Deadmans Bay Formation
Stubley, T.C., 2010. Structure and stratigraphy of the Ironbound Group, southwest Tasmania, Australia. University of Tasmania, Hobart., BSc Hons thesis, 69pp.

unnamed sediment - Millungera Basin
collected by GSQ for SHRIMP U-Pb analysis

Dresser Formation
Wingate, MTD, Bodorkos, S and Van Kranendonk, MJ 2009, 180070: volcaniclastic sandstone, drillcore PDP2c, Dresser Mine; Geochronology Record 811: Geological Survey of Western Australia, 4p.

alt. deposit age for 207Pb/206Pb: 2714-846 Ma. N = 54. analyses have 207Pb*/206Pb* and 238U/206Pb* dates that define significant age components and are interpreted as the ages of zircon-bearing rocks in the detrital source region(s) of the quartz sandstone.
Gap Creek Formation
Wingate, MTD 2007, 184268: quartz sandstone, Gap Spring; Geochronology Record 657: Geological Survey of Western Australia, 5p.

Bird Phyllite
quartzite layer within Bird Phyllite
Arthur R ~300m above Hilders Bridge, left bank at mouth of small creek

Bird Phyllite

Keith Schist
quartz mica schist

Timbs Group
"Fulfords Creek Schist"

Goat Island Conglomerate
Oonah Formation / Goat Island
matrix to conglomerate

Panama Group
Northeast Tasmania Region
Knight, E., Orth, K., Meffre, S., 2022. Radiometric age dating of the Scamander Formation and underlying units of the Mathinna Supergroup, Scamander area, eastern Tasmania. Mineral Resources Tasmania, TR 28, 21pp.

Crimson Creek Formation
DDH SY016
MRT supplied data - McMann unpublished data

Colson No.1 was drilled by North Broken Hill Limited under a farm-in agreement with the tenement titleholder, Beach Petroleum N.L in 1978. Colson No.1 was located on a seismically defined anticlinal structure and the well reached a total depth of 2432.3 metres (Beach Petroleum, 1979). At present, Colson 1 sits within the interpreted margin of the western Warburton Basin (Edgoose and Munson, 2013). In Colson 1, 42 m of muscovite-chlorite phyllite or slate with an interpreted structural cleavage was intersected below the Permian Crown Point Formation of the Pedirka Basin (Beach Petroleum, 1979). Pre-Permian rocks at the base of the well are fine- to medium-grained well sorted quartz sandstones and phyllitic shales, and these were collected to place constraints on the depositional age of this part of the Warburton Basin.
Colson 1

Author very tentatively assigned interpreted rock to be meta-igneous however, age is older than any other igneous rock recorded in Tasmania.
Biotite quartz schist with large albite. Biotite, quartz, garnet, albite porphyroblasts, titanite, rutile.
Mulder, J.A., 2013, The structure and metamorphism of the Cox Bight - Red Point Area, South West Tasmania. University of Tasmania. Centre for Ore Deposit and Exploration Studies. B.Sc. Hons Thesis, 209pp.

laser ablation: Coherent 193nm COMPexPro 110 UV excimer laser ablation system
Melba Flats mafic sediments
Phua, M., 2015, Petrogenesis of the Melba Flats Ni-Cu-PGE Deposit in Western Tasmania: Insights from a Geochemical and Geochronological Investigation. Unpublished M.Sc. thesis. University of Melbourne, Melbourne.

Big Duffer Creek, via Savage River Mine

White mica, biotite, quartz, albite porphyroblasts, garnet.
Mulder, J.A., 2013, The structure and metamorphism of the Cox Bight - Red Point Area, South West Tasmania. University of Tasmania. Centre for Ore Deposit and Exploration Studies. B.Sc. Hons Thesis, 209pp.

Age of youngest population estimated from plot
Quartz + white mica rich layers and biotite + K-feldspar layers with minor tourmaline.
Mulder, J.A., 2013, The structure and metamorphism of the Cox Bight - Red Point Area, South West Tasmania. University of Tasmania. Centre for Ore Deposit and Exploration Studies. B.Sc. Hons Thesis, 209pp.

White mica, quartz, albite porphyroblasts.

Bowry Formation
"Western Wall Banded Schist"
Rocky R DDH3

Parmeener Supergroup
Whitfield, A., 2010, Sedimentology and detrital zircon geochronology of a coastally exposed Permian-Triassic section of the Tasmania Basin, Tasman Peninsula. BSc Honours thesis, University of Tasmania, 89pp.

conservative max dep age. Youngest grain 1032 Ma
"Western Wall Banded Schist"

Bernafai Volcanics
Mixed glass shard and lithic-rich volcaniclastic granule to pebble sandstone. Large sub-rounded clasts with needle pyroxene microlites occurs along with lenticular siltstone and lithic clasts. These clasts are generally supported in a silty, grey, crystal-rich matrix.

Cooee Dolerite
Cooee Dolerites
Mulder, J.A., Berry, R.F., Halpin, J.A., Meffre, S., Everard, J.L., 2018. Depositional age and correlation of the Oonah Formation: refining the timing of Neoproterozoic basin formation in Tasmania. Australian Journal of Earth Sciences, 65/3, 391-407.

Mereenie Sandstone
The Mereenie Sandstone is widespread within the Amadeus Basin and forms prominent outcrops within Watarrka National Park. Depositional environment ranges from shallow marine to fluvial to aeolian (Edgoose 2013). A palaeomagnetic investigation by Li et al (1991) suggested that the Mereenie Sandstone is probably largely Silurian in age. The youngest maximum depositional age produced from previous detrital zircon studies of the Mereenie Sandstone is 486 +/- 5 Ma (Normington et al 2018). This sample (LA19VJN130) is a poorly-sorted, medium-grained sandstone of the Mereenie Sandstone collected from a ridge 75 km west-southwest of Kings Canyon.

Cleland Sandstone
The Cleland Sandstone of the Pertaoorrta Group is typically a red to purple, thin- to medium-bedded, medium- to coarse-grained, feldspathic, micaceous sandstone with occasional pebble beds and lenses. No fossils have been observed in the Cleland Sandstone; its stratigraphic position suggests a middle to early, late Cambrian age (Edgoose 2013). One previous detrital zircon sample of the Cleland Sandstone produced a maximum depositional age of 490 +/- 7 Ma (Beyer et al 2020). Sample LA19JMS066 is a moderately sorted, fine-grained sandstone collected from a ridge ~11 km west of Mount Tucker.

Medium grained hornblende rich, thought to be volcaniclastic rock at time of submission. Determined to be sedimentary rock after analysis. Dating Objective: Maximum age of deposition.

volcaniclastic sedimentary rock
Nelson, DR 2001, 168924: volcaniclastic sedimentary rock, Whim Creek Hotel; Geochronology Record 203: Geological Survey of Western Australia, 4p.

Balbirini Dolostone
lower evaporitic unit
Sample BD19TJM131 was collected from thinly bedded, fine-grained redbeds about 5 m above the base of the evaporitic unit of the lower Balbirini Dolostone at the base of the type section. Outcrop at this locality consists of scattered, poorly exposed, moderately northeast-dipping low beds and abundant tabular rubble. The rocks comprise red-brown, laminated dolomitic siltstone that is interlaminated and thinly interbedded with lesser, grey-pink, lenticular, very fine-grained dolomitic quartz sandstone. The sample is a composite of a few square metres of float and exposed beds, selected for relatively high sandstone content. In thin section, the sandstone is dominated by sub-rounded to angular quartz grains with accessory zircon and very rare chert, muscovite, tourmaline and indeterminate very fine-grained rock fragments. These are set in a dolomite cement that has partially replaced an earlier Fe-oxide cement. Sandstone laminae are very low-angle cross-laminated, have erosive bases and contain small, tabular rip-up clasts of laminated dolomitic siltstone. Previous SHRIMP U-Pb zircon dating of three samples of tuffaceous rocks constrains the timing of deposition of the sampled interval (Page et al 2000). An age of 1614 ± 4 Ma has been interpreted for a sample from the underlying Amos Formation (GA sample ID 9577902); the sampled tuffaceous layer is an estimated 40-50 m stratigraphically below BD19TJM131. Ages of 1609 ± 3 Ma and 1613 ± 4 Ma have been interpreted for samples from overlying tuffaceous beds within the evaporitic unit (GA sample IDs 95779074 and 91779038 respectively); the sample sites are an estimated 75-95 m stratigraphically above BD19TJM131. These three previous isotopic ages overlap within uncertainty and are indistinguishable from one another; they collectively provide a robust absolute depositional age for sample BD19TJM131.
Kositcin, N., Munson, T.J., 2020. Summary of results. Joint NTGS-GA geochronology project: Balbirini Dolostone, southern McArthur Basin, June 2019-September 2019. Northern Territory Geological Survey Record, 2020-002, 14p.

Croydon Homestead
Nelson, DR 2000, 142943: metasandstone, Croydon Homestead; Geochronology Record 311: Geological Survey of Western Australia, 5p.

A total of 88 analyses were collected from 88 zircon crystals. One analysis had excessively low 206Pbc (< -1.00%). Another four analyses yield individual 207Pb/206Pb dates that are older than 1400 Ma, but are more than 10% discordant. Two analyses gave spurious results from isotopic mixing across internal domains resulting in heterogeneous Pb ratios. A further eleven analyses were acquired during instrument instability. These 18 analyses are interpreted as unreliable and are not considered further. The remaining 70 analysed zircons are characterised by low to high U contents (45-1295 ppm, median 182 ppm), a wide range of Th/U (0.02-2.75, median 0.59), and low 206Pbc (maximum 0.68%, median -0.01%). The 70 accepted analyses are divided into six groups (Table 3.2): Group 1 is a single analysis with an individual 238U/206Pb date of 514 +/- 15 Ma (2sigma); Group 2 consists of 31 analyses from 31 zircons with individual 238U/206Pb dates between c. 700 Ma and 515 Ma; Group 3 consists of nine analyses from nine zircons with individual 238U/206Pb dates between c. 1050 Ma and 730 Ma; Group 4 consists of 13 analyses from 13 zircons with individual 238U/206Pb dates between c. 1205 Ma and 1085 Ma; Group 5 consists of six analyses from six zircons with individual 207Pb/206Pb dates between c. 1805 Ma and 1490 Ma; and Group 6 consists of ten analyses from ten zircons with individual 207Pb/206Pb dates between c. 3390 Ma and 2100 Ma.The individual 238U/206Pb date of 514 +/- 15 Ma (2sigma) is interpreted as a maximum depositional age for the 300 m interval of the Eneabba Formation. This age is considerably older than the biostratigraphically (C. torosa Zone) determined Early Jurassic age of this unit.

Browns Range Metamorphics
Lu, Y, Wingate, MTD, Morin-Ka, S and Beardsmore, TJ 2017, 213028: quartz-muscovite schist, GD5 Bore; Geochronology Record 1399: Geological Survey of Western Australia, 5p.

42 grains analysed, 24 <10% discordant and low common Pb. Younger group at 1621?14 (n=10, MSWD=0.25) - interp as partial Pb loss but no chemical or morphological difference between populations, NO CL.
Giles, D., Nutman, A.P., 2002. SHRIMP U-Pb monazite dating of 1600 - 1580 Ma amphibolite facies metamorphism in the southeastern Mt Isa Block, Australia. Australian Journal of Earth Sciences, 49 (3), 455-465.

Mount Start Member
Grey-pink, medium-fine grained hummocky sandstone