Stratno | Stratigraphic Name | Category | Contents | Last update 
24151|Algamba Dolomite Member|Name source|Algamba Bore (5453-793382), Reynolds Range 1:100 000 Sheet area.|16-MAY-23
24151|Algamba Dolomite Member|Unit history|Distinctive mappable unit; referred to as Lander Dolomite by Australian Geophysical (1967); mapped as 'Precambrian schist, metasediments, including marble' by Wells & others (1971).|16-MAY-23
24151|Algamba Dolomite Member|Type section locality|AX-3, 5.5 km southwest of Lander Bore: base of section at 5453-673411, top at -671407. Not measured.|16-MAY-23
24151|Algamba Dolomite Member|Extent|Entire length of Reynolds Range.|16-MAY-23
24151|Algamba Dolomite Member|Thickness range|425 m in type section is maximum.|16-MAY-23
24151|Algamba Dolomite Member|Lithology|Grey-brown laminated to thin-bedded fine-grained dolomite, and minor grey irregularly laminated fine-grained limestone.|16-MAY-23
24151|Algamba Dolomite Member|Relationships and boundaries|Conformable lens enclosed in Pine Hill Formation (q.v.): folding and faulting have formed several subsidiary lenses.|16-MAY-23
24151|Algamba Dolomite Member|Age reasons|Middle Proterozoic or older|16-MAY-23
24151|Algamba Dolomite Member|Proposed publication|2. Commentary on Geology of the Reynolds Range Region (BMR)|16-MAY-23
367|Amesbury Quartzite Member|Name source|The name is derived from Amesbury Bore (yard grid reference 653900E 2282800N) in the southeastern part of the Mount Peake 1:250 000 Sheet area. The Amesbury Quartzite Member crops out 7 km northeast of Amesbury Bore, and continues in scattered exposure for 29 km farther northwards.|16-MAY-23
367|Amesbury Quartzite Member|Type section locality|There is no measured section. The type section is situated 16 km east-northeast of Amesbury Bore, at yard grid reference 670800E, 2288200N. The sequence at the type locality begins with .5 m of poorly sorted conglomerate consisting of subrounded pebbles of white quartz, claystone, and shale, in a quartz sandstone matrix. This is overlain by about 20 m of coarse-grained colourless orthoquartzite, feldspathic in the lower part but clean above, medium-bedded, moderately rounded, blocky. There is no other rock-type above the quartzite. The unconformity between the basal conglomerate underlying weathered granite is very well exposed.|16-MAY-23
367|Amesbury Quartzite Member|Extent|The Amesbury Quartzite Member crops out intermittently for about 30 km northwards from the Djilbari Hills in the eastern part of the Mount Peake 1:250 000 Sheet area.|16-MAY-23
367|Amesbury Quartzite Member|Thickness range|The thickness at the type section is estimated at 20 m; away from there the thickness is rather less than this.|16-MAY-23
367|Amesbury Quartzite Member|Lithology|The Amesbury Quartzite  Member consists of crossbedded coarse-grained orthoquartzite, commonly with a pebble or granule conglomerate at the base. The phenoclasts in the conglomerate are composed of white quartz and pelitic rocks.|16-MAY-23
367|Amesbury Quartzite Member|Relationships and boundaries|The Amesbury Quartzite Member unconformably overlies granite of the Arunta Block, and the contact is well exposed at the type locality. The Member is conformably overlain by reddish-purple feldspathic quartz sandstone typical of the Central Stuart Beds. The upper contact of the quartzite is generally concealed, but a good exposure is present 4 km north-northwest of Boko Bore, at yard grid reference 670400E, 230 3400N in the eastern part of the Mount Peake 1:250 000 Sheet area. Here, the Amesbury Quartzite Member is conformably overlain by laminated siltstone and fine micaceous sandstone, followed by feldspathic quartz sandstone with clay galls. This is succeeded by a covered interval, and then by purple-brown to white feldspathic quartz sandstone, medium to coarse-grained. If it is valid to relate the Amesbury Quartzite Member to the type section of the Central Mount Stuart Beds, then upper and lower stratigraphic limits of the Quartzite can be interpolated into the type section on the following grounds: (1) There are no calcareous beds in or above the Amesbury Quartzite Member, therefore it must lie above the uppermost level of calcareous rocks in the type section of the Central Mount Stuart Beds, i.e., 183 m.  (2) The Amesbury Quartzite Member is overlain by laminated siltstone at the locality 4 km north-northwest of Boko Bore, therefore it must lie below the uppermost level of pelite in the type section of the Central Mount Stuart Beds i.e., 395 m. If these limits are accepted, the Amesbury Quartzite Member lies stratigraphically well above the basal tillite of the Central Mount Stuart Beds, by at least 179 m. |16-MAY-23
367|Amesbury Quartzite Member|Age reasons|The age of the Amesbury Quartzite Member can be determined no more accurately than that of the Central Mount Stuart Beds; it may be Adelaidean, or Cambrian, or it may straddle the Precambrian-Cambrian boundary.|16-MAY-23
367|Amesbury Quartzite Member|Comments|Reason for proposed name: The unit has a distinctive lithology, and is sufficiently extensive for it to be mapped as a separate member in the central Mount Stuart Formation.|16-MAY-23
24160|Ankala gneiss|Name source|Ankala Hill (GR 5751-081276), (pronounced "Angkarla"), Laughlen 1:100 000 Sheet area.|16-MAY-23
24160|Ankala gneiss|Unit history|Previously mapped by Wells and others (1968) as undivided Arunta Complex.|16-MAY-23
24160|Ankala gneiss|Type section locality|Reference area: Area surrounding Ankala Hill and between there and Gumtree Bore (i.e. between GR 5751-085284 and 5751-042264).|16-MAY-23
24160|Ankala gneiss|Extent|The unit forms a fault wedge widening eastwards from its apex near Gumtree Bore (GR 5751-42264) to the Pinnacles Fault (GR5751-195308), where it is offset to the south. The unit reappears farther southeast in the Winnecke Goldfield area, and also crops out south of a schist zone (Psr) southeast of the reference area.  It is also considered to occur in the hanging wall sequence at Rankin's Copper Prospect (GR 5751-093242).|16-MAY-23
24160|Ankala gneiss|Lithology|Quartzofeldspathic gneiss, subordinate calcsilicate gneiss, biotite gneiss, amphibolite and rare marble, meta-ultramafic rock, and quartz-hematite rocks, and extremely rare anthophyllite-rich rock.|16-MAY-23
24160|Ankala gneiss|Relationships and boundaries|The unit is faulted against Erontonga metamorphics, Utnalaname granulite, and Harry Anorthositic Gabbro, and also against Sliding Rock metamorphics except at Rankin's Prospect (5751-093343), where the two units appear to be conformable.|16-MAY-23
24160|Ankala gneiss|Age reasons|Middle Proterozoic or older. The first of several metamorphisms recognised in this unit is correlated with the earliest event identified in the Harry Creek area, which is dated at 1800 m.y. using 40Ar-39Ar incremental heating methods (Allen & Stubbs, in press).|16-MAY-23
24160|Ankala gneiss|Comments|The Ankala gneiss is distinguished from the Utnalanama granulite by its more biotite-rich and calcareous rocks, its lower metamorphic grade and the more acid composition and layered nature of its felsic rocks. The Ankala gneiss lacks the hornblende and garnet-bearing gneisses typical of the Sliding Rock metamorphics.|16-MAY-23
24160|Ankala gneiss|Proposer|Shaw R.D., Allen A.R. (in Shaw et al., in preparation)|16-MAY-23
27062|Anuma schist|Name source|Anuma Creek (GR5751-370220), in southeast of Laughlen 1:100 000 Sheet area, flows past eastern end of outcrop area of Schist.|16-MAY-23
27062|Anuma schist|Type section locality|Series of low but well exposed ridges extending from GR 5751-271254 for 600 m north to 5751-271260 in Laughlen 1:100 000 Sheet area.|16-MAY-23
27062|Anuma schist|Extent|Elongate body extending for 14 km east from Marbles Bore (GR 5751-264267) to Anuma Creek, in Laughlen.|16-MAY-23
27062|Anuma schist|Lithology|Sequence in type section begins in south with kyanite-muscovite schist containing segregations of coarse kyanite and biotite. Overlain to north by staurolite-muscovite schist, muscovite-biotite-quartz-feldspar gneiss, staurolite-biotite-muscovite schist, epidote-microcline rock, hematite-garnet quartzite, muscovite-biotite-quartz-feldspar gneiss, mica schist containing masses of pegmatite up to 7 m across, staurolite-biotite-muscovite schist, and interbedded marble and garnet-hematite quartzite at top (truncated by fault).|16-MAY-23
27062|Anuma schist|Relationships and boundaries|Concordantly overlies Erontonga Metamorphics (name to be submitted by R.D. Shaw) to south, may be conformable on them. Faulted against overlying Cadney metamorphics (to be submitted by R.D. Shaw) to north.|16-MAY-23
27062|Anuma schist|Age reasons|K-Ar dates of 993, 674, 371, 336 reflect partial argon loss during Alice Springs Orogeny (E. Carboniferous). Progressive regional metamorphism probably about 1700 m.y. on evidence from surrounding areas, but no Rb-Sr date determined. Time of deposition of parent sediments considered Early Proterozoic.|16-MAY-23
27062|Anuma schist|Comments|Reason for proposed name: Very distinctive body of coarse kyanite and staurolite schist cropping out between units lacking these minerals.|16-MAY-23
24191|Bond Springs gneiss|Name source|Bond Springs homestead, GR 5650-897960 Alice Springs 1:100 000 Sheet area.|16-MAY-23
24191|Bond Springs gneiss|Type section locality|North of homestead along tributary of Todd River: GR 5650-897964 to 897973. Leucocratic gneiss and muscovite schist.|16-MAY-23
24191|Bond Springs gneiss|Extent|Occur in an arc (about 9 km strike length by about 2 km width) in the northeast of the Alice Springs 1:100 000 Sheet area near Bond Springs homestead.|16-MAY-23
24191|Bond Springs gneiss|Lithology|Leucocratic medium-grained quartzfeldspathic and garnet-muscovite gneiss and lesser amounts of banded biotite gneiss, amphibolite and muscovite schist; southern part of gneiss is partly migmatitic.|16-MAY-23
24191|Bond Springs gneiss|Relationships and boundaries|Structurally overlain to the west and underlain to the east by unnamed gneiss; contacts are concordant with the foliation.|16-MAY-23
24191|Bond Springs gneiss|Identifying features|Reason for proposed name: Distinctive unit of leucocratic gneiss; surrounding rocks are composed of darker-coloured gneiss.|16-MAY-23
24191|Bond Springs gneiss|Age reasons|No direct evidence. Recrystallisation and metamorphic fabric of the unit may have occurred during the regional Chewings Phase of deformation which in Hermannsburg 1:100 000 Sheet area to the west has been dated by total-rock Rb-Sr at 1620+/-70 m.y.|16-MAY-23
24191|Bond Springs gneiss|Proposed publication|Geological report on 1:100 000 scale mapping of southeastern Arunta Block, Alice Springs 1:250 000 Sheet area, Northern Territory by R.D. Shaw et al. BMR.  Microfiche report in prep.|16-MAY-23
24193|Bonya metamorphic complex|Name source|Bonya Creek 22o53'S, 136o24'E, Huckitta 1:250 000 Sheet area.|16-MAY-23
24193|Bonya metamorphic complex|Type section locality|Reference area: Section from Charlottes Bore to Bonya Bore (22o45' 136o02' to 22o47' 136o09').|16-MAY-23
24193|Bonya metamorphic complex|Extent|Forms the hills drained by Bonya Creek, outcrops surrounding Jervois Mine.|16-MAY-23
24193|Bonya metamorphic complex|Thickness range|Unknown|16-MAY-23
24193|Bonya metamorphic complex|Lithology|Layered sequence of felsic gneiss, amphibolites, 2 mica schists and calc-silicate rocks. (Assumed that layering representing primary bedding but not proven).|16-MAY-23
24193|Bonya metamorphic complex|Relationships and boundaries|Intruded by Jinka Granite. Unconformably overlain by Myponga Gp (Late Proterozoic-Cambrian).|16-MAY-23
24193|Bonya metamorphic complex|Age reasons|In excess of 1803 m.y. (Probable age of Jinka Granite) (Wilson et al. 1960).|16-MAY-23
24193|Bonya metamorphic complex|Comments|Replaces "Bonya sequence" (Wararen, 1978).|16-MAY-23
2761|Buchanan Hills Beds|Name source|Buchanan Hills, latitude 18o53'S, longitude 131o05'E, Winnecke Creek Sheet area, SE52-12.|16-MAY-23
2761|Buchanan Hills Beds|Unit history|Milligan et al. (1966), included the Beds in the Merrina Beds.|16-MAY-23
2761|Buchanan Hills Beds|Type section locality|Reference section: At Buchanan Hills, latitude 18o51'36", longitude 131o05'36", in prominent scarp. Sandstone, very fine to coarse grained, angular, poorly sorted, ferruginous and siliceous cement is approximately 40 metres thick, and overlies siltstones of the Hooker Creek Formation with a sharp contact. Top of the unit is eroded, and the ferruginous zone of the laterite soil profile is developed in the upper part.|16-MAY-23
2761|Buchanan Hills Beds|Extent|The unit is exposed discontinuously, commonly as a capping on rises, throughout the Winnecke Creek, South Lake Woods, Tanami East, Green Swamp Well Sheet areas, and in the northern parts of the Mount Solitaire and Lander River Sheet areas. Its extent to the north of the Winnecke Creek and South Lake Woods Sheet areas is uncertain.|16-MAY-23
2761|Buchanan Hills Beds|Thickness range|Approximately 40 metres at reference section; maximum thickness observed elsewhere is 4 metres, although the base of the unit is rarely exposed.|16-MAY-23
2761|Buchanan Hills Beds|Lithology|Sandstone, typically poorly sorted, very fine to coarse grained, grades to sandy siltstone at some localities, contains pebbles and cobbles at some localities, typically angular, although also contains well rounded grains at some localities, mostly poorly exposed on rises, commonly weathered due to lateritization.|16-MAY-23
2761|Buchanan Hills Beds|Depositional environment|Poor sorting and rounding suggests a continental depositional environment.|16-MAY-23
2761|Buchanan Hills Beds|Relationships and boundaries|Overlies the Proterozoic Winnecke Granophyre of The Granites-Tanami Block, the Proterozoic Tomkinson Creek Group of the Tennant Creek Block, the Middle Cambrian Hooker Creek Formation and Lothari Hill Sandstone, the partly Middle Cambrian Point Wakefield Beds, the Ordovician Hanson River Beds, indicating an unconformable basal contact. Top of unit eroded. Unconformably overlain by Cainozoic rock units.|16-MAY-23
2761|Buchanan Hills Beds|Age reasons|Unfossiliferous. Overlies Hanson River Beds, indicating post Ordovician (Llanvirnian) age. The laterite soil profile developed on the Buchanan Hills Beds, indicating deposition earlier than the range late Early Cretaceous to early Miocene, the age of the laterite soil profile (Huleatt, in prep.). Similar sediments in other parts of Australia are of Cretaceous or Tertiary age, and this is considered the most likely age for the Buchanan Hills Beds. The possibility that the Buchanan Hills Beads are a lateral equivalent of part of the Hanson River Beds cannot be dismissed.|16-MAY-23
2761|Buchanan Hills Beds|Comments|The discontinuous nature of outcrops, and continental origin of the Beds makes the lateral equivalence of mapped outcrops uncertain; complete sections are rare; hence the designation "Beds" is proposed.|16-MAY-23
24201|Buckshee Breccia|Name source|Derived from Buckshee phosphate prospect; GR 163626, Bynoe 1:100 000 Sheet (5072).|16-MAY-23
24201|Buckshee Breccia|Unit history|Malone (1962) included these lithologies in the Depot Creek Sandstone Member. Informally referred to as the 'Nematitic quartzite breccia' or HQB by Walpole et al. (1968) and Johnson (1974).|16-MAY-23
24201|Buckshee Breccia|Type section locality|At Buckshee Prospect where a low rise of probably flat lying hematitic quartzite breccia of indeterminant depth crops out, grid co-ordinates 163626, Bynoe 1:100 000 Sheet (5072).|16-MAY-23
24201|Buckshee Breccia|Extent|The unit is exposed as generally small isolated outcrops near the margin of the Waterhouse Complex and near the south-east margin of the Rum Jungle Complex in the Bynoe, Batchelor and Reynolds Rivers 1:100 000 Sheet areas.|16-MAY-23
24201|Buckshee Breccia|Thickness range|Range 5 to 180 metres.|16-MAY-23
24201|Buckshee Breccia|Lithology|Quartzite breccia in lilac-red ferruginous quartzitic matrix, rare shale breccia; sericite, chlorite and quartz veined.|16-MAY-23
24201|Buckshee Breccia|Relationships and boundaries|Unconformably ;overlies Early Proterozoic sediments and is conformably overlain by Depot Creek Sandstone Member (Malone, 1962). Of relatively uniform lithology from base to top and clearly distinctive from overlying and underlying sediments. Considered to be a fossil regolith (Johnson, 1974).|16-MAY-23
24201|Buckshee Breccia|Age reasons|Overlies Early Proterozoic sediments of the Pine Creek Geosyncline and is overlain by :Middle Proterozoic Depot Creek Sandstone Member. Of indeterminate age but probably Middle Proterozoic.|16-MAY-23
24201|Buckshee Breccia|Proposed publication|BMR Report|16-MAY-23
27730|Cadney metamorphics|Name source|Cadney Creek, at 23o14'S, 134o44'E, Alice Springs 1:250 000 Sheet area.|16-MAY-23
27730|Cadney metamorphics|Type section locality|Reference area: The reference section is in the central part of the Riddoch 1:100 000 Sheet area and extends along the north of the main branch of Tug Creek from Eritjapunta Pass to the junction of Tug and Cadney Creeks and then from Mueller Bore (to the south) northeastwards to the track to Bungitina Well from Muller Flat Dam. The additional refereance section in Laughlen 1:100 000 Sheet area extends from GR 5751-113321 to -151361 then GR 5751-06325 to -74445.|16-MAY-23
27730|Cadney metamorphics|Extent|The Cadney metamorphics crop out extensively in the Riddoch and Laughlen 1:100 000 Sheet areas, principally in the headwaters of the Tug, Cadney, and Mueller Creeks in the Riddock 1:100 000 Sheet area and as a sinous belt extending across the central and southern Strangways Range in Laughlen 1:100 000 Sheet area.|16-MAY-23
27730|Cadney metamorphics|Lithology|Mainly calc-silicate rock, biotite gneiss, and sillimanite gneiss. The lower part of the unit also contains thick layers of quartzofeldspathic gneiss and felsic granulite. The unit also contains small amounts of marble, quartzite, and mafic granulite.|16-MAY-23
27730|Cadney metamorphics|Relationships and boundaries|The Cadney metamorphics consistently overlie (structurally) a number of units of mafic and felsic rocks assigned to the lower part of the Strangways Metamorphic Complex, and are thought to be younger than these felsic and mafic rocks, because it is extremely unlikely that overturning has occurred on a regional scale. These underlying units are the Yambah granulite, unnamed unit pCsp, the Ongeva granulite, and unnamed units pCu and pCx. The Cadney metamorphics have a sharp contact with these units, and their lithological differences suggest a regional discordance. The Erontonga metamorphics, which also underlie the Cadney metamorphics differ from the other underlying units in consisting largely of metasediments and in having a transitional contact with the Cadney metamorphics. In the White Range Nappe the Cadney metamorphics interfinger with the Hillsoak Bore metamorphics. Unit pCsl (in northern Riddoch 1:100 000 Sheet area) is considered to be a facies equivalent of the Cadney metamorphics (pCsl consists mainly of schistose biotite gneiss and layered amphibolite as well as small amounts of calc-silicate rock, marble and sillimanite gneiss identical to that in the Cadney metamorphics). Unit pCsl is overlain by the Irindina Gneiss of the Harts Range Group. The boundary between pCsl and the Harts Range Group is sharp and discordant; where a major angular break is evident between pCsl and the Harts Range Group there is evidence of a zone of structural disturbance. The Cadney metamorphics are distinguished from neighbouring units by their content of calc-silicate rock and sillimanite-bearing gneiss.|16-MAY-23
27730|Cadney metamorphics|Identifying features|Explanation of name variation:  Joklik named the unit Cadney Gneiss after Cadney Creek, but did not nominate a reference section. His type specimen, described as a meta-tuff, is part of the Cavenagh metamorphics and differs from any rock type present in the Cadney Creek area. Cadney Creek is unsuitable as a type area because it runs parallel to strike and only a part of the unit is present in this area. Although the unit is characterised by calc-silicate rock and marble it includes large amounts of pelitic gneisses and some quartzofeldspathic gneisses, so the term 'metamorphics' is preferred to 'Gneiss'. The stratigraphic name is regarded as informal beacause the unit may subsequently be amenable to formal subdivision.|16-MAY-23
27730|Cadney metamorphics|Age reasons|Middle Proterozoic or older. The unit is the uppermost member of the Strangways Metamorphic Complex, which underwent regional metamorphism at about 1800 m.y. (Black 1975; Iyer, Woodford & Wilson, 1976).|16-MAY-23
27730|Cadney metamorphics|References|R216; RC79/047; + As for Adla Granulite|16-MAY-23
24216|Cavenagh metamorphics|Name source|Cavenagh Range GR5851-630070 of Heavitree Quartzite which adjoins western margin of Cavenagh metamorphics, Riddoch 1:100 000 Sheet area.|16-MAY-23
24216|Cavenagh metamorphics|Type section locality|Reference area: 1) Western sub-unit: 3 km section from GR 5851-654015 to GR 5851-680032; moderately well exposed terrain through complete sequence of sub-unit.  2) Eastern sub-unit: 1.3 km section from GR 5851-703058 to GR 5851-695066 then 1.8 km to GR 5851-705081; well exposed hilly area through complete sequence of sub-unit.|16-MAY-23
24216|Cavenagh metamorphics|Extent|Southwestern part of Riddoch  and northwestern edge of Fergusson Range 1:100 000 Sheet areas, NT, in White Range Nappe of Arltunga Nappe Complex.|16-MAY-23
24216|Cavenagh metamorphics|Lithology|Two sub-units separated by a fault: 1) Western sub-unit: sequence (from west to east) of quartzofeldspathic gneiss, para-amphibolite, chlorite schist, andalusite schist, quartzite, biotite gneiss; 2) Eastern sub-unit: sequence (from north to south) of mica-quartz gneiss and marble, feldspathic schist, quartzite, granitic gneiss, amphibolite, quartz-rich metasediment.|16-MAY-23
24216|Cavenagh metamorphics|Relationships and boundaries|Almost wholly concealed by younger unconformably overlying Heavitree Quartzite and Quaternary cover. Parallel foliations in Cavenagh metamorphics and Hillsoak Bore metamorphics (q.v.) to west suggest conformable relationship, but contact concealed by alluvium. Atnarpa Igneous Complex to north contains rafts of amphibolite and quartz-rich metasediment of Cavenagh metamorphics.|16-MAY-23
24216|Cavenagh metamorphics|Identifying features|Reason for Proposed Name: Distinctive association of metamorphic rocks very different in mineralogical composition from adjoining rocks (quartzite and acid igneous rock).|16-MAY-23
24216|Cavenagh metamorphics|Age reasons|Time of metamorphism of parent rocks given by one sample of amphibolite, which lies on isochron at 1719 +/- 24 m.y. together with other samples from Cadney metamorphics (definition to be submitted by R.D. Shaw) and Atnarpa Igneous Complex (q.v.). Amphibolite is not sufficiently enriched in 87Rb and daughter 87Sr for estimate of maximum age of parent rocks to be meaningful.|16-MAY-23
24216|Cavenagh metamorphics|Proposed publication|1. 'Geological report on 1:100 000 scale mapping at southeastern Arunta Block, Alice Springs 1:250 000 Sheet area, Northern Territory', by R D. Shaw et al. BMR Microfiche Reprt, in prep.|16-MAY-23
24217|Cement Dam gneiss|Name source|Cement Dam, at 23o24'S, 134o11'E in the Alice Springs 1:250 000 Sheet area.|16-MAY-23
24217|Cement Dam gneiss|Unit history|Previously mapped as undivided Arunta Complex by Wells & others (1968).|16-MAY-23
24217|Cement Dam gneiss|Type section locality|Reference area: The type section is between GR 5751-183107 and 5751-175116 along the track between Randall's Peak and Porter's Well.|16-MAY-23
24217|Cement Dam gneiss|Extent|Over a strike length of 7 km in a valley 1.5 km south of Cement Dam.|16-MAY-23
24217|Cement Dam gneiss|Lithology|Schistose biotite gneiss containing conspicuous megacrysts of potassium feldspar. More details on lithology are given in Shaw & others (in preparation).|16-MAY-23
24217|Cement Dam gneiss|Relationships and boundaries|The southern boundary is faulted against the Randall Peak metamorphics. The northeastern boundary is a fault-branch of the same fault zone. The northern and southwestern boundaries appear to be conformable with a unit of unassigned amphibolite and subordinate biotite gneiss (pC). The unit is distinguished by its schistose nature and the conspicuous potassium feldspar megacrysts, which are absent from neighbouring units.|16-MAY-23
24217|Cement Dam gneiss|Age reasons|Middle Proterozoic or older. Precambrian. No isotopic dates available.|16-MAY-23
24218|Charles River gneiss|Name source|Charles River, a tributary of the Todd River in the Alice Springs 1:100 000 Sheet area.|16-MAY-23
24218|Charles River gneiss|Type section locality|About 10 km north of Alice Springs on the west side of the Stuart Highway; GR 5650-846882. Consists of banded garnet biotite gneiss, quartzofeldspathic gneiss and amphibolite.|16-MAY-23
24218|Charles River gneiss|Extent|Crops out about 9 km north of Alice Springs, extends to 30 km along strike into Undoolya 1:100 000 Sheet area to the east and is up to 4 km in width.|16-MAY-23
24218|Charles River gneiss|Lithology|Garnet-biotite gneiss, biotite gneiss, amphibolite, migmatite and a small amount of quartzofeldspathic gneiss.|16-MAY-23
24218|Charles River gneiss|Relationships and boundaries|To the west the Charles River gneiss is interlayered with the Old Hamilton Downs Gneiss (new name) and conformably in contact with unnamed gneiss. The unit is faulted on other sides. Dolerite of the Stuart Dyke Swarm (new name) intrudes the gneiss.|16-MAY-23
24218|Charles River gneiss|Identifying features|Reason for proposed name:  The unit is composed of garnet-bearing gneiss; neighbouring units contain only a small amount of garnet-bearing gneiss.|16-MAY-23
24218|Charles River gneiss|Age reasons|No direct evidence. Recrystallisation and metamorphic fabric of the unit may have occurred during the regional Chewings Phase of deformation which in Hermannsburg 1:100 000 Sheet area to the west has been dated by total-rock Rb-Sr at 1620 +/- 70 m.y. The dolerite dykes which intrude the gneiss have been dated as Upper Proterozoic.|16-MAY-23
24218|Charles River gneiss|Proposed publication|Geological report on 1:100 000 scale mapping of southeastern Arunta Block, Alice Springs 1:250 000 Sheet area, Northern Territory by R.D. Shaw et al.  BMR Microfiche Report in prep.|16-MAY-23
3988|Chilling Creek Formation|Name source|Chilling Creek in the Daly River and Wingate Mountains 1:100 000 Sheet area.|16-MAY-23
3988|Chilling Creek Formation|Type section locality|The replacement type section lies between 130o25'06"E, 14o12'09"S and 130o26'03"E, 14o14'15"S exposing 2500 m of the sequence from the clean, basal quartzite through less mature sandstones above the interlayered Berinka Volcanics. The new type section does not expose the entire sequence because the southern part of the Giant's Reef Fault truncates the upper part of the section, but the sequence continues, with some repeat, due south of the termination of the above replacement section until it passes under Cretaceous sediments. Because of faulting a complete, uninterrupted section can not be nominated but this section is well exposed, extensive, and representative of the bulk of the unit. The Berinka Volcanics do not separate the Chilling Creek Formation by forming continuous horizons but forms single or multiple flow lenses within the sequence. A reference section between 130o38'52"E, 14o04'18"S and 130o39'E, 14o04'38"S is also submitted which typifies sporadically developed, trough cross-bedded silts and ripple marked mud and fine sand occurring developing at the base of the sequence in some areas.|16-MAY-23
3988|Chilling Creek Formation|Identifying features|Revision of old terms; Modified from the old name 'Chilling Sandstone'. The name and the replacement type section have been proposed to accommodate the establishment of a new stratigraphic group (Wingate Group) due to the division of the Finniss River Group at a previously unrecognised unconformity by Hammond and others (in prep. A revision of the Finniss River Group, BMR Journal). The reference section, representing some 500 m, also includes lithologies not before recognised as part of the sequence. The total thickness of the sequence is estimated at 4500 to 5000 m. The old type section contains only moderately well sorted, compositionally mature, medium sandstones and does not represent parts of the sequence that are contaminated by volcanogenic material and form a large part of the exposed sequence. The old type section is also situated across a syncline which repeats only the basal 1000 to 1500 m of the sequence.|16-MAY-23
3988|Chilling Creek Formation|Age reasons|The sequence unconformably overlies the Litchfield complex which is believed to be late lower Proterozoic in age (I.e. 1800 ma).  Hammond, Nisbet, and Etheridge (A revision of the Finniss River Group, BMR Journal) regard the Chilling Creek Formation as older than the Tolmer Group which is Carpentarian to Adelaidean in age. The Chilling Creek Formation is probably Carpentarian (middle Proterozoic).|16-MAY-23
3988|Chilling Creek Formation|Proposed publication|BMR Journal|16-MAY-23
4021|Chiripee Gneiss|Name source|After Chiripee Dam (GR 426E, 7504N AMG metric) on western side of outcrop area. Chiripee Dam is in the southeast corner of Woodgreen Station in the central part of the Alcoota 1:250 000 Sheet area, SF 53-10, Australian map Grid.|16-MAY-23
4021|Chiripee Gneiss|Unit history|Previous informal names: Arno Gneiss; discontinued as Arno used. Reserved for Arno Gravel on Wyalla 1:250 000 Sheet area.|16-MAY-23
4021|Chiripee Gneiss|Type section locality|From near Arno Peak at 436500E, 7504500N (AMG) south to Alcoota boundary fence (GR 437E, 75035N AMG metric). Subunits pCr1, pCr2, pCr3 not at type locality.|16-MAY-23
4021|Chiripee Gneiss|Extent|Outcrop area extends 25 km south from Arno Peak to Plew Bore (GR 4226E, 7485N).|16-MAY-23
4021|Chiripee Gneiss|Lithology|Migmatitic garnet-biotite-feldspar gneiss; minor amphibolite (pCr1) and calc-silicate rock (pCr2 - 5 km northwest of 720 bore; muscovite-biotite gneiss. Resembles Langford Orthogneiss but lacks feldspar porphyroblasts. pCr2 - small outcrops area 5 km northwest of Lignum Dam - calc-silicate rock, quartzite, biotite gneiss. pCr3 - small area northwest of 720 bore - amphibolite (units pCr2 and pCr3 on Preliminary map only).|16-MAY-23
4021|Chiripee Gneiss|Relationships and boundaries|Possibly overlies the Mount Bleechmore Granulite as it is of lower metamorphic grade (i.e. lacks sillimanite, cordierite and hypersthene typical of Mt Bleechmore Granulite. Unconformably overlain by Tertiary sediments. Faulted against other metamorphic units.|16-MAY-23
4021|Chiripee Gneiss|Identifying features|Similar to Mount Bleechmore Granulite, but (except for rare localities) lacks mafic rocks. Similar to Mapata Gneiss, but contains garnet unlike the Mapata Gneiss.|16-MAY-23
4021|Chiripee Gneiss|Correlations|Tentative correlations: Correlated with parts of the Mapata Gneiss.|16-MAY-23
4021|Chiripee Gneiss|Proposed publication|BMR Report|16-MAY-23
75723|Collah Suite|Name source| After Collah Waterhole, GDA 94 52L 706200mE 8410100mN (14°22'25"S 130°54'44"E) and Collah Tinfield, GDA 94 Zone 52 703900mE 8410830mN (14°22'2"S 130°53'27" E) FERGUSSON RIVER, WINGATE MOUNTAINS, Litchfield Province, Pine Creek Orogen, Northern Territory|16-MAY-23
75723|Collah Suite|Unit history|Previously known as the Wangi Basics. The first use of the name Wangi Basics was by Needham and Stuart-Smith (1984) when it was published on the Geology of the Pine Creek Geosyncline, Northern Territory, 1:500 000 scale map. The first formal definition was by Dundas et al 1987. The name Wangi Basics is now abandoned as it is now known to comprise distinct geochemical groups which are genetically unrelated.|16-MAY-23
75723|Collah Suite|Geomorphic expression|Boulder-strewn hummocky rises|16-MAY-23
75723|Collah Suite|Type section locality|Large exposure in FERGUSSON RIVER  and central WINGATE MOUNTAINS ca 60 km south of Daly River township. GDA94 Zone 52 693500mE 8417500mN (14°18'28"S 130°47'38"E).|16-MAY-23
75723|Collah Suite|Description at type locality|Exposed in boulder-strewn hummocky rises (Edgoose et al 1989)|16-MAY-23
75723|Collah Suite|Extent|Mafic rocks in this area are exposed over an area of ca 8 km2. First vertical derivative magnetic image does not indicate greater subsurface extent.|16-MAY-23
75723|Collah Suite|General description|Slightly altered, lower-amphibolite-facies probable lamprophyre, includes minor shoshonitic cumulate. Rocks are characteristically low-SiO2 with no free quartz.|16-MAY-23
75723|Collah Suite|Lithology|Possible altered lamprophyre. Mineralogy dominated by sericitised plagioclase (labrodorite, andesine) and hornblende, and minor biotite and opaques (Edgoose et al 1989).|16-MAY-23
75723|Collah Suite|Depositional environment|Genesis: Intrusive|16-MAY-23
75723|Collah Suite|Relationships and boundaries|Intrudes the surrounding Burrell Creek Formation and intruded by Soldiers Creek Granite as inferred by Edgoose et al (1989).|16-MAY-23
75723|Collah Suite|Identifying features|Collah Suite consists of fine-grained, altered low-grade metamorphic rocks with distinctive strong alkaline geochemical signatures. Age of ca 1830 Ma distinguishes these rocks from other former Wangi Basics lithologies, which must be in the range 1860-1855 Ma, based on Stratigraphic relationships.|16-MAY-23
75723|Collah Suite|Structure and Metamorphism|Lower amphibolite-facies metamorphism. Structural relationships unknown.|16-MAY-23
75723|Collah Suite|Age reasons|Worden et al (2008) reported a 207Pb/206Pb SHRIMP zircon age of 1829 +/-4 Ma.|16-MAY-23
75723|Collah Suite|Correlations|Temporal correlative of olivine-mica-K-feldspar lamprophyre dykes at Mount Bundey, Central Domain, Pine Creek Orogen, Northern Territory (Sheppard and Taylor 1992).|16-MAY-23
75723|Collah Suite|Alteration and Mineralisation| Sericitic alteration of plagioclase feldspar. Some alteration of hornblende to actinolite and tremolite. Partial chloritisation of biotite. No known mineralisation.|16-MAY-23
75723|Collah Suite|Geophysical Expression|Has a positive magnetic response|16-MAY-23
75723|Collah Suite|Geochemistry|Mafic rocks with distinctive potassic signatures, silica values are typically low, <50 wt%,  alumina is high, ca 20 wt% Al2O3|16-MAY-23
75723|Collah Suite|Defn author|Glass, L.M.  03-NOV-2010|16-MAY-23
75723|Collah Suite|Comments|Rocks from this locality, described by Edgoose et al (1989) as "quartz-bearing diorite, gabbro and some dolerite" are not included in this unit. Although Collah Suite is defined by only a small number of historical samples, collected in 2004 from a region with restricted access, the distinctive geochemistry and younger age of these rocks distinguish them from other former Wangi Basics lithologies (Glass 2010).|16-MAY-23
75723|Collah Suite|References|**DUNDAS DL, Edgoose CJ, Fahey GM and Fahey JE, 1987. Daly River 1:100 000 Geological Map Series. Northern Territory Geological Survey Explanatory Notes (5070).    **EDGOOSE CJ, Fahey GM and Fahey JE, 1989. Wingate Mountains 1:100 000 Geological Map Series. Northern Territory Geological Survey Explanatory Notes (5069).    **GLASS LM, 2010. Palaeoproterozoic island-arc-related rocks of the Litchfield Province, western Pine Creek Orogen, Northern Territory. Northern Territory Geological Survey, Record 2010-005.    **NEEDHAM RS, Stuart-Smith PG, 1984. Geology of the Pine Creek Geosyncline, Northern Territory, 1:500 000 scale map. Bureau of Mineral Resources, Australia, Canberra.    **SHEPPARD S and Taylor WR, 1992. Barium- and LREE-rich olivine-mica-lamprophyres with affinities to lamproites, Mt. Bundey, Northern Territory, Australia: in Foley S and Peccerillo A (editors) 'Potassic and ultrapotassic magmas and their origin; Sixth meeting of the European Union of Geosciences (EUG VI)'. Lithos 28, (3-6), 303-325.    **WORDEN KE, Carson CJ, Close DF, Donnellan N and Scrimgeour IR, 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 2008-3.|16-MAY-23
4988|Cullen Granite Complex|Name source|Cullen River, a tributary of the Ferguson river. Pine Creek and Ferguson River 1:100 000 Sheet areas.|16-MAY-23
4988|Cullen Granite Complex|Unit history|Previously called the Cullen Granite by Noakes (1949).|16-MAY-23
4988|Cullen Granite Complex|Type section locality|An area of about 100 km2 southeast of Cullen Siding bordered by Copperfield Creek in the west and Driffield Creek in the south (Ferguson and Katherine 1:100 000 Sheet areas).|16-MAY-23
4988|Cullen Granite Complex|Extent|Crops out extensively over about 2800 km2 centred on Pine Creek (GR 060704, Pine Creek).|16-MAY-23
4988|Cullen Granite Complex|Lithology|At least thirteen varieties of granitic rock, including coarse pink and green porphyritic granite, coarse grey porphyritic granite, coarse pink leucogranite, fine leucogranite, medium granodiorite, fine pink and green granite, fine pink granite, coarse pink porphyritic leucogranite, coarse porphyritic quartz-leucogranite, coarse porphyritic grey granodiorite. Also included are blocks and rafts of metasediments up to several km across.|16-MAY-23
4988|Cullen Granite Complex|Relationships and boundaries|Individual granite phases comprise several plutons which have coalesced to form the present Batholith. Intrudes Early Proterozoic metasediments of the Pine Creek Geosyncline (1800 m.y.) and the El Sherana Group. Unconformably overlain by the Edith River Group.|16-MAY-23
4988|Cullen Granite Complex|Age reasons|Early Proterozoic 1780-1730 m.y. (Page & others, 1980, and Riley, 1980).|16-MAY-23
4988|Cullen Granite Complex|Proposed publication|Geological  map commentary McKinlay 1:100 000 Sheet|16-MAY-23
5258|Darwin Member|Name source|City of Darwin, Darwin 1:250 000 topographic Sheet. The name is synonymous with the Darwin Formation which formed part of the Mullaman Group of Noakes (1949).|16-MAY-23
5258|Darwin Member|Type section locality|The cliffs at Myilly Point, Darwin. 12o28'S, 130o49'E.|16-MAY-23
5258|Darwin Member|Extent|This distinctive unit has been recognised in all wells penetrating the base of the Cretaceous in the Bonaparte Gulf-Timor Sea area. (Pontalier, Australian Aquitane, pers. comm.). The Darwin Member extends beneath Bathurst and Melville Islands and was intersected in Tinganoo Bay 1. It outcrops across the NW part of Northern Territory and extends as far east as BMR East Alligator 9.|16-MAY-23
5258|Darwin Member|Thickness range|Range 20-50 m.|16-MAY-23
5258|Darwin Member|Lithology|At its type section a basal conglomerate of quartz fragments unconformably overlies steeply dipping Proterozoic rocks. Above this is up to 8 m of fine sandstone, which in turn is covered by up to 11 m of claystones and radiolarian shales (Skwarko, 1966). The Darwin Member is always fine-grained, except for a basal conglomerate, and is typically rich in Radiolaria.|16-MAY-23
5258|Darwin Member|Relationships and boundaries|The Darwin Member is a basal member of the Bathurst Island Formation and it disconformably overlies a friable, fine to medium quartzose sandstone with interbedded shales (the Petrel Formation, Hughes in prep.). In the Cobourg Peninsula sheet area it is replaced as the basal member of the Bathurst Island Formation by the Marligur Member; both are laterally equivalent, the change reflecting a facies change. The Darwin Member is overlain by the Wangarlu Mudstone Member of the Bathurst Island Formation.|16-MAY-23
5258|Darwin Member|Age reasons|Palynological examination by Burger (pers. comm.) of cores from the Darwin Member indicate that it ranges in age from Late Neocomian? to Aptian. Other fossils present include Radiolaria, Foraminifera, belemnites, echinoids, brachiopods, bryozoans, corals and molluscs.|16-MAY-23
5258|Darwin Member|Proposed publication|Bureau of Mineral Resources Australia Report|16-MAY-23
24249|Donkey Creek Beds|Name source|Donkey Creek, Barrow Creek 1:250 000 Sheet area.|16-MAY-23
24249|Donkey Creek Beds|Unit history|The Grant Bluff Formation and part of the Central Stuart Beads of the Barrow Creek 1:250 000 Geological Series Sheet. Identification as Grant Bluff Formation was a mapping mistake.|16-MAY-23
24249|Donkey Creek Beds|Type section locality|25 km SE of Neutral Junction Homestead (Barrow Creek 1:250 000 Sheet area).|16-MAY-23
24249|Donkey Creek Beds|Extent|Barrow Creek and Alcoota 1:250 000 Sheet areas.|16-MAY-23
24249|Donkey Creek Beds|Thickness range|In the type section only the upper 60 m has been measured accurately. The total thickness is estimated to be 180 m. Near Mt Octy 46 m of sequence is assigned to the Donkey Creek Beds.|16-MAY-23
24249|Donkey Creek Beds|Lithology|Brown and green-grey arkose, sandstone and siltstone with abundant trace fossils.|16-MAY-23
24249|Donkey Creek Beds|Relationships and boundaries|The upper boundary is unknown. In the type section the unit abuts sheared quartzite; the nature of this contact is unknown. Near Mt Octy the unit lies with structural conformity on the Central Mount Stuart Formation (Walter, 1979). Regional correlations indicate that this is a paraconformity.|16-MAY-23
24249|Donkey Creek Beds|Age reasons|Following Daily ;(1972) the fossil assemblage is taken to indicate an Early Cambrian (Tommotian) age.|16-MAY-23
24249|Donkey Creek Beds|Defn Reference|R214 as Donkey Creek beds|16-MAY-23
26523|Dorothy Basalt Member|Name source|Dorothy Creek, 24 km NE of Katherine NT on Katherine 1:250 000 Sheet area.|16-MAY-23
26523|Dorothy Basalt Member|Unit history|Dorothy Volcanics in part (Walpole & others, 1968; Randal, 1963).|16-MAY-23
26523|Dorothy Basalt Member|Type section locality|GR Katherine KE 298030; longitude 132o29'40"E, latitude 14o25'50"S. Basalt and mafic pyroclastics in gully banks.|16-MAY-23
26523|Dorothy Basalt Member|Extent|About 7 km2 near and east of the Maud Creek Mining Area, Katherine 1:100 000 and Eva Valley 1:100 000 Sheet areas.|16-MAY-23
26523|Dorothy Basalt Member|Thickness range|About 200 m in south. Possibly thicker in north (including type area).|16-MAY-23
26523|Dorothy Basalt Member|Lithology|Fine dark grey massive basalt and tuff, minor banded chert and pitchstone.|16-MAY-23
26523|Dorothy Basalt Member|Relationships and boundaries|Interbedded with Tollis Formation of El Sherana Group, with sharp conformable contacts against sediments; intruded by Maud Dolerite.|16-MAY-23
26523|Dorothy Basalt Member|Identifying features|Reason for name change and redefinition. The "Dorothy Volcanics" include areas now mapped as Maud Dolerite. Their relationship with other units has been determined so as to invalidate their inclusion in the Finniss River Group.|16-MAY-23
26523|Dorothy Basalt Member|Structure and Metamorphism|Not evident owing to massive and homogeneous nature of unit. Presumably folded about tight northerly axes well expressed in Tollis Formation sediments.|16-MAY-23
26523|Dorothy Basalt Member|Age reasons|Late Early Proterozoic; about 1860 Ma as implied from U-Pb zircon determinations from porphyry also interbedded with the Tollis Formation 40 km to NW near Edith Falls (Needham, Stuart-Smith & Page, in prep).|16-MAY-23
26523|Dorothy Basalt Member|Proposed publication|BMR 1:100 000 Geological Map Commentary - Geology of the Yeuralba Region.|16-MAY-23
24267|Emily Gap schist|Name source|Emily Gap, topographic feature 23o45'S, 133o57'E Alice Springs 1:250 000.|16-MAY-23
24267|Emily Gap schist|Type section locality|5 km east of Alice Springs township. GR 5650-905800.|16-MAY-23
24267|Emily Gap schist|Extent|Low to moderately high rubbly hills and ridges in two outcrop areas - about 6 km east and 5 km southeast of the Alice Springs township.|16-MAY-23
24267|Emily Gap schist|Lithology|Northeastern outcrop: biotite-feldspar-quartz schist with some layers of recrystallised micaceous-quartz sandstone and rare amphibolite. Southern-most schist zone: two-mica schist biotite schist, quartzose sericite-schist and recrystallised sericitic quartz sandstone and rare amphibolite.|16-MAY-23
24267|Emily Gap schist|Relationships and boundaries|Both outcrops are possibly intruded by the Sadadeen Range gneiss (new name) and are cut by dolerite (Stuart Dyke Swarm) and pegmatite dykes. The Heavitree Quartzite unconformably overlies the southern most exposure of the unit.|16-MAY-23
24267|Emily Gap schist|Identifying features|Reason for proposed name: Distinctive schist units within orthogneiss.|16-MAY-23
24267|Emily Gap schist|Age reasons|Assuming the schistocity formed during the Chewings Phase of deformation and metamorphism the unit is Middle Proterozoic or older. The dolerite dykes which intrude, and the Heavitree Quartzite which overlies the unit are both Upper Proterozoic in age.|16-MAY-23
24267|Emily Gap schist|Proposed publication|Geol. Report on 1:100 000 scale mapping of southeastern Arunta Block, Alice Springs 1:250 000 Sheet area, NT by R.D. Shaw et al. BMR Microfiche report in prep.|16-MAY-23
24267|Emily Gap schist|Defn Reference|80/20787|16-MAY-23
24267|Emily Gap schist|Reserved? Yes/No|Yes|16-MAY-23
24270|Erontonga metamorphics|Name source|Erontonga Waterholes at GR 5751-322242, Laughlen 1:100 000 Sheet area.|16-MAY-23
24270|Erontonga metamorphics|Unit history|Previously mapped by Wells & others (1968) as undivided Arunta Complex.|16-MAY-23
24270|Erontonga metamorphics|Type section locality|From GR 5751-072304 west of Johannsens Phlogopite Mine to GR 5751-089329 of the boundary with the adjoining Cadney metamorphics. The section is folded but the amount of folding is uncertain.|16-MAY-23
24270|Erontonga metamorphics|Extent|The unit crops out in three regions: 1. The main outcrop area surrounds Johannsen's Phlogopite Mine and exteands eastwards from here to Pinnacles Bore in the Laughlen 1:100 000 Sheet area.  2. In an arcuate belt in the central-northern part of Burt 1:100 000 Sheet area.  3. In the Winnecke Depot Creek region in the centre of Laughlen 1:100 0000 Sheet area.|16-MAY-23
24270|Erontonga metamorphics|Lithology|Mainly quartzofeldspathic and cordierite-bearing pelitic rocks (containing quartz + cordierite +/- orthopyroxene +/- garnet +/- plagioclase +/- sillimanite) and small amounts of calc-silicate, magnesian, and manganiferous rocks (together 5%).|16-MAY-23
24270|Erontonga metamorphics|Relationships and boundaries|The unit overlies the Utnalanama granulite and the Harry Anorthositic Gabbro, which it appears to truncate possibly because this lower boundary is an unconformity. The unit is conformably overlain by the Cadney metamorphics. The unit was intruded by the Johannsens Metagabbro, before the regional metamorphism, and was subsequently intruded by the Gumtree Granite.|16-MAY-23
24270|Erontonga metamorphics|Age reasons|Middle Proterozoic or older 40Ar-39Ar apparent age spectra of a hornblende from the mafic gneisses, and of a magnesian pargasite from a magnesian rock in the Erontonga metamorphics have been interpreted to indicate two metamorphic events at 1800 m.y. and 1700 m.y. (Allen & Stubbs, in press). The unit is at least 1800 m.y. old.|16-MAY-23
24270|Erontonga metamorphics|Proposed publication|Stewart & others, in prep.|16-MAY-23
24270|Erontonga metamorphics|Comments|Remarks: The unit differs from the adjoining units in containing abundant cordierite-bearing gneiss.|16-MAY-23
24270|Erontonga metamorphics|Defn Reference|80/20787|16-MAY-23
24270|Erontonga metamorphics|Proposer|Shaw R.D., Allen A.R. (in shaw & others, in preparation).|16-MAY-23
24271|Errarra Formation|Name source|Aboriginal name for Marshall Well, on Marshall River at approx. latitude 23o40'S, longitude 135o50'E.|16-MAY-23
24271|Errarra Formation|Unit history|Originally included as part of the Mount Baldwin Formation by Smith (Bureau of Mineral Resources Report 67, 1964). Alluded to by M.R. Walter (Bureau of Mineral Resources Report 214, 1980) who excluded it from a redefined Mount Baldwin Formation and left it as an un-named unit. Correlated with the Red Heart Dolomite on Tobermory and Hay River sheets and with the Todd River Dolomite of the eastern Amadeus Basin.|16-MAY-23
24271|Errarra Formation|Type section locality|Holostratotype: In cored hole DDH. NTGS. HUC 1, between 310.73 m and 372.52 m. To be stored in the NT Geological Survey, Alice Springs core store. Hole is at latitude 22o31'50"S, longitude 136o15'4"E.|16-MAY-23
24271|Errarra Formation|Extent|Huckitta 1:250 000 Sheet area, from the Jervois Range in the east to the Mopunga Range in the west.|16-MAY-23
24271|Errarra Formation|Thickness range|61.79 m in holostratotype.|16-MAY-23
24271|Errarra Formation|Lithology|In holostratotype from top it is comprised of brown silty, quartz-arenite over grey-green silty quartz sandstone over Archaeocyatha-bearing dolostone, grading down through silty shale to sandstone into a basal granule conglomerate. In outcrop, only the lower sandstone and siltstone crop out near the Jervois Range. Elsewhere, only the dolostone crops out. Drilling indicates that only the dolostone facies occurs away from the Jervois Range.|16-MAY-23
24271|Errarra Formation|Relationships and boundaries|Apparently conformably overlain by Arthur Creek Formation calcareous, grey siltstone. In the Jervois Range it disconformably overlies the Mount Baldwin Formation (Elb); commencing with a granule conglomerate and grading up into sandstone then into dolostone. In the Elua Range the contact is marked by the change from Clb red-brown siltstone into laminated silty dolostone. In the Mopunga Range, this same silty dolostone rests disconformably on yellow-brown, stromatolitic dolostone of the Elkera Formation.|16-MAY-23
24271|Errarra Formation|Age reasons|Lower Cambrian, abundant Archaeocyatha, described by Kruse and West (BMR Journal of Australian Geology and Geophysics, 5, 1980, 165-181).|16-MAY-23
35329|Fawcett Member|Name source|From Mount Fawcett, one of the higher points in the western Parsons Range, at lat. 13o26'14", long. 135o9'9"E, FLEMING 1:100 000 sheet (5971).|16-MAY-23
35329|Fawcett Member|Unit history|The Fawcett Member was not distinguished during previous mapping of the Parsons Range Group by Plumb & Roberts (1992).|16-MAY-23
35329|Fawcett Member|Geomorphic expression|Forms a narrow valley between resistant sandstone ridges.|16-MAY-23
35329|Fawcett Member|Type section locality|The base is at lat. 13o15'51"S, long. 135o31'44"E; the top is at lat. 13o16'0"S, long. 135o31'48"E.|16-MAY-23
35329|Fawcett Member|Extent|Outcrops all lie within the Parsons Range, paralleling the southern bank of Matta Murta Creek in the eastern Parsons Range, in an arcuate belt extending 45 km west, southwest then south, to a point about 7 km southeast of Mount Fawcett.|16-MAY-23
35329|Fawcett Member|Thickness range|Maximum of 265 m in central Parsons Range, and 250 m in type section, thinning to 0 m about 7 km southeast of Mount Fawcett.|16-MAY-23
35329|Fawcett Member|Lithology|Laminated to thin-bedded olive to grey mudstone and siltstone, coarse- to very coarse-grained glauconitic sandstone, minor stromatolitic dolostone, generally silicified to chert.|16-MAY-23
35329|Fawcett Member|Depositional environment|Shallow marine, probably intertidal and shallow subtidal.|16-MAY-23
35329|Fawcett Member|Relationships and boundaries|A member of the Badalngarrmirri Formation, Parsons Range Group.  Both lower and upper contacts are sharp. The lower contact may be unconformable, at least locally, eg, 23 km west of the type section, where stromatolitic chert encrusts lithified sandstone at the top of the Mattamurta Sandstone. The upper contact is probably conformable, and is placed at the change from recessive siltstone/mudstone to boldly outcropping medium-grained quartz arenite.|16-MAY-23
35329|Fawcett Member|Age reasons|Palaeoproterozoic: As for its parent formation, the maximum age for the Fawcett Member is well constrained by the age of the uppermost formation of the Donydji Group, the Fagan Volcanics, at 1710 Ma; minimum age is less well constrained, but must be greater than 1620 Ma, the age of the Yarrawirrie Formation in the overlying Balma Group (Haines and others, 1994), and most likely older than 1640 Ma, the age of the Barney Creek Formation (Page & Sweet, in press), a correlative of the central Balma Group (Haines, 1994).|16-MAY-23
35329|Fawcett Member|Correlations|No known correlatives.|16-MAY-23
35329|Fawcett Member|References|HAINES, P.W., 1994 - The Balma and Habgood Groups, Northern McArthur Basin, Northern Territory: stratigraphy and correlations with the McArthur Group. In HALLENSTEIN, C.P. (Editor), 1994 - AusIMM Annual Conference: 'Australian Mining looks north - the challenges and choices'. Australasian Institute of Mining and Metallurgy, Melbourne, 135-138. **HAINES, P.W., RAWLINGS, D.J., SWEET, I.P., PIETSCH, B.A., PLUMB, K.A., MADIGAN, T.L., & KRASSAY, A.A., 1997 - Blue Mud Bay, 1:250 000 geological series. Northern Territory Geological Survey, Explanatory Notes, SD53 7. **PAGE, R.W., & SWEET, I.P., (in press) - Geochronology of basin phases in the western Mount Isa Inlier, and correlation with McArthur Basin. Australian Journal of Earth Sciences. **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, N.T. In HALLENSTEIN, C.P. (Editor), 1994 - AusIMM Annual Conference: 'Australian Mining looks north - the challenges and choices'. Australasian Institute of Mining and Metallurgy, Melbourne, 135-138. **PLUMB, K.A., & ROBERTS, H.G., 1992 - The geology of Arnhem Land, Northern Territory. Bureau of Mineral Resources, Australia, Record, 1992/55, 193pp.|16-MAY-23
6636|Field River Beds|Identifying features|The name Field River Beds of Smith (1963) is here superseded by the following formations and groups: Yackah Beds, Yardida Tillite; Black Stump Arkose and Wonnadinna Dolomite (Keepera Group); Gnallan-a-gea Arkose (Mopunga Group).|16-MAY-23
6636|Field River Beds|Status|1|16-MAY-23
24277|Flint Spring gneiss|Name source|Flint Spring GR 5650-783902, Alice Springs 1:100 000 Sheet area.|16-MAY-23
24277|Flint Spring gneiss|Type section locality|Along tributary of Colyer Creek from GR 5650-833913 to 820916.|16-MAY-23
24277|Flint Spring gneiss|Extent|About 7 km x 1 km area north-northwest of Alice Springs township in the Alice Springs 1:100 000 Sheet area.|16-MAY-23
24277|Flint Spring gneiss|Lithology|Largely composed of porphyroblastic and augen feldspar gneiss; lesser amount of quartzofeldspathic gneiss, banded biotite gneiss and amphibolite.|16-MAY-23
24277|Flint Spring gneiss|Relationships and boundaries|Eastern and western contacts with unnamed gneiss are both gradational and conformable with the foliation.|16-MAY-23
24277|Flint Spring gneiss|Identifying features|Reason for proposed name: Distinctive unit of large-feldspar gneiss; surrounding units contain only a small amount of this rock type.|16-MAY-23
24277|Flint Spring gneiss|Age reasons|No direct evidence. Recrystallisation and metamorphic fabric of the unit may have occurred during the regional Chewings Phase of deformation which in Hermannsburg 1:100 000 Sheet area to the west has been dated by total rock Rb-Sr at 1620 +/- 70 m.y.|16-MAY-23
24277|Flint Spring gneiss|Proposed publication|Geological Report on 1:100 000 scale mapping of southeastern Arunta Block, Alice Springs 1:250 000 Sheet area, Northern Territory by R D Shaw et al. BMR Microfiche report in prep.|16-MAY-23
24277|Flint Spring gneiss|Defn Reference|80/20787|16-MAY-23
24277|Flint Spring gneiss|Proposer|Offe L.A.|16-MAY-23
24277|Flint Spring gneiss|Resdate|03-NOV-1975|16-MAY-23
24277|Flint Spring gneiss|Reserved? Yes/No|Yes|16-MAY-23
24279|Forster Member|Name source|Forster Range on Barrow 1:100 0000 sheet (AMG GR LS8010).|16-MAY-23
24279|Forster Member|Unit history|'Basal quartzose unit' (PuCs1) of Shaw et al. (1979), p.47, and Shaw and Warren (1975).|16-MAY-23
24279|Forster Member|Geomorphic expression|Forms a resistant mesa capping over Arunta Block rocks when horizontal. Forms cuestas where there is an apreciable dip.|16-MAY-23
24279|Forster Member|Type section locality|Base of section at head of creek 500 m east of Barrow Creek Telegraph Station (AMG GR LS856186; latitude 21o31'50"S, longitude 133o53'40"E) on Barrow 1:100 000 sheet. Base unconformably overlies early Proterozoic Granite. Section extends 300 m to southeast from this point to a gradational contact with the overlying Tops Member.|16-MAY-23
24279|Forster Member|Thickness range|18 m at type section. 32 m measured at AMG GR MR029959 on Home of Bullion 1:100 000 sheet. Shaw et al. (1979) reports 6-30 m in the southern part of its range.|16-MAY-23
24279|Forster Member|Lithology|Medium-coarse grained, white and purple, feldspathic quartz arenite. Local interbeds of friable red-brown sandstone, arkose and siltstone. Cross-bedded and ripple marked. Basal polymict conglomerate up to 4 m thick usually present.|16-MAY-23
24279|Forster Member|Relationships and boundaries|Unconformably overlies early Proterozoic crystalline basement (most commonly granite). Conformably overlain with gradational contact by Tops Member. Top of Forster Member picked at top of highest hard sandstone below friable arkose and siltstone of Tops Member.|16-MAY-23
24279|Forster Member|Structure and Metamorphism|Generally horizontal or gently dipping to the southwest. May dip steeply along faults.|16-MAY-23
24279|Forster Member|Age reasons|Late Proterozoic as it is conformably overlain by the Tops Member containing an element of the late Proterozoic (late Adelaidean) Ediacara assemblage.|16-MAY-23
24279|Forster Member|Correlations|May correlate with the lower Andagera Formation to the northwest.|16-MAY-23
24279|Forster Member|Proposed publication|Barrow Creek 1:250 000 Geol. Series, Explan. Notes, NT Geol. Surv.|16-MAY-23
24279|Forster Member|Category|2|16-MAY-23
24279|Forster Member|Proposer|Haines P.W.|16-MAY-23
7083|Gecko Volcanics|Name source|Gecko Mine, in Tennant Creek 1:250 000 Sheet area, GR 402850.|16-MAY-23
7083|Gecko Volcanics|Type section locality|The southwestern limb of the Mount Argo antiform GR 407845 is nominated as the type section locality. What is believed to be the lower part of the unit consists of well-jointed, blocky, purple to grey, vesicular quartz-feldspar porphyritic lava and tuff. The uppermost part consists of sheared quartz-feldspar and feldspar porphyry interbedded with shale.|16-MAY-23
7083|Gecko Volcanics|Extent|A series of small lenses with a total area less than 3 km2, within an unnamed shale-siltstone unit. The lenses stretch in a rough line from 3 km west to 9 km southeast of the Gecko Mine, alongside the track from Quartz Hill to the Marion Ross and Orlando Mines. At Mount Argo (GR 406846) the volcanics form two distinct beds which are folded into a northwest plunging antiform.|16-MAY-23
7083|Gecko Volcanics|Thickness range|The maximum thickness is 300 m.|16-MAY-23
7083|Gecko Volcanics|Lithology|Grey-green and purple tuff, quartz and feldspar porphyry and greywacke mostly derived from volcanic rock.|16-MAY-23
7083|Gecko Volcanics|Relationships and boundaries|Conformable with the underlying and overlying shale of the unnamed Pw2 unit.|16-MAY-23
7083|Gecko Volcanics|Age reasons|According to Black (1977) the Warramunga Group, of which the Gecko Volcanics is a constituent formation, is Early Proterozoic in age. It was intruded by granite as old as 1797 m.y.; the major deformation of the Group took place 1810 m.y. ago.|16-MAY-23
7083|Gecko Volcanics|Proposed publication|See list of references under Mendum and Tonkin; Dodson and Gardener|16-MAY-23
7083|Gecko Volcanics|Name first published by|Stewart A.J., Langworthy A.P., Warren R.G., Offe L.A., Glikson A.Y., Wells A.T., LeMessurier P., Gardener J.E.F., 1976.|16-MAY-23
8055|Hanson River Beds|Name source|Hanson River; a prominent river flowing from south of Ti Tree Well, NT, to the area north of Numagalong Homestead, NT, where, at latitude 20o25'S, it is about 7 km east of the reference area of the Beds.|16-MAY-23
8055|Hanson River Beds|Unit history|Probably included in Chewings' (1931) Winnecke Creek Tableland Formation.|16-MAY-23
8055|Hanson River Beds|Type section locality|Reference area: Low outcrops 7 km west of the Hanson River at latitude 20o25'S, longitude 133o17'E, in which fine to medium grained, well to poorly sorted, angular to rounded, fossiliferous sandstone with silica overgrowths on the grains is interbedded with medium crystalline, yellow, red-brown and black, very thinly bedded fossiliferous dolomite and rare sandy siltstone.|16-MAY-23
8055|Hanson River Beds|Extent|Very poor exposure makes extent uncertain. Underlies a northwest trending area of about 10,000 sq km in the southwest Bonney Well SF 53-2, north Lander River SF 53-1, south and southwest Green Swamp Well SE 53-13, southeast Tanami East SE 52-16 and northeast Mount Solitaire SF 52-4 1:250 000 Sheet areas.|16-MAY-23
8055|Hanson River Beds|Thickness range|The full thickness of the Beds cannot be measured because Quaternary sand obscures detail in much of the outcrop area. A seismic survey across the Lander Trough by Amoseas (1967) indicates that the Beds are part of a sequence at least 300 m thick beneath the reference area, and thickening to at least 800 m in the Lander Trough.|16-MAY-23
8055|Hanson River Beds|Lithology|Sandstone, fine to coarse grained, generally poorly sorted and angular, but well sorted and rounded in parts, very silicified in parts; siltstone, generally light green where fresh but weathers brown, sandy or clayey in parts, micaceous, fissile, minor glauconite in parts; dolomite, medium crystalline, white, light brown, yellow, red-brown, or black; dolomite, finely crystalline, white, chalcedonic in parts; coarse grained dolarenite.|16-MAY-23
8055|Hanson River Beds|Relationships and boundaries|The base of the Hanson River Beds is not exposed, but may be concealed by scree at Point Wakefield, latitude 19o59'S, longitude 133o21'E where they may overlie the Point Wakefield Beds. It may have been penetrated in BMR Barrow Creek 18 (GRG18) stratigraphic drillhole (Milligan, 1963), latitude 21o9'S, longitude 145o12'E, where it may also overlie the Point Wakefield Beds. The nature of the contact is not known. The Lake Surprise Sandstone overlies the Hanson River Beds. It directly overlies dolomites of both middle Arenig and late Arenig or early Llanvirnian age and the upper 10 m of the Hanson River Beds are red-brown in BMR Lander River 1, latitude 20o31'S, longitude 133o30'E, suggesting weathering below the contact.|16-MAY-23
8055|Hanson River Beds|Age reasons|Two Ordovician conodont faunas; one of middle Arenigian age, the other of late Arenigian or early Llanvirnian age (E. Druce, BMR, pers. Comm., 1976) have been recorded in the Beds. Macrofossils from latitude 20o16'S, longitude 132o47'E are of the late Arenigian or early Llanvirnian age (J. Gilbert Tomlinson, BMR, pers. comm., 1976). These fossils were obtained from a small section of the Beds, and the Beds may range in age from an older limit of Upper Cambrian based on the Hanson River Beds overlying Point Wakefield Beds containing a brachiopod of age younger than Upper Cambarian in BMR Grg 18, (Milligan, 1963) to an unknown younger limit for sediments which do not crop out, but are concealed beneath the Lake Surprise Sandstone in the Lander Trough.|16-MAY-23
8055|Hanson River Beds|Proposed publication|Bureau of Mineral Resources Bulletin|16-MAY-23
8055|Hanson River Beds|Comments|Notes: Name published without definition in Randal (1973). K.G. Smith, in his original definition (pers. comm., 1965) states that "the fauna, and in part, the lithology, of the Beds provides correlation with Upper Cambrian, Lower and Middle Ordovician units of the Georgina Basin, and the sequence provides new information on Upper Cambrian-Middle Ordovician sedimentation in the Wiso Basin, Northern Territory". Records of the fauna referred to are now unavailable, and presumably have been lost. The term "Beds" is proposed for this rock unit because of the poorly known nature of its basal contact, because the unit is extremely poorly exposed hence its lithology and age poorly known, and because its extent is uncertain.|16-MAY-23
8225|Heavitree Quartzite|Name source|The Heavitree Quartzite was named after Heavitree Gap by Joklik (1955). The four formal members of the Heavitree Quartzite are named after Undoolya, Temple Bar and Fenn gaps, and Mount Blatherskite (Stewart et al 1980).|16-MAY-23
8225|Heavitree Quartzite|Unit history|Heavitree Gap Quartzite or No. 1 quartzite of Chewings (1928), No. 1 Ridge quartzite (Ward 1925) and Heavitree Range quartzite and Heavitree quartzite (Madigan 1932). These names are no longer in use. See also the NT Stratigraphic Lexicon (1962) for more information on the history of this unit.|16-MAY-23
8225|Heavitree Quartzite|Constituents|Blatherskite Quartzite Member, Fenn Gap Conglomerate Member, Temple Bar Sandstone Member, Undoolya Siltstone Member.|16-MAY-23
8225|Heavitree Quartzite|Geomorphic expression|Prominent ridges that can extend for several 100s of kms.|16-MAY-23
8225|Heavitree Quartzite|Type section locality|The type area for undifferentiated Heavitree Quartzite includes the cliffs west of Ingwallumum Gap (Spring Gap) at GDA94 53K 524150mE 7247050mN in the 1:250 000 ILLOGWA CREEK sheet area.|16-MAY-23
8225|Heavitree Quartzite|Extent|Heavitree Quartzite crops out over a distance of ~ 800 km east-west along the northern margin of the Amadeus Basin. The quartzite forms an upstanding erosional strike ridge particularly along the upturned edge of the MacDonnell homocline in the MacDonnell Ranges. The less silicified portion of the unit is isolated to the Limbla Cliffs.|16-MAY-23
8225|Heavitree Quartzite|General description|Heavitree Quartzite crops out almost continuously over a distance of ~ 800 km east-west along the contemporary northern margin of the Amadeus Basin, where it forms the majority of the prominent ridges. The sedimentary rocks exposed in the type area show little evidence of silicification compared the members at Heavitree Gap. It is therefore difficult to directly correlate the  sequences in the northeastern Amadeus with the  formally defined, but strongly silicified members. Lindsay (1999) divided the Heavitree Quartzite at Heavitree Gap into four sequences, these likely correlate with the four formal members recognised at Heavitree Gap.	|16-MAY-23
8225|Heavitree Quartzite|Thickness range|100-300 m. Has been reported to be as thick as 440m at Ellery Creek, however, this is likely complicated by folding (Madigan 1932, Prichard and Quinlan 1962).|16-MAY-23
8225|Heavitree Quartzite|Lithology|Fine-, medium- or coarse-grained, planar and cross-bedded, variably feldspathic quartzose sandstone, pink, grey, pinkish-brown, purple or white weathering, and rare laminated mudstone or conglomerate intervals. Low angle sigmoidal cross-bed sets range from 1-10 m thick are distinctive and are characterised by three types of internal bedding: (a) primary erosional bedding surfaces; (b) sigmoidal foreset surfaces with (c) steeper cross-bed surfaces within them (Lindsay 1999). Large-scale planar and trough cross-beds area also common. Additional sedimentary structures include a variety of ripple mark types, and occasional herringbone cross-stratification.|16-MAY-23
8225|Heavitree Quartzite|Depositional environment|High-energy, open shelf-like tidal setting in which currents were alternately asymmetric and unidirectional (Lindsay 1999). Alternatively, Plummer (2015) suggested that the depositional setting was predominantly a fluvial-dominated catchement cluster that discharged through a deltaic system into a central shallow depocentre. This depocentre had marine-influences via a narrow seaway.|16-MAY-23
8225|Heavitree Quartzite|Fossils|None observed in type area, however possible trace fossils similar to Skolithos were reported by Lindsay (1991) from probable tidally influenced sandstones from the Heavitree Quartzite in the northeast of the Amadeus Basin. Lindsay (1991, 1999) said these 'burrow-like' structures may be organic in origin or possibly due to water-escape.|16-MAY-23
8225|Heavitree Quartzite|Diastems or hiatuses|Primary erosional bedding surfaces between depositional cycles.|16-MAY-23
8225|Heavitree Quartzite|Relationships and boundaries|Conformable, gradational contact with the overlying Bitter Springs Group. Ingwallamum granite (Whelan et al in prep), granitic gneiss, migmatite and mafic schist of the Arunta Region basement are exposed within the section but an exposed contact with the overlying Heavitree Quartzite was not observed.|16-MAY-23
8225|Heavitree Quartzite|Identifying features|These massive sandstone beds in fact range from 1-10 m thick and comprise low-angle, sigmoidal cross-bed sets.|16-MAY-23
8225|Heavitree Quartzite|Structure and Metamorphism|Part of the type area is on the southern limb of a shallowly dipping, northwest plunging anticline and the section is cross-cut by a northwest-trending fault. This apparently resulted in a partial repetition of the succession. Overall the Heavitree Quartzite has been significantly folded and faulted throughout the basin causing varying degrees of silicification of the unit.|16-MAY-23
8225|Heavitree Quartzite|Age reasons|Detrital zircon analysis suggests a maximum depositional age of 1050 to 1000 Ma (Camacho et al 2002, Maidment 2005, Maidment et al 2007; Kositcin et al 2014). It is thought that the Heavitree Quartzite sits in the Cryogenian subdivision of the Neoproterozoic (e.g. Grey 2005).|16-MAY-23
8225|Heavitree Quartzite|Correlations|The sedimentary rocks exposed in the type area show little evidence of silicification compared the members at Heavitree Gap. It is therefore difficult to directly correlate the sequences in the northeastern Amadeus with the  formally defined, but strongly silicified members. Lindsay (1999) divided the Heavitree Quartzite at Limbla into four sequences, these likely correlate with the four formal members recognised at Heavitree Gap. Heavitree Quartzite is interpreted to be correlative with the Dean Quartzite of the southwestern Amadeus Basin; Vaughan Springs Quartzite of the Ngalia Basin; Amesbury Quartzite and Yackah beds of the southwestern and southeastern Georgina Basin respectively and Stanovos Quartzite of Irindina Province, Arunta Region (Munson et al 2013 and references therein). Possibly correlates with the Kulail Sandstone, southwestern Amadeus Basin, in part.|16-MAY-23
8225|Heavitree Quartzite|Alteration and Mineralisation|Gold mineralisation within deformed Heavitree Quartzite in White Range area at the Arltunga Goldfield and Heavitree Quartzite/Bitter Springs Formation at Winneke goldfield. Gold mineralisation is mainly in basement rocks of the Arunta Region however some is found in overlying Heavitree Quartzite (Edgoose 2013). The Heavitree Quartzite-Gillen Formation succession has also been identified as a petroleum system and has been proven as a sub-economic resource of gas/helium in Magee -1 (Marshall 2003).|16-MAY-23
8225|Heavitree Quartzite|Defn author|VJ Normington, N Donnellan 28-SEP-2015. Definition approved by Jo Whelan and Verity Normington NT  Stratigraphic Names Subcommittee  29-SEP-2015.|16-MAY-23
8225|Heavitree Quartzite|References|Camacho A, Hensen B and Armstrong R, 2002. Isotopic test of a thermally driven intraplate orogenic model, Australia. Geology 30, 887-890.  **Chewings C, 1928. Further notes on the stratigraphy of central Australia. Transactions of the Royal Society of South Australia 52, 62-81.  **Edgoose C, 2013. Amadeus Basin: in Ahmad M and Munson  TJ (editors) 'Geology and mineral resources of the Northern Territory; Special Publication 5', Northern Territory Government.  **Grey, K. 2005. Ediacaran palynology of Australia. Association of Australasian Palaeontologists, Memoir 31.  **Jöklik GF, 1955. The geology of the mica fields of the Harts Range, central Australia. Bureau of Mineral Resources of Australia, Bulletin 26.  **Kositcin N, Whelan JA, Hallett L and Beyer EE, 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.  **Lindsay JF, 1991. New evidence for ancient metazoan life in the Late Proterozoic Heavitree Quartzite, Amadeus Basin, central Australia: in Korsch RJ and Kennard JM (editors) 'Geological and geophysical studies in the Amadeus Basin, central Australia'. Bureau of Mineral Resources, Australia, Bulletin 236, 7-32.   **Lindsay JF, 1999. Heavitree Quartzite, a Neoproterozoic (ca 800-760 Ma), high-energy, tidally influenced, ramp association, Amadeus Basin, central Australia. Australian Journal of Earth Sciences 46, 127-139.  **Madigan CT, 1932. The geology of the western MacDonnell Ranges, central Australia. Quarterly Journal of the Geological Society of London 88, 672-711.  **Maidment DW, 2005. Palaeozoic high-grade metamorphism within the Centralian Superbasin, Harts Range region, central Australia, Australian National Univeristy Canberra.  **Maidment DW, Williams IS and Hand M, 2007. Testing long-term patterns of basin sedimentation by detrital zircon geochronology, Centralian Superbasin, Australia. Basin Research 19, 355-360.  **Marshall T, 2003. Petroleum systems and source rocks in the Amadeus Basin, Northern Territory. Petroleum Exploration Society of Australia, Queensland Branch Symposium, 37-43.   **Munson TJ, Kruse PD and Ahmad M, 2013. Centralian Superbasin: in Ahmad M and Munson  TJ (editors) 'Geology and mineral resources of the Norhern Territory; Special Publication 5', Northern Territory Government.  **Normington VJ, Donnellan N and Edgoose C, in prep. Characterisation of the Neoproterozoic stratigraphy of the northeast Amadeus Basin, Northern Territory. : in Northern Territory Geological Survey R (editor).  **Plummer P, 2015. Heavitree Quartzite, Amadeus Basin: it's within the Centralian Superbasin. Annual Geoscience Exploration Seminar (AGES) 2015. Record of abstracts. NTGS Record 2015-002.  **Stewart AJ, Shaw RD, Langworthy AP, Warren RG, Allen AR and Clarke AB, 1980. Stratigraphic definitions of named units in the Arunta Block, Northern Territory, BMR Report 216, Bureau of Mineral Resources.  **Prichard CE and Quinlan T, 1962. The geology of the southern half of the Hermannsburg 1:250 000 sheet. BMR Report No. 61. Bureau of Mineral Resources Geology and Geophysics (editor).  **Ward LK, 1925. Notes on the geological structures of South Australia. Transactions of the Royal Society of South Australia 49, 34-61.  **Whelan JA, Webb G and Close DF, in prep. Limbla Special, Northern Territory. 1:100 000 geological map series 5950. Northern Territory Geological Survey, Darwin.|16-MAY-23
27659|Hillsoak Bore metamorphics|Name source|Hillsoak Bore (GR 5850-518004), situated in western part of outcrop area of Hilsoak Bore metamorphics, Fergusson Range 1:100 000 Sheet area.|16-MAY-23
27659|Hillsoak Bore metamorphics|Type section locality|Reference locality: 6 km section across well-exposed ridges of above sequence from GR 5850-515967 to GR 5850-565994 in Fergusson Range 1:100 000 Sheet area.|16-MAY-23
27659|Hillsoak Bore metamorphics|Extent|Northwestern part of Fergusson Range and southwestern part of Riddoch 1:100 000 Sheet area.|16-MAY-23
27659|Hillsoak Bore metamorphics|Lithology|Sequence (from west to east) of marble, calc-silicate rock, andalusite schist, interbedded amphibolite, schist and quartzite, granitic gneiss interfingering with two-mica schist, overlain by biotite gneiss containing amphibolite bodies; biotite gneiss grades into sillimanite gneiss at eastern end of sequence.|16-MAY-23
27659|Hillsoak Bore metamorphics|Relationships and boundaries|Older rocks not known or recognised. Interfingers with metatonalite of Atnarpa Igneous Complex, consistent with large-scale 'lit-par-lit' intrusion by Atnarpa Complex. Interfingers conformably with Cadney metamorphics to northwest, in Laughlen 1:100 000 Sheet area. Unconformably overlain by Heavitree Quartzite.|16-MAY-23
27659|Hillsoak Bore metamorphics|Identifying features|Reason for proposed name: A distinct and easily mapped sequence of metasediments, very different from adjoining rocks.|16-MAY-23
27659|Hillsoak Bore metamorphics|Age reasons|Time of metamorphism presumably same as 1719 +/- 24 m.y.  Rb-Sr whole-rock isochron on adjoining Cadney metamorphics, Cavenagh metamorphics (q.v.), and Atnarpa Igneous Complex (q.v.). Correlated with Cadney ;metamorphics, and estimate of maximum age of parent rock for the one sample of Cadney metamorphics on the 1719 isochron is 1800 m.y. = Early Proterozoic.|16-MAY-23
27659|Hillsoak Bore metamorphics|Proposed publication|1. 'Geological report on 1:100 000 scale mapping of southeastern Arunta Block, Alice Springs 1:250 000 Sheet area, Northern Territory' by R.D. Shaw et al. BMR Microficeh Report in prep.  2. 'Stratigraphic definitions in the Arunta Block' - BMR Microfiche Report.|16-MAY-23
27659|Hillsoak Bore metamorphics|Defn Reference|80/20787|16-MAY-23
27659|Hillsoak Bore metamorphics|Reserved? Yes/No|Yes|16-MAY-23
8641|Ida Granite|Name source|After Mount Ida (GR 4676E, 7512N AMG, metric) within outcrop area, Alcoota 1:250 000 Sheet area, SF 53-10, Australian map Grid.|16-MAY-23
8641|Ida Granite|Unit history|Previous informal name: Mount Ida Granite, discontinued as Mount Ida already used for stratigraphic unit in Victoria.|16-MAY-23
8641|Ida Granite|Type section locality|3 km north-northwest of Mount Ida in a tor-like hill at GR 4465E, 75150N.|16-MAY-23
8641|Ida Granite|Description at type locality|Grey even-grained gneissic granite.|16-MAY-23
8641|Ida Granite|Extent|From 7 km south of Mount Ida to 14 km north.|16-MAY-23
8641|Ida Granite|Lithology|Gneissic biotite granite, rare adamellite.|16-MAY-23
8641|Ida Granite|Relationships and boundaries|The Ida Granite intrudes the Delmore Metamorphics and probably intrudes the Delny Gneiss and the Mapata Gneiss. The Ida Granite intrudes the Copia Granite.|16-MAY-23
8641|Ida Granite|Proposed publication|BMR Report|16-MAY-23
8641|Ida Granite|Comments|Pegmatites common close to margin both within intrusive and in the country rock.|16-MAY-23
24316|Ingula migmatite suite|Name source|Ingula Hills, GR 5651-865406 Burt 1:100 000 Sheet area.|16-MAY-23
24316|Ingula migmatite suite|Unit history|Previously mapped by Wells & others (1968) as undivided Arunta Complex.|16-MAY-23
24316|Ingula migmatite suite|Type section locality|Refereance area: From Saltbush Bore (GR 5651-930399) northwest along creek to GR 5651-905436.|16-MAY-23
24316|Ingula migmatite suite|Extent|Highly faulted region in the central northeastern corner of Burt 1:100 000 Sheet area 7 km north-northeast of Snake Well.|16-MAY-23
24316|Ingula migmatite suite|Lithology|The suite is a complex unit consisting mainly of migmatite, granitic gneiss and quartzofeldspathic gneiss, with small amounts of cordierite gneiss, amphibolite, mafic granulite, and sillimanite gneiss.|16-MAY-23
24316|Ingula migmatite suite|Relationships and boundaries|The suite has a gradational contact with the Erontonga metamorphics as migmatisation decreases, and with the Wuluma Granitoid as migmatite passes into granitoid. The suite is faulted against the Enbra Granulite.|16-MAY-23
24316|Ingula migmatite suite|Age reasons|Middle Proterozoic or older. The unit is gradational with the Wuluma Granite which has a preliminary Rb-Sr total rock date of 1800 m.y. (L P Black, BMR, pers. comm., 1978). The suite has been placed in the Strangways Metamorphic Complex.|16-MAY-23
24316|Ingula migmatite suite|Proposed publication|Stewart & others in prep.|16-MAY-23
24316|Ingula migmatite suite|Defn Reference|80/20787|16-MAY-23
24316|Ingula migmatite suite|Proposer|Langworthy A.P. (in Shaw & others, in prep.)|16-MAY-23
75537|Jarong Spring Gabbro|Name source|After Jarong Spring GDA 94 52L, 695700mE 8409400mN (-14°22'51"S 130°48'54"E) on Fergusson River and Port Keats 1:250 000 mapsheets, Moyle and Wingate Mountains 1:100 000 mapsheets, Litchfield Province, Pine Creek Orogen, Northern Territory|16-MAY-23
75537|Jarong Spring Gabbro|Unit history|Previously known as Wangi Basics, first used by Needham and Stuart-Smith (1984) and formally defined in Dundas et al (1987). The name Wangi Basics is abandoned, as it is now known to comprise distinct geochemical groups of rocks which are genetically unrelated.|16-MAY-23
75537|Jarong Spring Gabbro|Geomorphic expression|Blocky ridges within surrounding metasedimentary host rocks.|16-MAY-23
75537|Jarong Spring Gabbro|Type section locality|Prominent sill (ca 0.6 km length) within Chilling Sandstone, Wingate Mountains 1:100 000 mapsheet (Fergusson River 1:250 000 mapsheet), GDA 94 52L 668414mE 8434455mN ( 14º9'22"S 130°33'37"E).|16-MAY-23
75537|Jarong Spring Gabbro|Description at type locality|Occurs as a prominent linear sill in Wingate Mountains  1:100 000 mapsheet, length ca 0.6 km within the Chilling Sandstone|16-MAY-23
75537|Jarong Spring Gabbro|Extent|Linear sills over an area of about 6 km long and 200 m wide in Wingate Mountains and Moyle 1:100 000 mapsheets.|16-MAY-23
75537|Jarong Spring Gabbro|General description|Occurs as a series of linear sills in Wingate Mountains and Moyle 1:100 000 mapsheets|16-MAY-23
75537|Jarong Spring Gabbro|Lithology|Metamorphosed high-Ti tholeiitic gabbro mostly occurring as SW-NE trending linear sills,  over an area ca 6 km long and 200m wide within Burrell Creek Formation and Chilling Sandstone (Edgoose et al 1989). Mostly quartz-hypersthene normative. Consists of metamorphosed equigranular assemblages of (rare) quartz, plagioclase with highly sausseritised/sericitised cores and unaltered rims, clinopyroxene, pale brown to green pleochroic hornblende. Fibrous actinolite/tremolite and uralitised hornblende is common.|16-MAY-23
75537|Jarong Spring Gabbro|Depositional environment|Genesis:  Intrusive sills into metasedimentary Burrell Creek Formation and Chilling Sandstone.|16-MAY-23
75537|Jarong Spring Gabbro|Relationships and boundaries|Intrudes the ca 1860 Ma Burrell Creek Formation and Chilling Sandstone in Wingate Mountains and Moyle 1:100 000 mapsheets|16-MAY-23
75537|Jarong Spring Gabbro|Identifying features|Typically high-Ti tholeiitic gabbros with characteristic alkaline enrichment (Glass 2007, 2010).|16-MAY-23
75537|Jarong Spring Gabbro|Structure and Metamorphism|Amphibolite-facies metamorphism. Disrupted by NNE¿SSW-trending faults. First Edition mapping  (Edgoose et al 1989) shows regional open folding of host successions around SSW-plunging axes.|16-MAY-23
75537|Jarong Spring Gabbro|Age reasons|Not adequately constrained but <ca 1860 Ma or younger based on field relationships with the metasedimentary Burrell Creek Formation and Chilling Sandstone.|16-MAY-23
75537|Jarong Spring Gabbro|Alteration and Mineralisation|Sausseritisation/sericitisation of feldspars. Hornblende altered to actinolite/tremolite and uralite. Minor chlorite alteration.|16-MAY-23
75537|Jarong Spring Gabbro|Geophysical Expression|Linear sills have a strong positive magnetic response|16-MAY-23
75537|Jarong Spring Gabbro|Geochemistry|High-Ti tholeiitic gabbro  (TiO2 values ranging from 1.9 to 4.2 wt%, average value 2.3 wt% TiO2) with some degree of alkaline enrichment (Glass 2007, 2010).|16-MAY-23
75537|Jarong Spring Gabbro|Defn author|Glass, L.M. (NTGS),  03-NOV-2010|16-MAY-23
75537|Jarong Spring Gabbro|References|**DUNDAS DL, Edgoose CJ, Fahey GM and Fahey JE, 1987. Daly River 1:100 000 Geological Map Series. Northern Territory Geological Survey Explanatory Notes (5070).    **EDGOOSE CJ, Fahey GM and Fahey JE, 1989. Wingate Mountains 1:100 000 Geological Map Series. Northern Territory Geological Survey Explanatory Notes (5069).    **GLASS LM, 2007. Geochemistry of mafic rocks in the Litchfield Province, western Pine Creek Orogen: Evidence for a Palaeoproterozoic arc-related setting and links to the Halls Creek Orogen: in 'Annual Geoscience Exploration Seminar (AGES) 2007. Record of Abstracts.' Northern Territory Geological Survey, Record 2007 001.    **GLASS LM, 2010. Palaeoproterozoic island-arc-related rocks of the Litchfield Province, western Pine Creek Orogen, Northern Territory. Northern Territory Geological Survey, Record 2010-005.    **NEEDHAM RS, Stuart-Smith PG, 1984. Geology of the Pine Creek Geosyncline, Northern Territory, 1:500 000 scale map. Bureau of Mineral Resources, Australian Bureau of Mineral Resources, Canberra. ACT.|16-MAY-23
27952|Jessie Gap gneiss|Name source|Jessie Gap - a water-gap in the Heavitree Quartzite about 6 km south of Undoolya homestead in Undoolya 1:100 000 Sheet.|16-MAY-23
27952|Jessie Gap gneiss|Type section locality|Alice Springs 1:100 0000 Sheet; GR 5650-968788.|16-MAY-23
27952|Jessie Gap gneiss|Extent|Crops out east of Alice Springs and exteands from the Alice Springs 1:100 0000 Sheet into Undoolya 1:100 000 Sheet.|16-MAY-23
27952|Jessie Gap gneiss|Lithology|Typically even-grained, mediu;m-grained poorly foliated gneiss of granitic composition. Some samples contain small amount of sillimanite. At margin of the Jessie Gap gneiss some interlayered amphibolite, hornblende gneiss and banded biotite gneiss. Contains some metamorphosed granite and porphyry.|16-MAY-23
27952|Jessie Gap gneiss|Relationships and boundaries|Unconformably overlain by the Heavitree Quartzite; intruded by Stuart Dyke Swarm (new name); concordant contact with unnamed metasediments to the west and grades into unnamed gneiss to the east.|16-MAY-23
27952|Jessie Gap gneiss|Identifying features|Reason for proposed name: Fairly homogeneous distinct unit cropping out in the eastern part of the Alice Springs Block.|16-MAY-23
27952|Jessie Gap gneiss|Age reasons|Jessie Gap gneiss may have been granitised and partly intruded by granite and porphyry during the thermal event which accompanied the Ormiston Phase of deformation at about 1080 m.y. The gneiss is older than the Late Proterozoic Heavitree Quartzite which unconformably overlies it and the dolerite dykes which intrude it.|16-MAY-23
27952|Jessie Gap gneiss|Proposed publication|Geological report on 1:100 000 scale mapping of southeastern Arunta Block, Alice Springs 1:250 000 Sheet area, Northern Territory by R D Shaw et al.  BMR Microfiche report in prep.|16-MAY-23
27952|Jessie Gap gneiss|Defn Reference|80/20787|16-MAY-23
27952|Jessie Gap gneiss|Proposer|Offe L.A.|16-MAY-23
27952|Jessie Gap gneiss|Resdate|18-MAR-1975|16-MAY-23
27952|Jessie Gap gneiss|Reserved? Yes/No|Yes|16-MAY-23
9201|Kanandra Granulite|Name source|After Kanandra Dam (GR 4982E, 7482N AMG-metric) within outcrop area; Alcoota 1:250 000 S/A SF53-10 AMG.|16-MAY-23
9201|Kanandra Granulite|Type section locality|Centred on Mount Swan (GR 492E, 748048N AMG metric) and up to 2 km away.|16-MAY-23
9201|Kanandra Granulite|Extent|Outcrop area extends northwest from Kanandra Gap virtually to the Bundey River and northeast into the Huckitta 1:250 000 Sheet area.|16-MAY-23
9201|Kanandra Granulite|Lithology|Felsic gneiss, mafic granulite, biotite-garnet-potassium feldspar-quartz migmatite, minor calc-silicate gneiss, rare cordierite-bearing felsic gneiss. All exposed in type area.|16-MAY-23
9201|Kanandra Granulite|Relationships and boundaries|Harts Range Group thought to overlie the Kanandra Granulite in a regional syncline. Mount Suan Granite either intrudes the Kanandra Granulite or is anatectically derived from the Kanandra Granulite. Possibly overlain by the Mapata Gneiss.|16-MAY-23
9201|Kanandra Granulite|Identifying features|Distinguished from Mapata Gneiss by considerably greater proportion of mafic rocks. Distinguished from Mount Bleechmore Granulite by higher content of felsic gneiss and very much smaller content of pelitic gneiss.|16-MAY-23
9201|Kanandra Granulite|Correlations|Tentative correlations: Considered equivalent to the Mount Bleechmore Granulite; and the Ongeva Granulite (Alice Springs 1:250 000 Sheet area).|16-MAY-23
9201|Kanandra Granulite|Proposed publication|BMR Report|16-MAY-23
9201|Kanandra Granulite|Name first published by|Shaw R.D., Warren R.G., Kopras J., Green D.E., 1975|16-MAY-23
75535|Keri Suite|Name source|After Keri homestead on Pine Creek 1:250 000 mapsheet, Reynolds River 1:100 000 mapsheet, Litchfield Province, Pine Creek Orogen, Northern Territory. GDA 94 52L 669230mE 8534660mN ( 13°15'9"S 130°33'43"E).|16-MAY-23
75535|Keri Suite|Unit history|Previously known as Wangi Basics, which was first used by Needham and Stuart-Smith (1984) and formally defined in Dundas et al (1987). The name Wangi Basics is abandoned, as it is now known to comprise distinct geochemical groups which are genetically unrelated.|16-MAY-23
75535|Keri Suite|Geomorphic expression|Boulder strewn outcrops and well-rounded boulders in Reynolds River 1:100 000 mapsheet.|16-MAY-23
75535|Keri Suite|Type section locality|Low boulder-strewn hills ca 12 km north of Keri homestead on Reynolds River 1:100 000 mapsheet. GDA 94 52L 670455mE 8548345mN (-13°7'35"S 130°34'21"E).|16-MAY-23
75535|Keri Suite|Description at type locality|Low boulder-strewn hills amongst Cenozoic cover.|16-MAY-23
75535|Keri Suite|Extent|Surface exposures occur within an area of ca 16 km2 in NW Reynolds River 1:100 000 mapsheet; however, magnetic imagery indicates that the true extent under surficial cover may be much greater.|16-MAY-23
75535|Keri Suite|General description|Metamorphosed noritic cumulates, metapyroxenite and metaperidotite, and garnet-bearing mafic amphibolite (Glass 2007, 2010). Only exposed in NW Reynolds River 1:100 000 mapsheet.|16-MAY-23
75535|Keri Suite|Thickness range|Not known due to poor exposure|16-MAY-23
75535|Keri Suite|Lithology|Metamorphosed mafic/ultramafic assemblages (metamorphosed noritic cumulates, metapyroxenite and metaperidotite) and garnet-bearing mafic amphibolite (meta-ferrogabbro) (Glass 2007, 2010).|16-MAY-23
75535|Keri Suite|Depositional environment|Genesis: Intrusive|16-MAY-23
75535|Keri Suite|Relationships and boundaries|Field contact relationships not observed, but possibly intrudes the Welltree Metamorphics (Pietsch 1989).|16-MAY-23
75535|Keri Suite|Identifying features|Metamorphosed mafic/ultramafic assemblages are moderate to strongly foliated (typical mineral assemblages include tremolite, anthophyllite, actinolite and hornblende). Meta-ferrogabbro has distinctive large garnet porphyroblasts up to and greater than 10 mm in diameter, which often amalgamate to form linear segregations in an amphibole-rich groundmass.|16-MAY-23
75535|Keri Suite|Structure and Metamorphism|Amphibolite-facies metamorphism.|16-MAY-23
75535|Keri Suite|Age reasons|Carson et al (2009) determined a weighted mean 207Pb/206Pb SHRIMP age of 1860 +/- 6 Ma (95% confidence level) for a garnet-bearing mafic amphibolite, which is interpreted to represent the magmatic crystallization age for this sample.|16-MAY-23
75535|Keri Suite|Alteration and Mineralisation|Abundant fibrous amphibole (tremolite-actinolite) is interlaminated with chlorite and is most likely the replacement product of primary orthopyroxene. Uralitic amphibole is most likely derived from granular clinopyroxene. Residual partly seriticised (+/- clinozoisite) platy plagioclase (up to 2 mm in size) has in part been overprinted by recrystallised amphibole. No known mineralisation.|16-MAY-23
75535|Keri Suite|Geophysical Expression|Appears to be associated with a magnetic high in NW corner of Reynolds River 1:100 000 mapsheet, which extends slightly into adjoining mapsheets. No observable radiometric or gravity response.|16-MAY-23
75535|Keri Suite|Geochemistry|Metamorphosed noritic cumulates are typically low-Ti, and highly magnesian. Meta-ferrogabbros are metamorphosed plagioclase-pyroxene cumulates with very high FeOt, 18.8 to 23.2 wt% (Glass 2010).|16-MAY-23
75535|Keri Suite|Defn author|Glass, L.M. (NTGS)  03-NOV-2010|16-MAY-23
75535|Keri Suite|References|**CARSON CJ, Claoué-Long J, Stern RA, Close DF, Scrimgeour IR and Glass, LM, 2009. Summary of results. Joint NTGS-GA geochronology project: Arunta and Pine Creek regions, July 2006-May 2007. Northern Territory Geological Survey Record 2009-1.    **DUNDAS DL, Edgoose CJ, Fahey GM and Fahey JE, 1987. Daly River 1:100 000 Geological Map Series. Northern Territory Geological Survey Explanatory Notes (5070).    **GLASS LM, 2007. Geochemistry of mafic rocks in the Litchfield Province, western Pine Creek Orogen: Evidence for a Palaeoproterozoic arc-related setting and links to the Halls Creek Orogen: in 'Annual Geoscience Exploration Seminar (AGES) 2007. Record of Abstracts.' Northern Territory Geological Survey, Record 2007 001.    **GLASS LM, 2010. Palaeoproterozoic island-arc-related rocks of the Litchfield Province, western Pine Creek Orogen, Northern Territory. Northern Territory Geological Survey, Record 2010-005.    **NEEDHAM RS, Stuart-Smith PG, 1984. Geology of the Pine Creek Geosyncline, Northern Territory, 1:500 000 scale map. Bureau of Mineral Resources, Australian Bureau of Mineral Resources, Canberra. ACT.    **PIETSCH BA, 1989. Reynolds River, 1:100 000 Geological Map Series. Northern Territory Geological Survey Explanatory Notes (5071).|16-MAY-23
9736|Kombolgie Formation|Name source|The name was defined by Walpole and others (1968) as comprising sandstone but with a large number of felsic and mafic volcanic units. Needham & Stuart-Smith (in press) determined that Walpole & others' Kurrundie Member and Plum Tree Creek Volcanic Member rest unconformably beneath the Kombolgie Formation, and have moved them (after elevation for each to Formation status) to the Edith River Group. The remaining volcanic members (all intermediate to mafic in composition) have been recorrelated largely on the basis of their position within the Kombolgie Formation sandstone sequence, so that the McAddens, Callanan, Birdie Creek and Nungbalgarri Volcanic Members all form one horizon generally between 120 m and 1100 m above the base of the formation, and the Henwood and Gilruth Volcanic Members form another horizon about 200 m higher. Elements of the definition of the Formation which here are changed as a consequence are:|16-MAY-23
9736|Kombolgie Formation|Type section locality|North side of Deaf Adder Gorge for a distance of 12 km from the mouth of Gorge (13o05'S, 132o50'E). Contains lower and upper (un-named) sandstone sequences separated by the Nungbalgarri Volcanic Member.|16-MAY-23
9736|Kombolgie Formation|Thickness range|On Arnhem Land Plateau the complete sequence measures up to 1050 m but generally thins northeast to about 650 m in the Goomadeer River area. In a number of basins in the El Sherana to Katherine area the complete sequence measures up to at least 1700 m in places.|16-MAY-23
9736|Kombolgie Formation|Lithology|Lithology: sandstone, pebbly sandstone, commonly cross-stratified and rippled in thin (~10 cm) to thick (>20 m) beds. Conglomerate, commonly near base. Rare siltstone beds <5 m thick. Andesite and basalt flows at two horizons. The arenite units are un-named. The volcanic members are: (lower horizon) McAddens, Callanan, Birdie Creek, Nungbalgarri  Volcanic Members; (upper horizon) Henwood and Gilruth Volcanic Members.|16-MAY-23
9736|Kombolgie Formation|Relationships and boundaries|Unconformably to disconformably overlies rocks of the Edith River Group, unconformable on rocks of the El Sherana Group, Finniss River Group and older units of the Early Proterozoic sequence of the Pine Creek Geosyncline and their metamorphic equivalents. Apparently unconformable on Oenpelli Dolerite. Unconformable on Jim Jim, Nabarlek and Tin Camp Granites. Overlain apparently conformably by Mount Rigg Group. Intruded by Wurugoij Dolerite.|16-MAY-23
9736|Kombolgie Formation|Age reasons|~1648 +/- 29 Ma (Page & others, 1980 Rs-Sr isochron on Nungbalgarri Volcanic Member). Rests unconformably on 1688 +/- 13 Ma Oenpelli Dolerite, intruded by ~1200 Ma Wurugoij Dolerite (Page & others, 1980).|16-MAY-23
9736|Kombolgie Formation|Proposed publication|Needham R.S. & Stuart-Smith (in press) Australian Journal of Earth Sciences. Needham R.S. & Stuart-Smith (1984) 1:500 000 scale map.|16-MAY-23
24341|Koolpinyah Dolomite|Name source|"Koolpinyah" Homestead on Koolpinyah 1:100 000 Sheet (5173) GR GM366295.|16-MAY-23
24341|Koolpinyah Dolomite|Unit history|Referred to on the 1980 BMR 1:500 000 geological map of the Pine Creek Geosyncline as Coomalie Dolomite.|16-MAY-23
24341|Koolpinyah Dolomite|Type section locality|Diamond Drill Hole Y22, location GM 442286. Intersection 52 m to 603 m. Hole drilled by Urangescellshaft Australia Pty Ltd. Core is stored at the Northern Territory Department of Mines and Energy Core Library, Darwin.|16-MAY-23
24341|Koolpinyah Dolomite|Extent|Central and eastern part of Koolpinyah 1:100 0000 sheet area, northwest part of Point Stuart 1:100 000 sheet area and extreme central northern part of Noonamah 1:100 000 sheet area. The unit is overlain by up to 80 metres of Mesozoic and Cainozoic sediments. Outcrop is extremely poor, confined to very small exposures of silicified carbonate and quartzite.|16-MAY-23
24341|Koolpinyah Dolomite|Thickness range|Unknown, at least 100 m and probably less than 1000 m.|16-MAY-23
24341|Koolpinyah Dolomite|Lithology|Dolomite, dolomitic marble, dolomitic chlorite +/- mica +/- quartz schist, mica-quartz schist, dolomitic quartzite, sandy intraclastic limestone.|16-MAY-23
24341|Koolpinyah Dolomite|Relationships and boundaries|Overlain by Whites Formation sediments in western and central part of Koolpinyah 1:100 000 sheet area. Unconformably overlies the Woolner Granite and Dirty Water Metamorphics in the north-eastern part of Koolpinyah 1:100 0000 sheet. The lower and uppermost units are massive dolomite. This formation appears to occupy the same stratigraphic position as the Coomalie Dolomite and is interpreted as a deeper water facies variant.|16-MAY-23
24341|Koolpinyah Dolomite|Age reasons|Early Proterozoic, as it forms part of the Early Proterozoic sedimentary sequence of the Pine Creek Geosyncline.|16-MAY-23
24341|Koolpinyah Dolomite|Proposed publication|Explanatory Notes, Koolpinyah 1:100 000 sheet (Northern Territory Geological Survey)|16-MAY-23
24341|Koolpinyah Dolomite|First Reference|86/25403 p.6 Described.|16-MAY-23
29263|Lander Rock beds|Name source|Lander Rock (5453-825374), a prominent hill between Reynolds and Anmatjira Ranges, Reynolds Range 1:100 000 Sheet area.|16-MAY-23
29263|Lander Rock beds|Unit history|Called by Australian Geophysical (1967) 'Elgamba Quartzite' in Reynolds Range, and 'Interbedded micaceous schists and schistose quartzite' at Lander Rock. Included in 'Metasediments and metamorphics of uncertain origin' of Evans & Glikson (1969). Mapped as 'Precambrian schist, metasediments, including marble' by Wells & others (1971).|16-MAY-23
29263|Lander Rock beds|Type section locality|Reference area: Lander Rock itself provides good exposure of the beds.|16-MAY-23
29263|Lander Rock beds|Extent|Mainly along northern flanks of Reynolds and Giles Ranges; northwest part of Aileron 1:100 000 Sheet; scattered exposures in northern part of Tea Tree and various parts of Denison 1:100 0000 Sheet areas and in Mount Peake, Mount Theo, Mount Solitaire and Lander River 1:250 000 Sheet areas. Also recognised but not yet mapped in northern part of Mount Doreen 1:250 000 Sheet area.|16-MAY-23
29263|Lander Rock beds|Lithology|Grey to brown thin to medium-bedded, weakly metamorphosed micaceous sandstone, siltstone, shale, slate; small amounts of phyllite, quartzite, chert, and amphibolite and their higher-grade metamorphic equivalents (pelitic schist, gneiss, and granofels) to the southeast.|16-MAY-23
29263|Lander Rock beds|Relationships and boundaries|No underlying unit known; faulted against Weldon metamorphics and Tyson Creek granulite (q.v.) to northeast: unconformably overlain by Mount Thomas Quartzite (q.v.) of Reynolds Range Group (q.v.) to southwest; intruded by Anmatjira, Mount Airy, and Yaningidjara Orthogneisses (q.v.), by Harverson Granite, by small bodies of unnamed granite, and by Warimbi Schist; adjoin and probably pass laterally into Mount Stafford beds (q.v.)|16-MAY-23
29263|Lander Rock beds|Age reasons|Older than 1642 +/- 100 m.y. Rb-Sr date on Anmatjira Orthogneiss; hence Middle Proterozoic or older.|16-MAY-23
29263|Lander Rock beds|Proposed publication|Stratigraphic definitions in the Arunta Block' - BMR microfiche Report.|16-MAY-23
29263|Lander Rock beds|Defn Reference|80/20787|16-MAY-23
29263|Lander Rock beds|Reserved? Yes/No|Yes|16-MAY-23
24397|Mount Dunkin schist|Name source|Mount Dunkin (5555-011069), in northwest part of Aileron 1:100 000 Sheet area.|16-MAY-23
24397|Mount Dunkin schist|Type section locality|Reference area: Mount Dunkin itself shows excellent exposures of sillimanite schist; copper minerals also present.|16-MAY-23
24397|Mount Dunkin schist|Extent|Immediately south of Woodforde River, northwest part of Aileron 1:100 000 Sheet area.|16-MAY-23
24397|Mount Dunkin schist|Lithology|Mostly sillimanite schist and gneiss, plus smaller amounts of biotite schist; quartzite, and calc-silicate rock.|16-MAY-23
24397|Mount Dunkin schist|Relationships and boundaries|Lies conformably above calc-silicate rock of the Wickstead Creek beds; faulted against Lander Rock beds and Woodforde River beds. Adjoins and probably intruded by two unnamed granites; presumed lateral equivalent to Mount Freeling schist, but separated from it by Wickstead Creek Beds.|16-MAY-23
24397|Mount Dunkin schist|Identifying features|Reason for Proposed Name: Distinct schist unit, different from adjoining calc-silicate and marble units on each side.|16-MAY-23
24397|Mount Dunkin schist|Age reasons|Same general age as Wickstead Creek beds, i.e., early Middle Proterozoic.|16-MAY-23
24397|Mount Dunkin schist|Proposed publication|Commentary on Reynolds Range-Aileron 1:100 000 Sheet Area|16-MAY-23
24397|Mount Dunkin schist|Defn Reference|80/20787|16-MAY-23
24397|Mount Dunkin schist|Proposer|Stewart A.J., Glikson A.Y., Warren R.G.|16-MAY-23
24397|Mount Dunkin schist|Reserved? Yes/No|Yes (as Beds)|16-MAY-23
24399|Mount Freeling schist|Name source|Mount Freeling (55520047020), highest peak in Aileron 1:100 000 Sheet area.|16-MAY-23
24399|Mount Freeling schist|Type section locality|Reference area: at 5552-086000, 1 km north of Anna Reservoir, Aileron 1:100 000 Sheet area; interbedded schist, quartz-rich metasediment, sillimanite schist and gneiss, and quartzite are well exposed on sides of gully cut by stream flowing south into Reservoir.|16-MAY-23
24399|Mount Freeling schist|Extent|Extends east and west of Anna Reservoir for total of 20 km; also small outcrops immediately south of Bluebush Swamp, and 10 km southeast of Aileron.|16-MAY-23
24399|Mount Freeling schist|Lithology|Mainly muscovite-biotite schist, with smaller amounts of quartzite (distinguished on map as separate sub-unit), quartzofeldspathic schist, cordierite granulite and gneiss, quartz-rich metasediment, and sillimanite schist.|16-MAY-23
24399|Mount Freeling schist|Relationships and boundaries|Lies above Wickstead Creek beds with apparent conformity; lies below Lander Rock beds with transitional contact; intruded by small unnamed granites and by Napperby Gneiss; presumed lateral equivalent of Mount Dunkin schist, but separatead from it by Wickstead Creek beds.|16-MAY-23
24399|Mount Freeling schist|Identifying features|Reason for proposed name: Distinct schist and gneiss unit different from surrounding calc-silicate and granitic rocks.|16-MAY-23
24399|Mount Freeling schist|Age reasons|No isotope dates; probably same age as Lander Rock beds, early Middle Proterozoic or older. Older than 1800-1500 m.y. date on Napperby Gneiss (L.P. Black, BMR, pes. comm., 1975).|16-MAY-23
24399|Mount Freeling schist|Proposed publication|Commentary on Reynolds Range-Aileron 1:100 000 Special Map.|16-MAY-23
24399|Mount Freeling schist|Defn Reference|80/20787|16-MAY-23
24399|Mount Freeling schist|Proposer|Stewart A.J., Glikson A.Y.|16-MAY-23
24399|Mount Freeling schist|Reserved? Yes/No|Yes (as Metamorphics)|16-MAY-23
27090|Mount Stafford beds|Name source|Mount Stafford (5453-578634), northwest part of Reynolds Range 1:100 0000 Sheet area.|16-MAY-23
27090|Mount Stafford beds|Unit history|Called 'Archaean interbedded micaceous schists and schistose quartzite' by Australian Geophysical (1967); included in map unit of 'Precambrian schist, quartzite, dolomite, and marble' by Wells & others (1971).|16-MAY-23
27090|Mount Stafford beds|Type section locality|Reference area: Well exposed strike ridges at 5453-510622, 1.2 km east of Tin Bore, northwest part of Reynolds Range 1:100 0000 Sheet area.|16-MAY-23
27090|Mount Stafford beds|Extent|Yundurbulu Range in northwest corner of Reynolds Range 1:100 000 Sheet area and southwest corner of Mount Peake 1:100 000 Sheet area; also in northwest part of Denison 1:100 000 Sheet area.|16-MAY-23
27090|Mount Stafford beds|Lithology|Thin to medium to thick-bedded grey or black layered or spotted hornfelses, typically composed of cordierite, biotite, andalusite, microcline, plagioclase, and quartz. To the northeast, approaching the Anmatjira Orthogneiss, hypersthene, garnet, and sillimanite are also present.|16-MAY-23
27090|Mount Stafford beds|Relationships and boundaries|No underlying or overlying units known; passes laterally into Lander Rock beds in Denison 1:100 000 Sheet area. Intruded by Anmatjira Orthogneiss, by small bodies of unnamed granite, and by metadolerite dykes and sills.|16-MAY-23
27090|Mount Stafford beds|Age reasons|Older than 1642 +/- 100 m.y. Rb-Sr date on Anmatjira Orthogneiss: hence Middle Proterozoic or older.|16-MAY-23
27090|Mount Stafford beds|Proposed publication|Stratigraphic definitions in Arunta Block - BMR Microfiche Report.|16-MAY-23
27090|Mount Stafford beds|Defn Reference|80/20787|16-MAY-23
27090|Mount Stafford beds|Name first published by|Shaw R.D., Warren R.G., 1975|16-MAY-23
24408|Mulga Creek granitic gneiss|Name source|Mulga Creek, a tributary of the Hale River, which flows through Georgina jGap at 23o19'S, 134o28'E in central Alice Springs 1:250 000 Sheet area.|16-MAY-23
24408|Mulga Creek granitic gneiss|Unit history|Previously mapped by Wells & others (1968) as undivided Arunta Complex.|16-MAY-23
24408|Mulga Creek granitic gneiss|Type section locality|Reference area: at GR 5751-406149 just west of its boundary with the Georgina Gap granitic gneiss.|16-MAY-23
24408|Mulga Creek granitic gneiss|Extent|The unit forms a small low plateau between the main quartzite range of Mount Laughlen and Mulga Creek.|16-MAY-23
24408|Mulga Creek granitic gneiss|Lithology|A chemically analysed granitic gneiss containing biotite and muscovite has the composition of a granite (specimen 5081). The unit includes the enclosed amphibolite. More details on lithology are given in Shaw & others (in preparation b).|16-MAY-23
24408|Mulga Creek granitic gneiss|Relationships and boundaries|Has a discordant, possibly intrusive, contact with unassigned gneiss and amphibolite (oC). It is intruded by the Georgina Gap granitic gneiss, and is conformably overlain by the Heavitree Quartzite.|16-MAY-23
24408|Mulga Creek granitic gneiss|Age reasons|Middle Proterozoic or older. No isotopic dates.|16-MAY-23
24408|Mulga Creek granitic gneiss|Proposed publication|Stewart & others, in prep.|16-MAY-23
24408|Mulga Creek granitic gneiss|Comments|Remarks: The foliation in the gneiss is thought to post-date the time of inferred intrusion of the Mulga Creek body. The unit is distinguished from the Georgina jGap granitic gneiss by its fine-grainsize and lack of potassium feldspar megacrysts.|16-MAY-23
24408|Mulga Creek granitic gneiss|Defn approved by|Branch C.T., Brown M. (per V. Passmore)|16-MAY-23
24408|Mulga Creek granitic gneiss|Defn Reference|80/20787|16-MAY-23
24408|Mulga Creek granitic gneiss|Proposer|Shaw R.D. (in Shaw & others, in preparation)|16-MAY-23
13613|Musselbrook Formation|Name source|From Musselbrook Creek, whose headwaters drain the area underlain by the formation in the Carrara 1:100 000 Sheet area (Sheet 6460), Northern Territory.|16-MAY-23
13613|Musselbrook Formation|Unit history|Smith & Roberts (1963) previously included the lower, sandstone-rich portion of the formation in their Carrara Range Formation, and the upper siltstone/chert-rich portion in their Bluff Range Beds.|16-MAY-23
13613|Musselbrook Formation|Type section locality|In northeastern Mitchiebo 1:100 000 Sheet area, it exteands from GR 603386 (base) to GR 602420 (top). The section is 1320 m thick.|16-MAY-23
13613|Musselbrook Formation|Extent|A series of faulted outcrops in the northeastern Mitchiebo and central-northern Carrara 1:100 000 Sheet areas; total outcrop area is about 400 km2.|16-MAY-23
13613|Musselbrook Formation|Lithology|Interbedded sandstone, siltstone and chert; minor conglomerate. The chert may be silicified dolomite. The proportion of sandstone decreases, and siltstone and chert increase, upwards.|16-MAY-23
13613|Musselbrook Formation|Relationships and boundaries|The Musselbrook Formation is the basal unit of the McNamara Group in the Carrara Range Region. It overlies Top Rocky Rhyolite disconformably in the Carrara Range. Northwest of the range it overlies Mitchiebo Volcanics with slight angular unconformity. It is overlain conformably by the Plain Creek Formation.|16-MAY-23
13613|Musselbrook Formation|Age reasons|Proterozoic, Carpentarian - correlated with sequences of known Carpentarian age by Plumb & Derrick (1975) and Hutton & Sweet (1982, in press).|16-MAY-23
13613|Musselbrook Formation|Proposed publication|BMR Report 242|16-MAY-23
13613|Musselbrook Formation|Comments|Discussion: The formation records the beginning of a major episode of sandstone-siltstone-carbonate deposition which has been recognised in the Lawn Hill (Sweet & Hutton, 1982) and Hedleys Creek (Sweet, Mock & Mitchell, 1981) regions where it is known as the McNamara and Fickling Groups respectively. Consideration was given to dividing the Musselbrook Formation, as defined above, into a lower sandstone siltstone unit and an upper sandstone/siltstone/chert unit, but this was rejected because (a0 the unit is of mixed lithology throughout, and it would have been difficult to nominate a satisfactory stratigraphic level for the boundary; and (b) the unit as it stands seems to constitute a natural cycle, perhaps reflecting a gradual lessening of relief and teactonic activity (i.e. increasing stability), in both source area and sedimentary basin.|16-MAY-23
13613|Musselbrook Formation|Defn approved by|Brakel A.T. (subject to Hutton & Sweet reference details being entered when available)|16-MAY-23
13613|Musselbrook Formation|Defn Reference|83/23538|16-MAY-23
13613|Musselbrook Formation|Proposer|Sweet I.|16-MAY-23
27515|Myra Falls Metamorphics|Name source|The name was first introduced by Dunn (1962) to describe metamorphic rocks in the Oenpelli area thought to be Archaean. Needham & others (1974) determined an Early Proterozoic age for them and placed them either in the Early Proterozoic sequence or, in areas of higher metamorphic grade and where original stratigraphy could not be determined, in the Nimbuwah Complex which was interpreted as a mantled gneiss dome with an anatectic core. Subsequently (Needham, 1984), the central parts of the Nimbuwah Complex were recognised to be meta-igneous, and the term Nimbuwah Complex has been retained to describe these rocks. The surrounding parts of the complex (Transitional and Lit-par-lit Gneiss Zones) have been reinstated as Myra Falls Metamorphics, to distinguish their metasedimentary origin. |16-MAY-23
27515|Myra Falls Metamorphics|Type section locality|Bed of Tin Camp Creek 1 to 2 km west of crossing of Nabarlek to GR AMG KG116229 (latitude 12o27'S, longitude 13o16'E).|16-MAY-23
27515|Myra Falls Metamorphics|Extent|North, east and southeast of Oenpelli, between Murgenella Creek in the north, Goomadeer River in the east, and the southern edge of the Myra Falls Inlier in the south (Needham & Stuart-Smith, 1984).|16-MAY-23
27515|Myra Falls Metamorphics|Thickness range|Indeterminate; formation involved metamorphism of at least 2-4 km of stratigraphic sequence.|16-MAY-23
27515|Myra Falls Metamorphics|Lithology|Interbanded quartz-feldspar-biotite-muscovite schist and gneiss, +/- garnet and amphibole, leucogneiss, feldspathic and micaceous quartzite. Range from finely to coarsely banded, commonly with quartz-feldspar rich pods or bands.|16-MAY-23
27515|Myra Falls Metamorphics|Relationships and boundaries|Unconformably overlain by Kombolgie Formation. Intruded by unmetamorphosed Oenpelli Dolerite, and by amphibolite of the Zamu Dolerite which has undergone the same amphibolite facies metamorphism and complex deformation. In places contains 'resisters' of Cahill Formation and Kakadu Group, indicating the dominant parent sedimentary units to the metamorphics. Gradational contact with Nourlangie Schist to west, which is differentiated by its relative homogeneity (mica quartz schist) and absence of differentiated quartz-feldspar bands.|16-MAY-23
27515|Myra Falls Metamorphics|Age reasons|Early Proterozoic. Formed by metamorphism of Early Proterozoic metasediments at about 1800 Ma (Page & others, 1980).|16-MAY-23
27515|Myra Falls Metamorphics|Proposed publication|Needham; 1984 - Nabarlek region NT.  BMR Map Commentary|16-MAY-23
27515|Myra Falls Metamorphics|Status|1|16-MAY-23
29226|Nolans Dam metamorphics|Name source|Nolans Dam (5552-218991), north-central part of Aileron 1:100 0000 Sheet area.|16-MAY-23
29226|Nolans Dam metamorphics|Type section locality|Reference Area: Area of hills and gullies at 5552-248955, 5 km west of Aileron; here, cordierite gneiss contains garnet and is layered.|16-MAY-23
29226|Nolans Dam metamorphics|Extent|Between Nolans Dam and Bluebush Swamp, in northern part of Aileron 1:100 000 Sheet area.|16-MAY-23
29226|Nolans Dam metamorphics|Lithology|Largely cordierite gneiss (cordierite, andalusite, garnet, biotite, plagioclase, orthoclase, quartz), with lens of quartzofeldspathic gneiss 400 m x 5 km as separate mapped subunit; small amounts of garnet-biotite gneiss, sillimanite gneiss, muscovite schist, quartzite, and retrogressively metamorphosed rock accompany the cordierite gneiss.|16-MAY-23
29226|Nolans Dam metamorphics|Relationships and boundaries|Passes laterally into schist of Lander Rock beds, probably conformably but age relation unknown because of absence of facings; intruded by Napperby Gneiss.|16-MAY-23
29226|Nolans Dam metamorphics|Identifying features|Reason for Proposed Name: Distinctive readily mapped unit different from neighbouring granitic rocks.|16-MAY-23
29226|Nolans Dam metamorphics|Age reasons|Probably same age as Lander Rock beds, I.e. early Middle Proterozoic or older; must be older than 1800-1500 m.y. date on Napperby Gneiss (L P Black, BMR, pers. comm. 1975).|16-MAY-23
29226|Nolans Dam metamorphics|Proposed publication|Commentary on Reynolds Range-Aileron 1:100 0000 Special Map|16-MAY-23
29226|Nolans Dam metamorphics|Defn Reference|80/20787|16-MAY-23
29226|Nolans Dam metamorphics|Proposer|Stewart A.J., Glikson A.Y.|16-MAY-23
29226|Nolans Dam metamorphics|Reserved? Yes/No|Yes|16-MAY-23
24439|Ongeva granulite|Name source|Ongeva Creek, tributary of the Waite River, 23o07'S, 134o35'E, in the Alice Springs 1:250 000 Sheet area.|16-MAY-23
24439|Ongeva granulite|Unit history|Previously mapped by Wells & others (1968) as undivided Arunta Complex.|16-MAY-23
24439|Ongeva granulite|Type section locality|Refereance area: an area of several square kilometres centred on GR 460330.|16-MAY-23
24439|Ongeva granulite|Extent|Central eastern margin of Laughlen 1:100 000 Sheet area, and central western margin of Riddoch 1:100 000 Sheet area.|16-MAY-23
24439|Ongeva granulite|Lithology|Interlayered mafic granulite, felsic granulite, and migmatite with small amounts of cordierite gneiss, garnet gneiss, mafic calc-silicate, and biotite gneiss.|16-MAY-23
24439|Ongeva granulite|Relationships and boundaries|The unit is overlain by Cadney metamorphics and has a complex boundary with unnamed unit pCu. This later boundary is thought to be largely a metamorphosed intrusive contact, much of pCu being considered to be a metamorphosed granite complex. The boundary is further complicated by retrograde metamorphism to the amphibolite facies near and north of the boundary. Relics of original unretrogressed country rock in pCu resemble the Ongeva granulite.|16-MAY-23
24439|Ongeva granulite|Age reasons|Middle Proterozoic or older. Metamorphosed at 1800 m.y. (Black, 1975), and cut by retrograde zones, e.g. Gough Dam Schist Zone, at several times subsequent to that.|16-MAY-23
24439|Ongeva granulite|Proposed publication|Stewart & others, in prep.|16-MAY-23
24439|Ongeva granulite|Defn Reference|80/20787|16-MAY-23
24439|Ongeva granulite|Proposer|Shaw R.D., Warren R.G. Mapped by A.P. Langworthy and R.D. Shaw (in Shaw & others, in preparation)|16-MAY-23
24442|Oolbra orthogneiss|Name source|Oolbra Dam, 23o20'S, 133o52'E, Alice Springs 1:250 000 Sheet.|16-MAY-23
24442|Oolbra orthogneiss|Unit history|Previously mapped by Wells & others (1968) as undivided Arunta Complex.|16-MAY-23
24442|Oolbra orthogneiss|Type section locality|Reference area: The type area is a 1 km2 region centred on GR 5651-885229, Burt 1:100 000 Sheet area.|16-MAY-23
24442|Oolbra orthogneiss|Extent|South of the vehicle track between Oolbra Dam and Scrub Hill, in central Burt 1:100 000 Preliminary Sheet area.|16-MAY-23
24442|Oolbra orthogneiss|Lithology|Macroscopically homogeneous granitic gneiss containing conspicuous porphyroblasts of orthoclase (up to 75 mm across) in a matrix of quartz, biotite, plagioclase, garnet, orthoclase, hornblende and opaque minerals. The orthogneiss is markedly schistose.|16-MAY-23
24442|Oolbra orthogneiss|Relationships and boundaries|Intrudes Sliding Rock metamorphics and Narbib granulite, and is cut by Narbib Deformed Zone.|16-MAY-23
24442|Oolbra orthogneiss|Age reasons|Middle Proterozoic or older; possibly same as Anamarra orthogneiss based on their similarity in degree of deformation and metamorphism.|16-MAY-23
24442|Oolbra orthogneiss|Proposed publication|Stewart & others, in prep.|16-MAY-23
24442|Oolbra orthogneiss|Defn Reference|80/20787|16-MAY-23
24442|Oolbra orthogneiss|Proposer|Langworthy A.P. (in Shaw & others, in preparation a)|16-MAY-23
24444|Ooradidgee Subgroup|Name source|Ooradidgee 1:100 000 Sheet area (sheet 5857), Bonney Well 1:250 000 Sheet area.|16-MAY-23
24444|Ooradidgee Subgroup|Unit history|Corresponds to the Lower Hatches Creek Group of Blake & others (1982 - BMR Report 239, 1983 - BMR 83) and Blake & Wyche (1983 - BMR Record 1983/18).|16-MAY-23
24444|Ooradidgee Subgroup|Constituents|Epenarra Volcanics, Edmirringee Volcanics, Rooneys Formation, Kurinelli Sandstone, Taragan Sandstone, Treasure Volcanics, and Mia Mia Volcanics. These formations are partly lateral equivalents of one another, and interfingering relationships between them are common.|16-MAY-23
24444|Ooradidgee Subgroup|Extent|Throughout the Davenport Province - east and central parts of Bonney Well, southwest part of Frew River, northwest part of Elkedra and northeast part of Barrow Creek 1:250 000 Sheet areas.|16-MAY-23
24444|Ooradidgee Subgroup|Thickness range|Variable; maximum probably more than 5000 m.|16-MAY-23
24444|Ooradidgee Subgroup|Lithology|Generally recessive felsic and basaltic volcanic rocks, friable arenite, siltstone and shale, which are commonly cleaved, and ridge-forming quartz arenite, feldspathic/lithic arenite, pebbly arenite and conglomerate.|16-MAY-23
24444|Ooradidgee Subgroup|Relationships and boundaries|Unconformable on Warramunga Group in north; base not seen elsewhere. Overlain conformably and possibly disconformably by, and locally interfingers with, the basal formation (Unimbra Sandstone) of the Wauchope Subgroup of the Hatches Creek Group. Intruded by Devils Marble Granite, Elkedra Granite, unnamed granite, and mainly sill-like bodies of granophyre and dolerite/gabbro. Overlain unconformably by flat-lying Cambrian strata.|16-MAY-23
24444|Ooradidgee Subgroup|Age reasons|Younger than 1870 m.y. - U-Pb zircon age for volcanics in the Warramunga Group unconformably underlying the Ooradidgee Subgroup. Older than about 1640 m.y. - Rb-Sr whole rock approximate age of granite intruding the Ooradidgee Subgroup.|16-MAY-23
24444|Ooradidgee Subgroup|Defn author|Blake D.H., Stewart A.J., Sweet I.P., Wyche S., 1985|16-MAY-23
24444|Ooradidgee Subgroup|Comments|Remarks: The oldest subgroup of the Hatches Creek Group. Unlike the two younger subgroups of the Hatches Creek Group (Wauchope and Hanlon Subgroups), its constituent formations show an interfingering rather than a layer-cake type of stratigraphy, it has a greater volcanic component, and its sedimentary component is thought to be predominantly fluvial, rather than mixed fluvial and marine (Wauchope Subgroup) or entirely marine (Hanlon Subgroup).|16-MAY-23
24444|Ooradidgee Subgroup|Defn Reference|86/25362 (misspelt as Ooradigee)|16-MAY-23
24444|Ooradidgee Subgroup|Proposer|Blake D.H.|16-MAY-23
15001|Pedestal Beds|Name source|Pedestal Hills, 20o35'S, 129o17'E, The Granites 1:250 000 Sheet area NT.|16-MAY-23
15001|Pedestal Beds|Unit history|Previously mapped as undivided Permian and undivided Palaeozoic (Casey & Wells, 1964).|16-MAY-23
15001|Pedestal Beds|Type section locality|Reference area: 5 km east of Macfarlanes Peak Bore, at 20o22'10"S, 129o29'00"E, The Granites 1:250 000 Sheet area. Here 20 m of Sandstone with minor thin siltstone interbeds dips 10-15o south.|16-MAY-23
15001|Pedestal Beds|Extent|Southeast parts of the Lucas and Stansmore 1:250 000 Sheet areas WA, and east part of The Granites 1:250 000 Sheet area, NT.|16-MAY-23
15001|Pedestal Beds|Thickness range|Maximum exposed is about 40 m.|16-MAY-23
15001|Pedestal Beds|Lithology|Mainly medium- to fine-grained, friable, clayey, quartzose sandstone; minor conglomerate, siltstone and shale. Cross-bedding and ripple marks common.|16-MAY-23
15001|Pedestal Beds|Relationships and boundaries|Unconformable on Archaean or Lower Proterozoic Tanami complex, Lower Proterozoic unnamed granite, and probably Adelaidean Redcliff Pound Group. Probably unconformable on Lower Cambrian Antrim Plateau Volcanics and probably Palaeozoic Lucas Formation.|16-MAY-23
15001|Pedestal Beds|Age reasons|Probably Palaeozoic|16-MAY-23
15001|Pedestal Beds|Defn approved by|Taken from xerox copy of approved def. Sent by WA Sub-Committee|16-MAY-23
15001|Pedestal Beds|Name first published by|Blake D.H., Hodgson I.M., Walton D.G., 1976|16-MAY-23
27540|Point Wakefield Beds|Name source|Point Wakefield, latitude 19o59'S, longitude 133o21'E, Green Swamp Well 1:250 000 Sheet area SE 53-13.|16-MAY-23
27540|Point Wakefield Beds|Unit history|Included in Chewings' (1931) Winnecke Creek Tableland Formation. Milligan, Smith, Nichols and Doutch (1966) included these Beds in the Merrina Beds.|16-MAY-23
27540|Point Wakefield Beds|Type section locality|Reference Section: In BMR Green Swamp Well 1, latitude 19o25'S, longitude 133o30'E; from 0.7 to 25.9 m. Brown and white claystone, calcareous in parts, silty in parts, is the dominant lithology, with a few chert beds (possibly resulting from weathering).|16-MAY-23
27540|Point Wakefield Beds|Extent|Poorly exposed in low rises in north part of the Green Swamp Well 1:250 000 Sheet area SE 53-13, and the South Lake Woods 1:250 000 Sheet area SE 53-9. May extend as belt about 25 km wide around northern part of Lander Trough, concealed beneath Cainozoic deposits including extensive calcrete deposits on Bonney Well SF 53-2, Green Swamp Well SE 53-13 and Tanami East SE 52-16 1:250 000 Sheet areas. Its extent in the north Wiso Basin, and in the Lander Trough, where it is concealed by younger sediments is not known.|16-MAY-23
27540|Point Wakefield Beds|Thickness range|Maximum recorded thickness is 37.5 m in BMR Barrow Creek 18 (GRG18) stratigraphic drillhole, latitude 21o9'S, longitude 145o11'E (Milligan, 1963). Thickness is 26.2 m in currings from Green Swamp Well 3 stratigraphic drillhole, latitude 19o20'S, longitude 133o03'E (Kennewell & Huleatt, in prep.). Greatest recorded thickness in outcrop is 22 metres at Point Wakefield. Total thickness of the Point Wakefield Beds is probably much greater than thicknesses recorded here.|16-MAY-23
27540|Point Wakefield Beds|Lithology|Claystone, calcareous in many places, white to brown, soft to hard, chalcedonic in parts, silty in party, may contain sand grains; sandstone, red to white, generally fine grained, angular, well sorted, typically ;micaceous, bioturbated in parts, low angle cross-bedding in parts; siltstone, red-brown, sandy in parts, micaceous; claystone, red-brown and white, silty laminae in parts, typically laminated, bioturbated, and micaceous; 2 m of conglomerate, possibly a basal conglomerate, crops out at latitude 18o22'S, longitude 132o57'E.|16-MAY-23
27540|Point Wakefield Beds|Relationships and boundaries|Cuttings from stratigraphic drill holes BMR Green Swamp Well 1, 2 and 3, at latitude 19o25'S, longitude 133o30'E; latitude 19o24'S, longitude 133o16'E and latitude 19o20'S, longitude 133o03'E respectively (Kennewell & Huleatt, in prep.), show the Point Wakefield Beds overlying the Montejinni Limestone, the Hooker Creek Formation and the Lothari Hill Sandstone respectively (Kennewell & Huleatt, in prep.). In the South Lake Woods Sheet area the Beds overlie the Proterozoic Tomkinson Creek Group. Hence the basal contact is unconformable. At Point Wakefield astronomical station, latitude 19o59'S, longitude 133o21'E, sandstone, possibly of the Hanson River Beds, overlies the Point Wakefield Beds, but the contact is not exposed and its nature is not known. Elsewhere the Buchanan Hills Beds, or Cainozoic rock units overlie the Beds.|16-MAY-23
27540|Point Wakefield Beds|Age reasons|The stratigraphic position of the Beds indicates an age between the limits lower Middle Cambrian (Ordian) and Lower Ordovician (Arenig). White silty claystone of the point Wakefield Beds at locality, latitude 19o20'S, longitude 133o37'E, contains ptychopariid trilobites from which a Templetonian (lower Middle Cambrian) age has been determined (P Jell, University of Qld, pers. comm., 1976). A brachiopod recovered from the Point Wakefield Beds in BMR Barrow Creek 18 (GRG 18) was recognised by Dr A.A. Opik as having a structure characteristic of an age no older than Upper Cambrian (Milligan, 1963). The Point Wakefield Beds hence range in age at least from lower Middle Cambrian (Templetonian) to Upper Cambrian.|16-MAY-23
27540|Point Wakefield Beds|Proposed publication|Bureau of Mineral Resources Bulletin|16-MAY-23
27540|Point Wakefield Beds|Comments|Notes: The term "Beds" is proposed for this rock unit, as it commonly crops out as thin deposits preserved in topographically higher areas, and its lateral continuity is difficult to prove, particularly as fossils have been found only at one locality. It is postulated that calcareous claystone is a major component of the beds but does not crop out due to its soft nature; when incised, this lithology develops a thin capping of calcrete. Two distinct rock units may be present in the Point Wakefield Beds; an upper sandstone, siltstone and claystone sequence typified by outcrops at Point Wakefield, and a lower calcareous siltstone sequence which is commonly capped by calcrete.|16-MAY-23
27540|Point Wakefield Beds|References|01/31588; B205; 63/086; 66/047.|16-MAY-23
27540|Point Wakefield Beds|Unit name|Point Wakefield Beds (new name)|16-MAY-23
24465|Quartz Knob Metamorphics|Name source|The geographic feature marked as Quartz Knob at 130o29'30"E, 13o51'42"S in the Greenwood 1:100 000 Sheet area.|16-MAY-23
24465|Quartz Knob Metamorphics|Type section locality|An area of 35 km2 being a rectangle with its northeastern corner at 130o33'57"E, 13o54'18"S. The northern side runs 5 km due west from the above locality and the eastern side 7 km due south. The area encompasses most of the following reference localities: Mafics:- A hillock at 130o34'20"E, 13o51'54"S and boulder piles around 130o32'28"E, 13o50'17"S. A further reference locality at 130o35'08"E, 13o51'58"S typifies the unretrogressed, two pyroxene granulite.  Schists:- Predominately coherently banded schist well exposed around a creek junction at 130o33'57"E, 13o54'18"S and more massive schists, and well developed younger deformational events in a low hill at 130o33'18"E, 13o55'59"S with an incised creek bed adjacent to the north providing good outcrop.|16-MAY-23
24465|Quartz Knob Metamorphics|Extent|The mafics are exposed in a broad band to the east and up to 17 km southeast of Hermit Hill. The banded schists occur in 4-5 km wide zones to the south and southeast of the mafics and to the west. These areas trend north and northeast from Ti-Tree Creek. Total extent is unknown.|16-MAY-23
24465|Quartz Knob Metamorphics|Lithology|The mafic unit is a dark, fine grained, lightly banded mafic gneiss. The banding is alternating plagioclase-hornblende and actionolite-cummingtonite. Rare outcrops contain two pyroxenes rather than the actinolite-cummingtonite bands and are massive in appearance. The schists are banded, fine grained, retrogressed gneisses, essentially quartz-mica schists. Banding consists of quartz rich bedding remnants, intensely deformed, quartz veins, and sericitised quartzofeldspathic bands. There is evidence for at least five deformational events the youngest of which forms crenulations and small scale folds locally. The prograde metamorphism appears to have accompanied a transpositional event, followed by retrogression and further intense deformation. The complex deformational history, including a transpositional event, renders any assessment of the thickness of the unit quite impossible. For similar reasons it is difficult to assess the original relationship between the mafic and pelitic members. However, it is considered likely that the mafics were basalts or dolerites partially interlayered with and under- or overlying sediments. Macroscopic pods of mafic rock occur within the schists and vice versa lending limited support to this interpretation although the deformational history could allow for this to have occurred tectonically. This unit is distinguished from the Hermit Creek Metamorphics for three main reasons: 1) A much more complicated deformational history (at least five deformational events compared to two);  2) Metamorphism to very high grades and subsequent retrogression; and 3) A lack of coherently preserved primary igneous or sedimentary structures.|16-MAY-23
24465|Quartz Knob Metamorphics|Relationships and boundaries|The Quartz Knob Metamorphics are intruded by the Buffallo Fly Hill granodiorite (informal name of 1,840 ma granitoid) and faulted against the Hermit Creek Metamorphics.|16-MAY-23
24465|Quartz Knob Metamorphics|Age reasons|The Quartz Knob Metamorphics are intruded by a relatively undeformed Buffallo Fly Hill granodiorite whilst they are intensely deformed, suggesting that they are considerably older than late lower Proterozoic. They are thought to be Archaean by Hammond and others (in prep., the Litchfield Complex, northwest Northern Territory; Archaean basement or Proterozoic cover?, Aust. J.E. Sci.).|16-MAY-23
24465|Quartz Knob Metamorphics|Proposed publication|Australian Journal of Earth Science|16-MAY-23
24465|Quartz Knob Metamorphics|Proposer|Hammond R.L., Nisbet B.W., Etheridge M.A., Wall V.J.|16-MAY-23
27544|Queenie Flat Granite|Name source|After Queenie Flat Dam (GR 478E, 7478N, AMG metric) in east-northeast of outcrop area. Queenie Flat Dam is just off the road to 'New Macdonald Downs' in the southeast of the Alcoota 1:250 000 Sheet area, SF 53-10, Australian map Grid.|16-MAY-23
27544|Queenie Flat Granite|Type section locality|South of Queenie Flat Dam (about 0.5 km) in low hills.|16-MAY-23
27544|Queenie Flat Granite|Description at type locality|Gneissic granite consisting of pink microcline phenocrysts in a dark grey gneiss.|16-MAY-23
27544|Queenie Flat Granite|Extent|Near Queenie Flat Dam|16-MAY-23
27544|Queenie Flat Granite|Lithology|Porphyritic biotite gneissic, adamellite; rare granite.|16-MAY-23
27544|Queenie Flat Granite|Relationships and boundaries|Very irregular intrusive contact with sub-unit 3 of the Harts Range Group.|16-MAY-23
27544|Queenie Flat Granite|Proposed publication|BMR Report|16-MAY-23
27544|Queenie Flat Granite|Comments|Lake Mount Swan Granite but with smaller and less euhedral phenocrysts.|16-MAY-23
27544|Queenie Flat Granite|Name first published by|Shaw R.D., Warren R.G., Kopras J., Green D.E., 1975|16-MAY-23
27544|Queenie Flat Granite|Unit name|Queenie Flat Granite (Pgf)|16-MAY-23
15826|Randall Peak metamorphics|Name source|Randall Peak Bore 23o23'S, 134o11'E, Alice Springs 1:250 000 Sheet area. Also after Randall's Peak GR 5751-142097.|16-MAY-23
15826|Randall Peak metamorphics|Unit history|Previously mapped by Wells & others (1968) as undivided.|16-MAY-23
15826|Randall Peak metamorphics|Type section locality|Reference area: From Porters Well (GR 5751-221093) for about 4 km farther to the southeast.|16-MAY-23
15826|Randall Peak metamorphics|Extent|Complex arcuate pattern of ridges in the southern part of Laughlen and northern part of Undoolya 1:100 000 Sheet areas.|16-MAY-23
15826|Randall Peak metamorphics|Lithology|Quartzofeldspathic gneiss, amphibolite, biotite gneiss, and subordinate muscovite-biotite gneiss. Other minor rock types include hornblende gneiss, sillimanite gneiss, and megacrystic feldspar gneiss. More details on lithology are given in Shaw & others (in preparation).|16-MAY-23
15826|Randall Peak metamorphics|Relationships and boundaries|The surrounding rocks are dominantly biotite gneisses (C.I. 12), which lack the quartzofeldspathic gneiss layers (C.I. 12) which characterise the Randall Peak metamorphics. The unit is surrounded, for the most part, by unassigned biotite gneisses (pC). Based on meagre foliation-dip information, the metamorphcis consistently dip underneath the unit pC and may be older. The Trephina granitic gneiss has discordant contacts against the Randall Peak metamorphics and encloses a raft of the metamorphics. The Jennings Granitic Gneiss has some conformable contacts and some discordant contacts with the metamorphics. The metamorphics are intruded by a number of small gabbroic plugs, and unconformably overlain by the Heavitree Quartzite.|16-MAY-23
15826|Randall Peak metamorphics|Age reasons|Middle Proterozoic or older. No isotopic dates.|16-MAY-23
15826|Randall Peak metamorphics|Proposed publication|Stewart & others, in prep.|16-MAY-23
15826|Randall Peak metamorphics|References|Branch C.T., Brown M.|16-MAY-23
15826|Randall Peak metamorphics|Defn Reference|80/20787|16-MAY-23
24483|Sadadeen Range gneiss|Name source|Sadadeen Range in Alice Springs 1:100 000 Sheet area; GR 5650-865775.|16-MAY-23
24483|Sadadeen Range gneiss|Type section locality|Sadadeen Range; GR 5650-865775|16-MAY-23
24483|Sadadeen Range gneiss|Extent|Crops out east and west of Alice Springs for about 11 km.|16-MAY-23
24483|Sadadeen Range gneiss|Lithology|Orthogneiss; megacrysts of perthitic microcline in a schistose matrix.|16-MAY-23
24483|Sadadeen Range gneiss|Relationships and boundaries|Concordant contact with unnamed metasediments, calc-silicate rocks, Emily Gap schist (new name), and Alice Springs Granite (new name); interlayered with the Teppa Hill metamorphics (new name); non-conformably overlain by the Simpsons Gap Metasediments (new name) and the Heavitree Quartzite. Dolerite dykes from the Stuart Dyke Swarm (new name) intrude the Sadadeen Range gneiss.|16-MAY-23
24483|Sadadeen Range gneiss|Identifying features|Reason for proposed name: Distinctive unit of orthogneiss enveloping metasedimentary units.|16-MAY-23
24483|Sadadeen Range gneiss|Age reasons|Older than the Late Proterozoic Heavitree Quartzite which unconformably overlies, and the dolerite dykes which intrude the Sadadeen Range gneiss. Recrystallisation and metamorphic fabric may have developed during the regional Chewings Phase of deformation which in Hermannsburg 1:100 0000 Sheet area to the west has been dated by total-rock Rb-Sr at 1620 +/- 70 m.y.|16-MAY-23
24483|Sadadeen Range gneiss|Proposed publication|Geological report on 1:100 0000 scale mapping of southeastern Arunta Block, Alice Springs 1:250 000 Sheet area, Northern Territory, by R D Shaw et al.  BMR Microfiche report in prep.|16-MAY-23
24483|Sadadeen Range gneiss|Defn Reference|80/20787|16-MAY-23
24483|Sadadeen Range gneiss|Proposer|Offe L.A.|16-MAY-23
24483|Sadadeen Range gneiss|Resdate|03-NOV-1975|16-MAY-23
24483|Sadadeen Range gneiss|Reserved? Yes/No|Yes|16-MAY-23
24497|Sliding Rock metamorphics|Name source|Sliding Rock Well at 23o19'S, 134o13'E in the Alice Springs 1:250 000 Sheet area.|16-MAY-23
24497|Sliding Rock metamorphics|Unit history|Previously mapped as undivided Arunta Complex by Wells & others (1968).|16-MAY-23
24497|Sliding Rock metamorphics|Type section locality|Reference area: On the eastern side of the track from Sliding Rock Well to Randall Peak Bore, I.e. between GR 5751-193207 and 5751-178185, Laughlen 1:100 000 Sheet area.|16-MAY-23
24497|Sliding Rock metamorphics|Extent|A series of broad east-striking ridges which parallel Harry Creek to the north and extend from the headwaters at White Tree Creek in the Burt 1:100 000 Sheet area to Turner's Prospect in the Laughlen 1:100 000 Sheet area.|16-MAY-23
24497|Sliding Rock metamorphics|Lithology|A sequence of hornblende-biotite gneiss, garnet-biotite gneiss, biotite gneiss, quartzofeldspathic gneiss, and amphibolite. Granitic gneiss and rare kyanite gneiss are confined to the western end of the outcrop. Sillimanite gneiss is confined to the southern margin of the unit and to the inferred contact with the Ankala gneiss in the northeast of the unit of Rankin's Prospect. More details on lithology are given in Shaw & others (in preparation).|16-MAY-23
24497|Sliding Rock metamorphics|Relationships and boundaries|The southern boundary of the unit is conformable against unassigned rocks (pC) and is marked by the outgoing of garnetiferous biotite gneiss and an increase in the biotite content of the gneiss giving rise to rocks that have a relatively high colour index (CI   20). At the northeastern end of the unit the southern margin is intruded by the Oolbra orthogneiss. The northern margin is faulted against the Ankala gneiss for most of its length. At Rankin's Prospect the metamorphics are conformably overlain by a thin unit of schist, marble, calc-silicate rock, and magnetite quartzite followed by a unit of mainly quartzofeldspathic gneiss; both units are tentatively assigned to the Ankala gneiss. The common occurrence of either garnet or hornblende in the gneisses of the Sliding Rock metamorphics makes the unit distinctive.|16-MAY-23
24497|Sliding Rock metamorphics|Age reasons|Middle Proterozoic or older. No isotopic dates.|16-MAY-23
24497|Sliding Rock metamorphics|Proposed publication|Stewart & others, 1980|16-MAY-23
24497|Sliding Rock metamorphics|Defn Reference|80/20787|16-MAY-23
24497|Sliding Rock metamorphics|Proposer|Shaw R.D. (in Shaw & others, in preparation)|16-MAY-23
17445|Stuart Dyke Swarm|Name source|Stuart Highway, the main road extending north and south of Alice Springs.|16-MAY-23
17445|Stuart Dyke Swarm|Type section locality|Typical dykes of this Swarm can be seen 22 km west-southwest of Alice Springs along the Larapinta Road (in the Alice Springs 1:100 000 Sheet area).|16-MAY-23
17445|Stuart Dyke Swarm|Extent|Throughout the southern part of the Arunta Block.|16-MAY-23
17445|Stuart Dyke Swarm|Lithology|Clinopyroxene and plagioclase; varying amounts of olivine, hornblende and biotite. Commonly ophitic to sub-ophitic texture preserved although dykes may be altered to greenschist facies assemblages.|16-MAY-23
17445|Stuart Dyke Swarm|Relationships and boundaries|In southern Arunta the dykes intrude all basement units. Unconformably overlain by the Heavitree Quartzite.|16-MAY-23
17445|Stuart Dyke Swarm|Age reasons|Older than unconformably overlying Late Proterozoic Heavitree Quartzite. Preliminary dating indicates an age not younger than 910 m.y. and not older than 1050 m.y.|16-MAY-23
17445|Stuart Dyke Swarm|Proposed publication|Geological report on the 1:100 0000 scale mapping of southeastern Arunta Block, Alice Springs 1:250 000 Sheet area, Northern Territory by R.D. Shaw et al. BMR Microfiche report in prep.|16-MAY-23
17445|Stuart Dyke Swarm|Comments|Reason for proposed name: Distinctive set of fairly fresh dolerite dykes which commonly trend north-south.|16-MAY-23
24516|Teppa Hill metamorphics|Name source|Teppa Hill; GR 5650-850795 in Alice Springs 1:100 000 Sheet area.|16-MAY-23
24516|Teppa Hill metamorphics|Type section locality|From GR5650-818783 to 826792 in Alice Springs 1:100 000 Sheet area.|16-MAY-23
24516|Teppa Hill metamorphics|Extent|Crop out in an arc extending from a few km northwest of Alice Springs to the township itself (Alice Springs 1:100 000 Sheet area).|16-MAY-23
24516|Teppa Hill metamorphics|Lithology|Mainly composed of metasediments; interlayered muscovite-biotite quartzose gneiss, metaquartzite, biotite-muscovite schist and a small amount of calc-silicate rock. Small amount of amphibolite; orthogneiss at the margin of the unit.|16-MAY-23
24516|Teppa Hill metamorphics|Relationships and boundaries|Apparent concordant contact with the Sadadeen Range gneiss to the east, northeast, west and southwest. Southeast boundary outlined by interfingering of Teppa Hill metamorphics and Sadadeen Range gneiss. The concordant contact (mentioned above) in detail consists of intimately interlayered metasediment and orthogneiss; for practical purposes the boundary between the orthogneiss of the Sadadeen Range gneiss and the metasediment has been placed such that, by definition, the Teppa Hill metamorphics include the minor portion of the orthogneiss which is intimately interlayered with metasediment. Dolerite of the Stuart Dyke Swarm (new name) intrudes the Teppa Hill metamorphics.|16-MAY-23
24516|Teppa Hill metamorphics|Identifying features|Reason for proposed name: Metamorphosed sediments, amphibolite and some marginal orthogneiss within orthogneiss of the Sadadeen Range gneiss (new name) i.e. distinct group of rocks within a fairly homogeneous orthogneiss.|16-MAY-23
24516|Teppa Hill metamorphics|Age reasons|Thought to be metamorphosed during the Chewing Phase of deformation at about 1620 +/- 70 m.y. Known to be older than the Late Proterozoic dolerite dykes which intrude them.|16-MAY-23
24516|Teppa Hill metamorphics|Proposed publication|Geological report on 1:100 000 scale mapping of Southeastern Arunta Block, Alice Springs 1:250 000 Sheet area Northern Territory by R.D. Shaw et al. BMR Microfiche report in prep.|16-MAY-23
24516|Teppa Hill metamorphics|Defn Reference|80/20787|16-MAY-23
24516|Teppa Hill metamorphics|Proposer|Offe L.A.|16-MAY-23
24516|Teppa Hill metamorphics|Resdate|03-NOV-1975|16-MAY-23
24516|Teppa Hill metamorphics|Reserved? Yes/No|Yes|16-MAY-23
28172|Tomkinson Creek Beds|Name source|Tomkinson Creek, Helen Springs 1:250 000 Sheet area.|16-MAY-23
28172|Tomkinson Creek Beds|Unit history|Ashburton Sandstone (Noakes & Traves, 1954); invalid because of prior usage for a Western Australian rock unit. First named the Tomkinson Creek Beds in an unpublished report by Randal, Brown and Doutch (1966); the name was published in Dunnet and Harding (1967). Randal and Brown (1969) defined the Tomkinson Creek Beds, but did not name or define any constituent rock units. Mendum and Tonkin (in prep.) named and defined the constituent formations in the Tennant Creek Sheet area: they are the Hayward Creek Formation with its Blanche Creek Member, the Whittington Range Volcanics, the Morphett Creek Formation, the Short Range Sandstone and the Attack Creek Formation.|16-MAY-23
28172|Tomkinson Creek Beds|Type section locality|The reference area (Randal and Brown, 1969) is the Ashburton Range, including its extension northward from Powell Creek telegraph station to near Newcastle Waters, and the Whittington Range southwest of Banka Banka Homestead. Mendum and Tonkin (in prep.) nominate type section localities for the constituent formations in the Tennant Creek Sheet area.|16-MAY-23
28172|Tomkinson Creek Beds|Extent|Northern part of Tennant Creek 1:250 000 Sheet area, western parts of Helen Springs and Beetaloo 1:250 000 Sheet areas, and eastern parts of Green Swamp Well, South Lake Woods and Newcastle Waters 1:250 000 Sheet areas. The Beds have been mapped in greatest detail in the Whittington, Short and Ashburton Ranges in the Tennant Creek  (Dodson and Gardener, in prep.) and Helen Springs (Randal and Brown, 1969) 1:250 000 Sheet areas.|16-MAY-23
28172|Tomkinson Creek Beds|Thickness range|Randal and Brown (1969) estimated 50 000 to 55 000 feet in the Helen Springs Sheet area, mainly based on measurements from aerial photographs. Dunnet and Harding (1967) found a thickness of at least 11 500 feet in the upper reaches of Gibson Creek in the Hayward Creek 1-Mile Sheet area. Mendum and Tonkin (in prep.) record a maximum thickness of 9100 m in the Tennant Creek 1:250 000 Sheet area.|16-MAY-23
28172|Tomkinson Creek Beds|Lithology|According to Randal and Brown (1969) the Tomkinson Creek Beds in the Helen Springs 1:250 000 Sheet area consist of quartz sandstone, glauconitic sandstone, pebbly sandstone, dolomite, leached carbonate rocks, chert, and minor conglomerate and dolomite breccia. In the Tennant Creek Sheet area Dunnet and Harding (1967), principally in the Mount Woodcock 1-Mile Sheet area, recorded quartz pebble conglomerate, quartz sandstone, feldspathic quartz sandstone and minor shale and sisltstone. Mendum and Tonkin (in prep.) in the Tennant Creek 1:250 000 Sheet area record dominantly cross-bedded and ripple-marked sandstone (orthoquartzite) (about 70%), pebbly sandstone, shale, siltstone and limestone (about 25%) and a thin layer of basalt and minor acid volcanics (about 5%).|16-MAY-23
28172|Tomkinson Creek Beds|Relationships and boundaries|The Tomkinson Creek Beds overlie the Early Proterozoic Warramunga Group with a slight angular unconformity (Dodson and Gardener, in prep.). They are overlain with angular unconformity by the Cambrian Helen Springs Volcanics and Gum Ridge Formation (Dunnet and Harding, 1967).|16-MAY-23
28172|Tomkinson Creek Beds|Age reasons|By assumed correlation with the Hatches Creek Group, late Early Proterozoic to Early Carpentarian (Dodson and Gardener, in prep.).|16-MAY-23
28172|Tomkinson Creek Beds|Proposed publication|See References under Mendum and Tonkin; Dodson and Gardener|16-MAY-23
28172|Tomkinson Creek Beds|Status|1|16-MAY-23
18319|Tomkinson Creek Subgroup|Name source|From Tomkinson Creek which rises in the Ashburton Range east of Muckaty homestead (lat. 18deg37'30"S, long. 133deg53'00"E; GR LU822940).|16-MAY-23
18319|Tomkinson Creek Subgroup|Unit history|Defined as Tomkinson Creek Beds by Randal and Brown (1969) on HELEN SPRINGS.|16-MAY-23
18319|Tomkinson Creek Subgroup|Constituents|Hayward Creek Formation, Morphett Creek Formation, Short Range Sandstone, Attack Creek Formation, and Whittington Range Member (formerly Whittington Range Volcanics) of the Hayward Creek Formation.|16-MAY-23
18319|Tomkinson Creek Subgroup|Extent|Upstanding ridges of Short and Whittington Ranges on north-central and northwestern TENNANT CREEK, and continuation of Whittington Ranges together with Ashburton Ranges on HELEN SPRINGS. Minor exposure of continuation of Ashburton province on GREEN SWAMP  WELL, SOUTH LAKE WOODS, NEWCASTLE WATERS and  BEETALOO.|16-MAY-23
18319|Tomkinson Creek Subgroup|Thickness range|About 6 km is exposed on FLYNN.|16-MAY-23
18319|Tomkinson Creek Subgroup|Lithology|Predominantly a clastic sequence comprising lithic, sublithic and quartz arenites and subordinate siltstone and carbonate rocks (both limestone and dolostone); intermediate volcanic rocks particularly associated with Hayward Creek Formation.|16-MAY-23
18319|Tomkinson Creek Subgroup|Relationships and boundaries|Conformable, transitional (e.g., lat. 19deg17'00"S, long. 133deg52'00"E; GR LU809674), locally erosional (e.g., lat. 19deg08'00"S, long. 134deg09'00"E; GR MU106842) or faulted (e.g., lat. 19deg13'00"S, long. 134deg09'00"E; GR MU107750) contact with underlying Flynn Subgroup. Unconformably overlain by probable Neoproterozoic - Cambrian Helen Springs Volcanics, Cambrian Gum Ridge Formation and Cretaceous sedimentary rocks.|16-MAY-23
18319|Tomkinson Creek Subgroup|Structure and Metamorphism|Moderately to steeply dipping. Folded into broad domes and basins.|16-MAY-23
18319|Tomkinson Creek Subgroup|Age reasons|Palaeoproterozoic.  Compston  (1994) gives an age of 1784+/-9 Ma as maximum age of sedi­ mentation of the Hayward Creek Formation, the lowermost lithostratigraphic unit of  the  Tomkinson Creek  Subgroup.|16-MAY-23
18319|Tomkinson Creek Subgroup|Correlations|Wauchope Subgroup, and Ooradidgee and Hanlon Subgroups in part, of the Hatches Creek Group.|16-MAY-23
18319|Tomkinson Creek Subgroup|Defn author|Donnellan, N. 1995.|16-MAY-23
24529|Tommys Gap metamorphics|Name source|Tommys Gap (GR 5850-622855), a watergap in Heavitree Quartzite, which is part faulted against, part unconformably above basic volcanics of Tommys Gap metamorphics, Fergusson Range 1:100 0000 Sheet area.|16-MAY-23
24529|Tommys Gap metamorphics|Type section locality|Reference area: 1. Tommys Gap and for 1.5 km north from there; shows good exposures of western area across low hills and gullies. 2. GR5850-802930, 3.5 km east-southeast of Chabbana Waterholes - good exposure of hornblende gneiss of eastern area, as low well exposed hilly terrain. 3. GR 5850-702924, 0.5 km south-southeast of Marmalade Dam - prominent hill of well exposed orthoamphibolite intruded by granite of Atnarpa Igneous Complex.|16-MAY-23
24529|Tommys Gap metamorphics|Extent|Three separate areas in Giles Creek Synform of Arltunga Nappe Complex, northern part of Fergusson Rnage 1:100 000 Sheet area, NT.|16-MAY-23
24529|Tommys Gap metamorphics|Lithology|Three separate areas separated by igneous rocks of Atnarpa Igneous Complex: 1) Eastern area: Layered hornblende gneiss (andesine-hornblende-quartz-accessories).  2) Central aarea: Orthoamphibolite (labradorite-hornblende-clinopyroxene-epidote-sphene-opaques), quartz-rich metasediment (quartz-microcline-chylorite-epidote +/- actinolite), hornblende gneiss, quartzofeldspathic gneiss, biotite gneiss. Last 4 form interlayered sequence west of orthoamphibolite.  3) Western area: Basic metavolcanics (hornblende-oligoclase-quartz-ilmenite-sphene-accessories) with smaller amounts of ?tuffaceous metasiltstone, ferruginous quartzite, calc-silicate rock; quartzite and amphibolite; marble and chlorite schist.|16-MAY-23
24529|Tommys Gap metamorphics|Relationships and boundaries|Rocks older than or basement to Tommys Gap metamorphics are not exposed or recognised. There are no younger rocks in sequence with the Tommys Gap metamorphics. The metamorphics are intruded by granite and hypabyssal members of the Atnarpa Igneous Complex (q.v.) by dykes of ultramafic rocks, by an amphibolite dyke, and by a dolerite plug correlated with the Stuart Dyke Swarm (name not yet submitted - to be submitted by R.D. Shaw). The metamorphics are unconformably overlain by the Upper Proterozoic Heavitree Quartzite.|16-MAY-23
24529|Tommys Gap metamorphics|Identifying features|Reason for proposed name: A distinct assemblage of diverse but closely associated metasedimentary and metavolcanic rocks, very different from adjoinging acid igneous rocks and overlying quartzite.|16-MAY-23
24529|Tommys Gap metamorphics|Age reasons|Time of deposition of parent sediments and of crystallisation of parent dolerite of orthoamphibolite not known, but must be older than Rb-Sr whole-rock isochron age of 1710 +/- 50 m.y. on adjoining Atnarpa Igneous Complex. Using lowest realistic initial 87Sr/86Sr ratio (= .7000) and Rb-Sr data on one whole-rock sample of biotite gneiss, parent sediment for that rock can be no older than 2300 m.y. (Early Proterozoic).|16-MAY-23
24529|Tommys Gap metamorphics|Proposed publication|1. 'Geological report on 1:100 000 scale mapping of southeastern Arunta Block, Alice Springs 1:250 000 Sheet area, Northern Territory' by R.D. Shaw et al. BMR Microfiche Report, in prep. 2. 'Stratigraphic definitions in Arunta Block' - BMR Microfiche Report.|16-MAY-23
24529|Tommys Gap metamorphics|Proposer|Stewart A.J.|16-MAY-23
24529|Tommys Gap metamorphics|Reserved? Yes/No|Yes|16-MAY-23
24548|Utnalanama granulite|Name source|Utnalanama Range, 23o14'S, 134o07'E, in the Alice Springs 1:250 000 Sheet area.|16-MAY-23
24548|Utnalanama granulite|Unit history|Previously mapped as undivided Arunta Complex by Wells & others (1968).|16-MAY-23
24548|Utnalanama granulite|Type section locality|Reference area: At GR 5751-050300, 2 km west-southwest of Johannsen's Phlogopite Mine.|16-MAY-23
24548|Utnalanama granulite|Extent|Southern foothills of Utnalanama Range.|16-MAY-23
24548|Utnalanama granulite|Lithology|Coarse-grained pale to dark grey tonalitic to dioritic granulite with a granular texture (I.e. a granofels). The tonalite phase consists principally of quartz and antiperthitic plagioclase (An40), together with orthopyroxene (10%) and ilmenite (1%). The dioritic to leucogabbroic phase is composed of quartz (10%) antiperthitic plagioclase (An40), orthopyroxene, clinopyroxene, and ilmenite (1%). The unit has undergone extensive retrograde metamorphism.|16-MAY-23
24548|Utnalanama granulite|Relationships and boundaries|Intruded by the Harry Anorthositic Gabbro; overlain by the Erontonga metamorphics which differ from the Utnalanama granulite in consisting of an interlayered sequence of quartzofeldspathic, cordierite and garnet-bearing gneisses. The unit is also intruded by the Johannsen Metagabbro Dyke Swarm, and by numerous intrusive bodies including the Gumtree Granite.|16-MAY-23
24548|Utnalanama granulite|Age reasons|Middle Proterozoic or older. The first ganulite facies metamorphism, which brought about partial melting of the unit, has been dated as 1800 m.y. using 40Ar-39Ar methods (Allen & Stubbs, in preparation).|16-MAY-23
24548|Utnalanama granulite|Proposed publication|Stewart & others, in prep.|16-MAY-23
24548|Utnalanama granulite|Comments|A.R. Allen prefers to use the name 'Utralanama granofels' because of the extent of retrogression and the granofelsic texture typical of the west of the unit. However Utnalanama granolite is preferred to allow consistency with similar units in the region.|16-MAY-23
24548|Utnalanama granulite|Defn Reference|80/20787|16-MAY-23
24548|Utnalanama granulite|Proposer|Shaw R.D., Allen A.R. (in Shaw & others, in prep.)|16-MAY-23
19295|Wallis Siltstone Member|Name source|Wallis Creek, a small tributary of the Nicholson River, which flows into the Gulf of Carpentaria. This creek rises as 137degrees 27' E, 17degrees51' S, 20 miles SSW of Seigals Creek Homestead, NT, and joins the Nicholson River at 137degrees 34' E, 18degees 00' S.|16-MAY-23
19295|Wallis Siltstone Member|Unit history|This member was defined by Roberts (unpubl. MS) and was mapped by Roberts et al. (1963) in the Calvert Hills 1:250 000 Sheet area. It is also present in Mount Drummond, Westmoreland, and Lawn Hill 1:250 000 Sheet areas, but was not delineated on the 1st editions of those sheets.|16-MAY-23
19295|Wallis Siltstone Member|Type section locality|137degrees 40' E, 17degrees 56' S, 4miles WSW of Fish River, Calvert Hills sheet area [from Roberts manuscript, pre-AGD66],  revised to 'a scarp in that general area, at long. 137degrees41' E' by Sweet & Slater (1975). Ahmad & Wygralak (1989), describe this location as '7km WSW of the Fish River-Tin Hole Creek conjunction.|16-MAY-23
19295|Wallis Siltstone Member|Thickness range|The member is 96 m thick [originally 250 ft] at the type section and probably has a similar thickness for about 10 km westwards along strike. It thins rapidly between 10 and 15 km west of the type section, and is absent farther west in the Seigal Sheet area. However, Roberts et al. (1963) mapped the member in the western part of the Calvert Hills Sheet area. East of the type section the member has a constant thickness in an easterly direction, but it thins southwards, and lenses out just south of the southern margin of the Seigal Sheet area. However, a siltstone unit mapped as the Wallis Siltstone Member is present in the Hedleys Creek Sheet area, and is assumed to have been connected to the outcrops to the west before folding, faulting, and erosion.|16-MAY-23
19295|Wallis Siltstone Member|Lithology|The dominant lithologies in the Wallis Siltstone Member are flaggy and fissile greyish-green and reddish brown micaceous siltstone and fine sandstone. In the type section, interbeds of fine micaceous sandstone and glauconitic sandstone are interbedded with siltstone. One kilometre to the east similar thin sandstone beds show ripple laminations, shaly partings, primary current lineations, and skip casts, and thicker sandstone beds show pillow structures. The rock types exposed in the Hedleys Creek Sheet area are identical to those in the type section, and include glauconitic sandstone. The thickness exposed in one section in the southwestern part of the Hedleys Creek Sheet area is 90 m, or almost the same as that in the type section.|16-MAY-23
19295|Wallis Siltstone Member|Relationships and boundaries|The upper and lower contacts of the member are both conformable [with parts of the Constance Sandstone].|16-MAY-23
19295|Wallis Siltstone Member|Identifying features|Local abundant glauconite.|16-MAY-23
19295|Wallis Siltstone Member|Defn author|Roberts, H.G. ~1962 from Techfile E/53-8 [Calvert Hills], with updates from Sweet & Slater (1975), Ahmed & Wygralak (1989)|16-MAY-23
19295|Wallis Siltstone Member|References|ROBERTS, H.G., RHODES, J.M., & YATES, K,R., 1963 - Calvert Hills, Northern Territory - 1:250 000 Geological Series. Bur. Miner. Resour. Aust. explan. Notes SE/53-8.  **SMITH, J.W., & ROBERTS, H.G., 1963 - Mount Drummond, Northern Territory - 1:250 000 Geological Series. Ibid SE/53-12.  **Sweet, I.P., Slater, P.J. 1975. Precambrian geology of the Westmoreland region, northern Australia. Part I: regional setting and cover rocks. BMR Record 1975/88.|16-MAY-23
24554|Wanapi Dolomite Member|Name source|The Aboriginal name for the small group of hills south of the Naburula Hills (Metric Grid Reference for Wanapi Escarpment) (7320:5290-7380:5230).|16-MAY-23
24554|Wanapi Dolomite Member|Type section locality|The type section, WX-2, is located in the eastern part of the Naburula Hills (7385:5337).|16-MAY-23
24554|Wanapi Dolomite Member|Extent|The Wanapi Dolomite Member is found in practically all outcrops of the Mount Doreen Formation. It occurs as far west as Albinia Springs to Naburula Hills in the east. Outcrops are mostly incomplete and sporadic; they are confined to the Mount Doreen 1:250 000 sheet area (SF 52-12).|16-MAY-23
24554|Wanapi Dolomite Member|Thickness range|The member is 3 m thick in the type section in the Naburula Hills.  4.3 m of the member was measured in a nearby section but no estimate of regional variation is possible because of its poor exposure; it appears to maintain this order of thickness in the known exposures.|16-MAY-23
24554|Wanapi Dolomite Member|Lithology|Fine-grained, pink laminated dolomite containing pyrite holomorphs and manganese staining.|16-MAY-23
24554|Wanapi Dolomite Member|Relationships and boundaries|The Wanapi Dolomite Member is conformably overlain by 17 m of red-brown poorly exposed shale of the Newhaven Shale Member and conformably overlies the Mount Davenport Diamictite Member. In places the Wanapi Dolomite Member is overlain with angular unconformity by the Mount Eclipse Sandstone. The Wanapi Dolomite Member occurs near the top of the Mount Doreen Formation.|16-MAY-23
24554|Wanapi Dolomite Member|Identifying features|Reason for proposed name: A prominent, widespread, thin sequence of dolomite occurring in the top of the Mount Doreen Formation which has been described but not previously named.|16-MAY-23
24554|Wanapi Dolomite Member|Age reasons|Adelaidean by lithological similarity and stratigraphic position with dolomite in the Amadeus Basin that lies below earliest Cambrian rocks.|16-MAY-23
24554|Wanapi Dolomite Member|Proposed publication|Geology of the Ngalia Basin.  BMR Bulletin|16-MAY-23
24554|Wanapi Dolomite Member|Defn Reference|83/24047|16-MAY-23
24630|Wangi Basics|Name source|Wangi Homestead; Reynolds River (5071) 1:100 0000 Sheet, AMG 780450 (latitude 13o09'30", longitude 130o38'20").|16-MAY-23
24630|Wangi Basics|Unit history|Includes meta-dolerite on the Daly River (5070) 1:100 000 sheet which was previously mapped as un-named Proterozoic dolerite by White and others (1959). Some of the metabasic rocks previously included in the Hermit Creek Metamorphics (White and others, 1959) are now recognised as Wangi Basics.|16-MAY-23
24630|Wangi Basics|Type section locality|Within the area bounded by AMG 698489 (latitude 13o07'25", longitude 130o34'00"), 698470 (latitude 13o8'20", longitude 130o34'00"), 730489 (latitude 13o07'25", longitude 130o35'40"), 730470 (latitude 13o34'00", longitude 130o38'20") on the Reynolds River (5071) 1:100 000 sheet.|16-MAY-23
24630|Wangi Basics|Extent|Exposed in numerous outcrops throughout the Reynolds River (5071), Daly River (5070), Greenwood (4970), Wingate Mountains (5069), Moyle (4969) 1:100 000 sheets.|16-MAY-23
24630|Wangi Basics|Lithology|Rock types: Metamorphosed basic and ultra-basic igneous rocks; meta-gabbro, -dolerite, -diorite, -pyroxenite, -peridotite, -harzburgite.|16-MAY-23
24630|Wangi Basics|Relationships and boundaries|Intrudes Early Proterozoic Hermit Creek Metamorphics, Early Proterozoic Burrell Creek Formation and Welltree Schists. Intruded by Early Proterozoic granite.|16-MAY-23
24630|Wangi Basics|Age reasons|The above relationships limit the age to late Early Proterozoic.|16-MAY-23
24630|Wangi Basics|Proposed publication|Pietsch G.A., in prep - Explanatory Notes (for) Reynolds River (5071). Northern Territory Geological Survey 1:100 000  Geological Map Series. Northern Territory Government Printer, Darwin.|16-MAY-23
24630|Wangi Basics|Comments|Notes: Not all the above relationships are exhibited at the type area; I.e. intrusion into the Hermit Creek Metamorphics and Burrell Creek Formation.|16-MAY-23
24630|Wangi Basics|Proposer|Fahey J.E., Fahey G.M., Pietsch B.A. (submitted by J E Fahey)|16-MAY-23
27071|Weldon metamorphics|Name source|Mount Weldon (294100E, 7534100N) third-highest peak in Anmatjira Range, Tea Tree 1:100 000 Sheet area. Mount Weldon is composed of Weldon metamorphics.|16-MAY-23
27071|Weldon metamorphics|Type section locality|In bed of Possum Creek at point 293500E, 7538300N, 4 km N of Mt Weldon, in Anmatjira Range, Tea Tree 1:100 000 Sheet area. Excellent exposure of main gneiss and lens of amphibolite, intruded by Anmatjira Orthogneiss.|16-MAY-23
27071|Weldon metamorphics|Extent|SE half of Anmatjira Range in Reynolds Range and Tea Tree 1:100 000 Sheet areas. Also one isolated outcrop mapped 5 km SE of Mt Stafford, in NW part of Anmatjira Range.|16-MAY-23
27071|Weldon metamorphics|Lithology|In type area and throughout main mass of the unit, it is a layered gneiss of pelitic composition (sillimanite-oligoclase-garnet-biotite-orthoclase-cordierite-quartz) plus minor biotite-garnet quartzite +/- clinopyroxene +/- orthopyroxene/- bytownite. Main mass also includes large separately mapped lens of sillimanite-garnet-biotite-cordierite granofels (massive, not layered or foliated). Two other lithological variants form separate bodies in Anmatjira Range: (a) sillimanite-biotite-cordierite-granulite +/- orthoclase +/- quartz +/- spinel; (b) garnet-plagioclase-sillimanite-biotite-orthoclase-cordierite-quartz granulite. Amphibolite forms discrete lenses and layers a few metres in extent, and consist of greenish-brown or brown hornblende + labradorite +/- clinopyroxene +/- orthopyroxene.|16-MAY-23
27071|Weldon metamorphics|Relationships and boundaries|Underlying rocks not known. Adjoins Tyson Creek granulite (q.v.) with apparent conformity, but which one is older is not known (no facings known). Is intruded by Anmatjira Orthogneiss, probably by Aloolya Gneiss (q.v.), and by dolerite dykes. Faulted against Lander Rock beds.|16-MAY-23
27071|Weldon metamorphics|Identifying features|Reason for proposed name: A distinctive unit of several varieties of metapelitic gneiss and granulite, easily recognised and mapped from surrounding rocks.|16-MAY-23
27071|Weldon metamorphics|Age reasons|Neither time of deposition of parent sediments, nor time of their regional metamorphism is known with certainty. Almost certainly metamorphosed at same time as adjoining Tyson Creek granulite, which has given K-Ar date on hornblende = 1650 m.y. Is intruded by Anmatjira Orthogneiss, which has given Rb-Sr whole-rock isochron date of 1642 +/- 100 m.y. (L P Black, BMR pers. comm., 1975). Depositional and metamorphic ages thought to be Early Proterozoic - may be older, but no evidence of that.|16-MAY-23
27071|Weldon metamorphics|Proposed publication|1. 'Geology of NW Arunta Block, NT' - BMR Publication.  2. 'Stratigraphic definitions in Arunta Block' - BMR Microfiche Report.|16-MAY-23
27071|Weldon metamorphics|Comments|Remark: Pelitic composition + presence of impure quartzite + mafic meta=igneous rock, and fault relationship with Lander Rock beds arae consistent with supposition that Weldon metamorphics are deeply metamorphosed Lander Rock beds, now upfaulted.|16-MAY-23
27071|Weldon metamorphics|Defn Reference|80/20787|16-MAY-23
27071|Weldon metamorphics|Proposer|Stewart A.J.|16-MAY-23
27071|Weldon metamorphics|Reserved? Yes/No|As Weldon Gneiss|16-MAY-23
25621|Whittington Range Volcanics|Name source|Whittington Range, Tennant Creek 1:250 000 Sheet area.|16-MAY-23
25621|Whittington Range Volcanics|Type section locality|Near grid reference 407892. The stratigraphic section of this locality starts with 10 m of interbedded quartz sandstone and basalt, overlain by 35 m of coarse-grained basalt and 12 m of micaceous quartz sandstone with some brown micaceous siltstone. This is overlain by 290 m of vesicular and fine-grained basalt, much of it epidotised, with some interbedded flows of white and blue-green spherulitic rhyolite. The basalt is veined with jasper and quartz, and vesicules are filled with chlorite, pumpellyite, calcite, quartz, epidote, jasper and albite.|16-MAY-23
25621|Whittington Range Volcanics|Extent|Six small outcrops in the central southern part of the Whittington Range, and two in the eastern part of the Short Range about 7.5 km northwest of Phillip Creek Station. The volcanics typically form low mesa-like outcrops capped with Tertiary silcrete. Elsewhere, angular rubble on the valley floor consists mostly of quartz sandstone fragments, but also includes pebbles and angular fragments of vein quartz, blue-green rhyolite, epidotised basalt and red jasper.|16-MAY-23
25621|Whittington Range Volcanics|Thickness range|200 to 400 m.|16-MAY-23
25621|Whittington Range Volcanics|Lithology|In outcrop the rock is highly weathered. Fresh rock obtained from diamond drill core consists of coarse-grained weathered basalt (12 m) overlain by micaceous quartz sandstone and red-brown micaceous siltstone (6 m). These sediments are capped by volcanic rocks 30 to 100 m thick; they consist predominantly of highly altered vesicular and non-vesicular basalt, with some interbedded flows of white and blue-green spherulitic rhyolite(?).|16-MAY-23
25621|Whittington Range Volcanics|Relationships and boundaries|Conformably overlies Hayward Creek Formation, and is conformably overlain by the Morphett Creek Formation.|16-MAY-23
25621|Whittington Range Volcanics|Age reasons|By assumed correlation of Tomkinson Creek Beds with Hatches Creek Group, late Early Proterozoic to Early Carpentarian.|16-MAY-23
25621|Whittington Range Volcanics|Proposed publication|See References under Mendum and Tonkin; Dodson and Gardener|16-MAY-23
25621|Whittington Range Volcanics|Name first published by|Stewart A.J., Langworthy A.P., Warren R.G., Offe L.A., Glikson A.Y., Wells A.T., Le Messurier P., Gardener J.E.F., 1976|16-MAY-23
24578|Wingate Group|Name source|The Wingate Mountains 1:100 000 Sheet area.|16-MAY-23
24578|Wingate Group|Relationships and boundaries|Revision of old terms: The Wingate Group essentially encompasses the upper part of the old Finniss River Group within which a major unconformity between the Burrell Creek Formation and the old Chilling Sandstone was found. The Wingate Group therefore contains all the units in the old Finniss River Group that lie above the newly recognised unconformity (Hammond, Nisbet and Etheridge, in prep. A revision of the Finniss River Group. BMR Journal). These units are as follows: the Chilling Creek Formation, the Berinka Volcanics, Meeway Volcanics and the Henschke Breccia. The definitions of these units remain unaltered with the exception of the Chilling Creek Formation. This new group is dominantly made up of the Chilling Creek Formation and its estimated thickness is similar to that for the Chilling Creek Formation; 4500 to 5000 m.|16-MAY-23
24578|Wingate Group|Proposed publication|BMR Journal, Australian Journal of Earth Sciences|16-MAY-23
24578|Wingate Group|Proposer|Hammond R.L. Nisbet B.W., Etheridge M.A., Wall V.J.|16-MAY-23
20459|Wonnadinna Dolomite|Name source|Wonnadinna Waterhole, Field River, Hay River 1:250 000 Sheet area.|16-MAY-23
20459|Wonnadinna Dolomite|Unit history|The dolomite of the Field River Beds of Slmith (1963).|16-MAY-23
20459|Wonnadinna Dolomite|Type section locality|A composite section composed of measured section GEO708, BMR Hay River No. 8 drill hole, and outcrops, 5.3 km N to 4.7 k, NNE of Gnallan-a-gea Bore, Hay River 1:250 000 Sheet area; the thickness of the lower part was measured from aerial photographs (Adam Special 1:100 0000 Geological Sheet). Hay River No. 8 is at grid reference 53KQQ750390; the core is stored in the BMR Core & Cuttings Laboratory, Canberra. GEO708 is at grid reference 53KQQ623455.|16-MAY-23
20459|Wonnadinna Dolomite|Extent|Hay River and Tobermory 1:250 000 Sheet areas.|16-MAY-23
20459|Wonnadinna Dolomite|Thickness range|460 m in the type section, about 450 m on the southern limb of the Desert Syncline (measured from aerial photographs) and a minimum of 380 m north of Boat Hill and in the Keepera Ridges (Tobermory 1:250 000 Sheet area).|16-MAY-23
20459|Wonnadinna Dolomite|Lithology|Purple-brown, red-brown and green-grey dolomite; locally sandy, and with abundant oncolites, and with structures resembling columnar branching stromatolites but not clearly biogenic. Interbedded with rarely outcropping red-brown, purple and green-grey arkose, siltstone and shale, some of which is dolomitic. In the Keepera Ridges and at Limestone Creek boulders of granite occur in the dolomite.|16-MAY-23
20459|Wonnadinna Dolomite|Relationships and boundaries|The lower boundary is considered to be gradational with the Black Stump Arkose (Walter, 1979) and is placed at the base of the first prominent dolomite bed 4.7 km NNE of Gnallan-a-gea Bore. The upper boundary is placed at the base of the lowest pebbly arkose of the Gnallan-a-gea Arkose (Walter, 1979). Regional correlations suggest that the upper boundary is a disconformity, because a slight angular unconformity occurs at this position in the Mopunga Trough, and because of the abrupt change of lithology.|16-MAY-23
20459|Wonnadinna Dolomite|Age reasons|Adelaidean. The unit is correlated with the cap dolomites above the upper of the two major late Proterozoic tillites.|16-MAY-23
20459|Wonnadinna Dolomite|First Reference|79/20074|16-MAY-23
75720|Woolianna Suite|Name source|After Woolianna homestead, Woolianna Road and Woolianna school ca 5 km north of Daly River township, Northern Territory, Pine Creek 1:250 000 mapsheet, Daly River 1:100 000 mapsheet, Litchfield Province, Pine Creek Orogen, Northern Territory.|16-MAY-23
75720|Woolianna Suite|Unit history|Previously known as Wangi Basics, which was first used by Needham and Stuart-Smith (1984) and formally defined in Dundas et al (1987). The name Wangi Basics is abandoned, as it is now known to comprise distinct geochemical groups which are genetically unrelated.|16-MAY-23
75720|Woolianna Suite|Geomorphic expression|Large stock in Moyle and Wingate Mountains 1:100 000 mapsheets and scattered outcrops in Daly River, Greenwood and Reynolds river 1:100 000 mapsheets.|16-MAY-23
75720|Woolianna Suite|Type section locality|Large outcrop exposure on Moyle and Wingate Mountains 1:100 000 mapsheets about 40 km SW of Daly River township. GDA 94 Zone 52L 663172mE 8442583mN). (-14°4'59"S 130°30'41"E)|16-MAY-23
75720|Woolianna Suite|Description at type locality|Forms a large area of outcrop with good exposure. Comprises metamorphosed medium- to coarse-grained, variably altered, equigranular rocks that include gabbro, hypersthene gabbro, micro-gabbro to coarse-grained dolerite.|16-MAY-23
75720|Woolianna Suite|Extent|Has surface exposures in Moyle, Greenwood, Wingate Mountains, Daly River and Reynolds River 1:100 000 mapsheets.|16-MAY-23
75720|Woolianna Suite|General description|Occurs as a large stock covering an area of 28 km2 (Edgoose et al 1989) in Wingate Mountains and Moyle 1:100 000 mapsheets, and also occurs as scattered exposures in Reynolds River, Greenwood and Daly River 1:100 000 mapsheets. Unifying characteristic is distinctive back-arc basin geochemical signature.|16-MAY-23
75720|Woolianna Suite|Thickness range|Thickness for large stock in Wingate Mountains 1:100,000 mapsheet is  about 28 km2 (Edgoose et al 1989)|16-MAY-23
75720|Woolianna Suite|Lithology|In Wingate Mountains 1:100,000 mapsheet, Woolianna Suite comprises metamorphosed medium- to coarse-grained, variably altered, equigranular rocks which include gabbro, hypersthene gabbro, micro-gabbro to coarse-grained dolerite. In Daly River 1:100,000 mapsheet, it comprises metaperidotite, metapyroxenite, metaharzburgite, amphibolite, metadolerite and metabasalt|16-MAY-23
75720|Woolianna Suite|Depositional environment|Genesis: Intrusive rocks related to island-arc/back-arc basin setting.|16-MAY-23
75720|Woolianna Suite|Relationships and boundaries|Field contact relationships between the large stock and surrounding rock units are not known. Edgoose et al (1989) inferred that the stock most likely intruded the nearby Hermit Creek Metamorphics, Burrell Creek Formation and Berinka Volcanics. Mafic xenoliths in the adjacent Murra-Kamangee Granodiorite are thought to be of the Woolianna Suite (former Wangi Basics; Edgoose et al 1989).|16-MAY-23
75720|Woolianna Suite|Identifying features|Woolianna Suite is metamorphosed to amphibolite facies with overprinting greenschist-facies retrogression. It is characterized by a distinctive island-arc (back-arc basin) chemical signature which is most apparent in Daly River 1:100 000 mapsheet (Glass 2007).|16-MAY-23
75720|Woolianna Suite|Structure and Metamorphism|Amphibolite-facies metamorphism with greenschist-facies retrogressive overprint.|16-MAY-23
75720|Woolianna Suite|Age reasons|Not adequately constrained, but believed to be between ca 1860 Ma and ca 1855 Ma (Glass 2010) based on stratigraphic constraints.|16-MAY-23
75720|Woolianna Suite|Correlations|Possible correlative of Tickalara Metamorphics in the Central Zone of the Halls Creek Orogen, Western Australia (Sheppard et al 1999).|16-MAY-23
75720|Woolianna Suite|Alteration and Mineralisation|Localised chlorite and sericite alteration. A minor occurrence of shear-zone-hosted polymetallic Cu-Pb-Zn-Ag veins occurs at MGA94 Zone 52 682030mE 8492161mN (-13°38'1" 130°40'58") in Daly River 1:100 000 mapsheet (Ferenzi 1990, NTGS MODAT database).|16-MAY-23
75720|Woolianna Suite|Geophysical Expression| Large stock on Wingate Mountains 1:100 000 mapsheet has strong magnetic response.|16-MAY-23
75720|Woolianna Suite|Geochemistry| Woolianna Suite rocks are characterised by a distinctive island-arc (back-arc basin) chemical signature (Glass 2007) which is further reinforced by positive ¿Nd isotopic signatures (Glass 2010).|16-MAY-23
75720|Woolianna Suite|Defn author|Glass, L.M. (NTGS),  03-NOV-2010|16-MAY-23
75720|Woolianna Suite|References|**DUNDAS DL, Edgoose CJ, Fahey GM and Fahey JE, 1987. Daly River 1:100 000 Geological Map Series. Northern Territory Geological Survey Explanatory Notes (5070).    **EDGOOSE CJ, Fahey GM and Fahey JE, 1989. Wingate Mountains 1:100 000 Geological Map Series. Northern Territory Geological Survey Explanatory Notes (5069).    **FERENZI PA, 1990. The Daly River Mineral Field. NTGS Technical Report 1990-017, Northern Territory Geological Survey.    **GLASS LM, 2007. Geochemistry of mafic rocks in the Litchfield Province, western Pine Creek Orogen: Evidence for a Palaeoproterozoic arc-related setting and links to the Halls Creek Orogen: in 'Annual Geoscience Exploration Seminar (AGES) 2007. Record of Abstracts.' Northern Territory Geological Survey, Record 2007 001.    **GLASS LM, 2010. Palaeoproterozoic island-arc-related rocks of the Litchfield Province, western Pine Creek Orogen, Northern Territory. Northern Territory Geological Survey, Record 2010-005.    **NEEDHAM RS, Stuart-Smith PG, 1984. Geology of the Pine Creek Geosyncline, Northern Territory, 1:500 000 scale map. Bureau of Mineral Resources, Australian Bureau of Mineral Resources, Canberra. ACT.    **SHEPPARD S, Tyler IM, Griffin TJ and Taylor WR, 1999. Palaeoproterozoic subduction-related and passive margin basalts in the Halls Creek Orogen, northwest Australia. Australian Journal of Earth Sciences 46, 679-690.|16-MAY-23
20556|Woolla Gneiss|Name source|After 'Woola Downs' outstation (GR 3826E, 75448N AMG metric) - closest feature to outcrop area. Outstation is on 'Mount Skinner' Station, northwestern Alcoota 1:250 000 Sheet area, SF 53-10, Australian map Grid.|16-MAY-23
20556|Woolla Gneiss|Type section locality|Along Tea Tree Road from northwest of Mount Solitary (GR 3605E, 75460N AMG metric) to western Sheet margin.|16-MAY-23
20556|Woolla Gneiss|Extent|West and west-northwest from 'Woolla Downs' outstation to beyond Sheet boundary.|16-MAY-23
20556|Woolla Gneiss|Lithology|Quartz-biotite-feldspar gneiss, muscovite-biotite-quartz schist, garnet-biotite-quartz feldspar gneiss. All exposed in type area.|16-MAY-23
20556|Woolla Gneiss|Relationships and boundaries|Overlain by slate and quartzite correlated with the Ledan Schist at Mount Solitary. Unconformably overlain by Central Mount Stuart Beds.|16-MAY-23
20556|Woolla Gneiss|Proposed publication|BMR Report|16-MAY-23
20556|Woolla Gneiss|Name first published by|Shaw R.D., Warren R.G., Kopras J., Green D.E., 1975.|16-MAY-23
24586|Wuluma granitoid|Name source|Wiluma Hills, GR 5651-940372 in the Alice Springs 1:250 000 Sheet ara. The Hills are shown in the Burt 1:100 000 preliminary geological map.|16-MAY-23
24586|Wuluma granitoid|Unit history|Previously mapped as undivided Arunta Complex by Wells and others (1968).|16-MAY-23
24586|Wuluma granitoid|Type section locality|Reference area: 1 km2 area centred on GR 930372, each side of the vehicle track.|16-MAY-23
24586|Wuluma granitoid|Extent|Rounded hills, over 16 km2, immediately southeast of Salt Bush Bore.|16-MAY-23
24586|Wuluma granitoid|Lithology|The unit consists of a granitoid: that is, coarse-grained granitic rock gradational with the mobilisate of the adjacent migmatitic rocks of the Ingular Migmatite suite. Small amounts of mafic granulite and sillimanite gneiss occur as xenoliths.|16-MAY-23
24586|Wuluma granitoid|Relationships and boundaries|Gradational with the migmatite of the Ingula migmatite suite and intrudes the Erontonga metamorphics. It is part of the Ingoola migmatite suite.|16-MAY-23
24586|Wuluma granitoid|Age reasons|Middle Proterozoic or older. A preliminary Rb-Sr total rock date of about 1800 m.y. has been obtained for the granitoid (L P Black, BMR, pers. comm., 1978).|16-MAY-23
24586|Wuluma granitoid|Proposed publication|Stewart & others, in prep.|16-MAY-23
24586|Wuluma granitoid|Defn Reference|80/20787|16-MAY-23
24586|Wuluma granitoid|Proposer|Langworthy A.P. (in Shaw & others, in preparation a)|16-MAY-23
24586|Wuluma granitoid|Unit name|Wuluma Granitoid (informal)|16-MAY-23
20739|Yackah Beds|Name source|Yackah Waterhole, Field River, Hay River 1:250 000 Sheet area.|16-MAY-23
20739|Yackah Beds|Unit history|This is the lowermost unit of the Field River Beds of Smith (1963).|16-MAY-23
20739|Yackah Beds|Type section locality|Because of extremely poor outcrop no type section has been nominated. The outcrops flanking the northern and eastern margins of the Mt Dobbie Granite (Adams Special 1:100 0000 Geological Sheet). Near Mt Cornish on the Huckitta Sheet the unit is 26 m thick.|16-MAY-23
20739|Yackah Beds|Extent|The formation is exposed on the Hay River and Huckitta 1:250 000 Sheet areas.|16-MAY-23
20739|Yackah Beds|Relationships and boundaries|Nonconformably overlies granite basement. Upper boundary not exposed on the Hay River Sheet area but it is probably a disconformity with the Yardida Tillite. The upper boundary near Mt Cornish is formed by the base of the Mt Cornish Formation (as redefined by Walter, 1979); the two units are structurally conformable but on regional grounds the units are considered to be disconformable, i.e. disconformities occur at this level in the nearby Ngalia and Amadeus Basins. In addition, the Mt Cornish Formation contains boulders of stromatolitic dolomite probably derived from the Yackah Beds.|16-MAY-23
20739|Yackah Beds|Age reasons|The stratigraphic position and presence of the stromatolite Acaciella australica indicate correlation with the Bitter Springs Formation and probably also the Heavitree Quartzite of the Amadeus Basin. These units are Adelaidean.|16-MAY-23
20739|Yackah Beds|First Reference|79/20074|16-MAY-23
