Stratno | Stratigraphic Name | Category | Contents | Last update 
376|Amphitheatre Formation|Name source|The Amphitheatre - an amphitheatre shaped arrangement of hills about 15 km west of Cobar - grid reference 367100 Cobar 1:250 000 sheet (SH55-14) (NB.  This name has also been given to a nearby property and a government tank).|16-MAY-23
376|Amphitheatre Formation|Unit history|Andrews (1913) included these beds in his Amphitheatre Series. Mulholland (1937) included them in his Amphitheatre Stage. Thomson (1950) included them in his Amphitheatre Series except for the lower part (his CSA Beds) which he included in his Cobar Group. Joklik (1950) and Iten and Carter (1951) divided the sequence into their Amphitheatre and CSA Groups. Rayner (1961) followed Thomson (1950) by dividing the sequence into his Amphitheatre Group and CSA Beds (which he included in the Cobar Group), Russell and Lewis (1965) divided the sequence into the Amphitheatre Beds, Water Tower and Alley Beds and the CSA Siltstone (which they included in the Cobar Group). Brunker (1970) followed Russell and Lewis but included the Water Tower and Alley Beds in his Amphitheatre Beds.|16-MAY-23
376|Amphitheatre Formation|Type section locality|No type section has been measured because of the poor outcrop and the folding. An incomplete section has been measured across the road to the CSA mine from GR 851202 to 858203 (Cobar 1:100 0000). The formation is well exposed in this area and in the Amphitheatre Dome area. The base of the formation is exposed only where there is no basal CSA Siltstone Member e.g. GR 378129 Cobar 1:250 000.|16-MAY-23
376|Amphitheatre Formation|Extent|The unit is exposed over most of the western third of the Cobar 1:250 000 Sheet, along most of the eastern edge and the southeastern quarter of the Barnato 1:250 000 sheet (SH55-13) and in the McCullochs Ranges on the eastern Wilcannia sheet (SH54-16).|16-MAY-23
376|Amphitheatre Formation|Thickness range|A thickness of 757 m was measured in the incomplete section referred to above. A thickness of at least 1500 m would be expected in that vicinity. Durney (1975) reports a thickness of 5700 m in the Tyncin district (NW corner of the Cobar 1:250 000 sheet).|16-MAY-23
376|Amphitheatre Formation|Lithology|Claystone, siltstone, fine to medium grained sandstone, quartzite; thinly bedded; graded bedding, convolute bedding, cross bedding, cross bedded ripples, climbing ripples, casts of worm trails, flute casts, scour and tool marks and load casts are common.|16-MAY-23
376|Amphitheatre Formation|Relationships and boundaries|Conformably overlies the Great Cobar Slate - boundary marked by an influx of thin siltstone and sandstone beds. Overlain by the Mulga Downs Group (basal coarse sandstone and conglomerate in some areas) with at least local unconformity.|16-MAY-23
376|Amphitheatre Formation|Age reasons|Early Devonian - fossil localities are common and widely distributed. The assemblages consist largely of lamellibranchs and brachiopods, in particular Howellella jaqueti (Dun). The fauna has been described, in part, from erratic boulders found at White Cliffs (Dun W.S., 1898). Notes on the fauna of the Devonian boulders occurring at the White Cliffs opalfields. Rec. geol. Surv. 5 (4), 160-174.|16-MAY-23
376|Amphitheatre Formation|References|GOLD0014; 51/013; 01/31569; GOLD1604; GOLD0957.|16-MAY-23
820|Ayr Conglomerate|Name source|Manser, 1968 Geological Map of New England, Wingen, 1:100 000 Sheet.|16-MAY-23
820|Ayr Conglomerate|Unit history|Previously Ayr Conglomerate now Ayr Conglomerate Member of the Isismurra Formation.|16-MAY-23
820|Ayr Conglomerate|Type section locality|See Manser (1968): Wingen district. Manser (1968) has not adequately defined a type section.|16-MAY-23
820|Ayr Conglomerate|Extent|Widely distributed throughout the Wingen and Rouchel districts.|16-MAY-23
820|Ayr Conglomerate|Thickness range|a) At type Section: -          b) Maximum known:  470 m at Benmore in the Rouchel district.|16-MAY-23
820|Ayr Conglomerate|Lithology|See Manser (1968)|16-MAY-23
820|Ayr Conglomerate|Relationships and boundaries|Occurs within the lower part, or forms the basal unit of the Isismurra Formation (Manser 1968). Because the conglomerate is interbedded with sediments referable to the Isismurra Formation it is reduced in status to a member of the latter formation.|16-MAY-23
820|Ayr Conglomerate|Age reasons|Lower Carboniferous (early Visean). Occurs between marine units containing the Pustula gracilis and Orthotetes australis Zones.|16-MAY-23
852|Back Yamma Andesite|Name source|Back Yamma School GR 621886, Forbes 1:250 000|16-MAY-23
852|Back Yamma Andesite|Unit history|Previously named Goonumbla Volcanics (Forbes 1:250 000 Geological Sheet 1972). When the Goonumbla Volcanics were redefined by Sherwin (Rec. geol. Surv. NSW 15(1), 1973) a new name was required for this unit.|16-MAY-23
852|Back Yamma Andesite|Type section locality|GR 619885, on side of road.|16-MAY-23
852|Back Yamma Andesite|Extent|Narrow (0.5 km wide) northeasterly trending belt, 5 km long, 2 km west of school.|16-MAY-23
852|Back Yamma Andesite|Lithology|Andesite|16-MAY-23
852|Back Yamma Andesite|Relationships and boundaries|Intrusive (?) dyke (?) into Late Ordovician sediments.|16-MAY-23
852|Back Yamma Andesite|Age reasons|Late Ordovician (?) by analogy with other andesites in the Parkes area.|16-MAY-23
27282|Ballallaba Adamellite|Name source|Ballallaba Homestead GR 372583.|16-MAY-23
27282|Ballallaba Adamellite|Unit history|Included as part of the Boro Granite by previous workers, however the Boro mass is a separate body in the Braidwood 1:100 000 sheet area to the north.|16-MAY-23
27282|Ballallaba Adamellite|Type section locality|A 3 m high tor about 20 m west of the Captains Flat-Braidwood Road at GR 321568.|16-MAY-23
27282|Ballallaba Adamellite|Extent|Between Gourock Range and Shoalhaven River in western part of Araluen 1:100 000 Sheet area, west of Shoalhaven Fault. Occupies about 220 square kilometres.|16-MAY-23
27282|Ballallaba Adamellite|Lithology|Medium to coarse-grained inequigranular adamellite with prominent quartz phenocrysts up to 10 mm and rarer plagioclase also to 10 mm. Mafic minerals (biotite >hornblende) make up about 10% of the rock. The rock is finer grained, more mafic (colour index = 16) and of granodiorite composition near GR 328458. The change is gradational.|16-MAY-23
27282|Ballallaba Adamellite|Age reasons|Early Devonian. K/Ar biotite dates of 398 +/- 13 and 394 +/- 6 Ma. Rb/Sr biotite-whole rock isochron of 389 +/- 8 Ma with initial ratio 0.7085.|16-MAY-23
27105|Banar Formation|Name source|Parish of Banar, County Gipps|16-MAY-23
27105|Banar Formation|Type section locality|The type Section for the formation is along the east-west Burcher-Forbes road. The base of the formation and its contact with the Ina Volcanics is here exposed, however the top of the formation is not exposed. Contacts with the overlying Corringle Formation outcrop further to the south.  533857 (bottom) to 528858 (top) Forbes 1:250 000.|16-MAY-23
27105|Banar Formation|Extent|Exposed for about 20 km of strike between Lake Cowal siding and Burcher.|16-MAY-23
27105|Banar Formation|Thickness range|Above 4000 m.|16-MAY-23
27105|Banar Formation|Lithology|It consists of a rather uniform sequence of a fine grained, finely laminated quartz greywacke or tuff. The Banar Formation has a very characteristic lithology: it is almost invariably laminated. The laminae are about 1 mm thick, very regular and persistent. They are marked by very fine layers of sericite in between which there are angular grains of quartz, plagioclase and sericitic quartz-feldspar rock fragments. It is difficult to decide whether the unit is a tuff or a greywacke or a combination of both. The unit contains a few dolerite or diorite sills.|16-MAY-23
27105|Banar Formation|Relationships and boundaries|The Banar Formation conformably overlies the Ina Volcanics and conformably underlies the Corringle Formation. It is characterised by its vertical and lateral lithologic uniformity. It is both a stratigraphic interval and lithological unit.|16-MAY-23
27105|Banar Formation|Age reasons|Probably Silurian, from stratigraphic position.|16-MAY-23
27105|Banar Formation|Proposed publication|Bulletin Australian Society of Exploration Geophysicists (V.7 No. 1)|16-MAY-23
24174|Bannister Basalt|Name source|Bannister locality; grid reference 28086895, Goulburn 1:250 000 Sheet area (SL 55-12).|16-MAY-23
24174|Bannister Basalt|Type section locality|30 m section in a tributary gully to Kialla Creek, from 28856885 (bottom) to 28856880 (top). Base is identified by brownish-grey very weathered basalt overlying orange-brown quartzose sediment, and the top is the upper sub-aerial surface of the basalt.|16-MAY-23
24174|Bannister Basalt|Extent|Unit is a 5 km tongue of basalt in the headwatears of Kialla Creek, a tributary to the Wollondilly River.|16-MAY-23
24174|Bannister Basalt|Thickness range|30 to 40 m.|16-MAY-23
24174|Bannister Basalt|Lithology|Porphyritic, even-grained and glassy basanite (11 analyses) with local high concentrations of ultramafic xenoliths. Columnar, platy, hackly and massive forms all common. Contains minor interbeds of inter-flow silcrete and black pedal clays with quartz granules.|16-MAY-23
24174|Bannister Basalt|Relationships and boundaries|Discontinuously conformably overlies 1 m of essentially contemporaneous orange-brown, cross-bedded quartzose sand and granules. Where this sub-basaltic sediment is absent, disconformably overlies undifferentiated Ordovician phyllites. The upper boundary is the sub-aerial top surface of the basalt.|16-MAY-23
24174|Bannister Basalt|Age reasons|Early Miocene on basis of K-Ar ages (Young & Bishop, 1980).|16-MAY-23
24174|Bannister Basalt|References|85/24947|16-MAY-23
37927|Barneys Springs Andesite Member|Name source|After Barneys Springs Creek in the Wean region (Willuri 1:25,000 sheet).|16-MAY-23
37927|Barneys Springs Andesite Member|Unit history|Name was first applied informally to the andesite by Nott (1968).|16-MAY-23
37927|Barneys Springs Andesite Member|Geomorphic expression|Rounded hills.|16-MAY-23
37927|Barneys Springs Andesite Member|Type section locality|The type section is taken along Barneys Springs Creek (GR461045 to 457044 Willuri 1:25,000 sheet).|16-MAY-23
37927|Barneys Springs Andesite Member|Extent|The andesite crops out for approximately 8 km from 1.5 km north-northwest of Our Hill (GR459059 Willuri 1:25,000 sheet) in the north to Mount Surprise (GR463996 Willuri) in the south in the Wean Gap region north of Gunnedah.|16-MAY-23
37927|Barneys Springs Andesite Member|Thickness range|> 300m|16-MAY-23
37927|Barneys Springs Andesite Member|Lithology|Brown to grey, locally agglomeratic andesite with large crystals of rimmed and resorbed plagioclase, clinopyroxene, orthopyroxene and opaque minerals, the last three commonly as crystal aggregates. The groundmass is predominantly red-brown glass partially replaced by chlorite and zeolite. Vitric beds at the base and top of the andesite are extensively zeolitised, exhibit perlitic textures and are usually red-brown in colour.|16-MAY-23
37927|Barneys Springs Andesite Member|Depositional environment|Largely a volcanic flow unit.|16-MAY-23
37927|Barneys Springs Andesite Member|Age reasons|Carboniferous (Visean)|16-MAY-23
37927|Barneys Springs Andesite Member|Correlations|Barneys Spring Andesite Member (Brown et al. 1990 - 94/28024). Barneys Springs Andesite (Opdyke et al. 2000).|16-MAY-23
37927|Barneys Springs Andesite Member|References|94/28024;  **NOTT S.A. 1968. The Upper Devonian-Carboniferous sequence at Wean, west of Manilla, New South Wales. BSc (Hons) thesis, University of New England, Armidale (unpubl.).  **OPDYKE N.D., ROBERTS J., CLAOUE-LONG J., IRVING E. & JONES P.J. 2000. Base of the Kiaman: Its definition and global stratigraphic significance. Geological Society of America Bulletin 112, 1315-1341.|16-MAY-23
1154|Barracks Creek Adamellite|Name source|From Barracks Creek, a tributary of the Queanbeyan River, south of Queanbeyan.|16-MAY-23
1154|Barracks Creek Adamellite|Unit history|Barrack Creek Adamellite (Phillips, 1956); Queanbeyan Granite (Stauffer and Richard 1968).|16-MAY-23
1154|Barracks Creek Adamellite|Type section locality|A large quarry on the old Cooma-Queanbeyan road at GR 019/807 (Canberra 1:100 000 sheet 8727). The rock is a pale-grey medium-grained adamellite permeated by quartz veinlets and locally intruded by dolerite dykes. The exposure of the contact zone with the Colinton Volcanics depends on quarrying operations. Within the zone the adamellite appears to dip steeply beneath grey foliate and progressively silicified dacitic ignimbrite.|16-MAY-23
1154|Barracks Creek Adamellite|Extent|Poorly exposed over an area of 4 km2. The arcuate outcrop pattern is bounded to the southeast by a prominent strike swing in the Colinton Volcanics (Stauffer 1967).|16-MAY-23
1154|Barracks Creek Adamellite|General description|The intrusion ranges in composition from admellite to leucogranite. The adamellite consists of quartz, plagioclase, perthitic K-feldspar and biotite. synemplacment deformation is indicated by fracturing and kaolinite/epidote-rich deuteric alteration. Determination of the S or I-type affinities of the intrusion is precluded by the weathered state of the rocks and absence of geochemical data.|16-MAY-23
1154|Barracks Creek Adamellite|Age reasons|The Barracks Creek Adamellite intrudes and is faulted against the late Ordovician Pittman Formation (Henderson, 1978). A Late Silurian (possibly post Ludlovian) age is indicated by a discordant contact with Colinton Volcanics. A minimum age is indicated by intrusion of east-west trending, probably Early Devonian, dolerite dykes. The Barracks Creek Adamellite is probably co-magmatic with the Googong Adamellite and other minor granite bodies intruding the Late Silurian volcano-sedimentary sequence of the Canberra Block.|16-MAY-23
26293|Bevendale Basalt|Name source|Hamlet of Bevendale; GR 9450 7650 Goulburn 1:250 000 Sheet area (SI 55-12).|16-MAY-23
26293|Bevendale Basalt|Type section locality|The unit is poorly exposed and many outcrops are quite weathered. The type section is weathered but is the thickest exposure. It is designated as a 70 m section on a tributary gully to Jerrara Creek, 3 km NW of Mullengrove hamlet, from 9680 8445 (bottom) to 9645 8415 (top). The top is the sub-aerial, upper surface of the basalt and the base is the lowest lava overlying Ordovician phyllite.|16-MAY-23
26293|Bevendale Basalt|Extent|The unit occurs in discontinuous, narrow, linear outcrops which run from Mt Martin to Dalton and from Dalton to the junction of the Lachlan and crookwell Rivers.|16-MAY-23
26293|Bevendale Basalt|Thickness range|Range 20 m to 100 m.|16-MAY-23
26293|Bevendale Basalt|Lithology|Alkaline, fine-grained to porphyritic olivine basalt; occasionally coarse-grained (doleritic); generally columnar but massive, hackly and platy forms are all present. One outcrop of palagonitized flow-foot breccia incorporating black, glassy basalt, basaltic glass and palagonite (01106360). Individual flows rarely distinguishable on field criteria, but breaks between flows are occasionally marked by interbedded Au silcrete.|16-MAY-23
26293|Bevendale Basalt|Relationships and boundaries|Conformably overlies the Hollymount Foundation. Where this formation absent, disconformably overlies either Ordovician phyllites or Palaeozoic granitic rocks of the Wyangala Batholith. Base of unit occasionally marked by either a prominent ironstone band or a grey clay which is very weathered basalt. Upper boundary is sub-aerial upper surface of basalt.|16-MAY-23
26293|Bevendale Basalt|Age reasons|Early Miocene on basis of K-Ar ages (Wellman & McDougall, 1974; Young & Bishop, 1980).|16-MAY-23
26293|Bevendale Basalt|References|79/04604; 85/24947|16-MAY-23
27338|Bijerkerno Beds|Name source|Bijerkerno property, Broken Hill, 1:250 000 Sheet area SH 54.14 GR 4643 1136.|16-MAY-23
27338|Bijerkerno Beds|Unit history|Unit named originally by Rose (1970), but not clearly defined. The same name is retained.|16-MAY-23
27338|Bijerkerno Beds|Type section locality|900 m of carbonaceous slates, phyllites, quartzites and schists along an east-west section north of Bijerkerno H.S. Unconformably overlain by the late Pre-Cambrian Adelaidean system. Base defined by top of underlying laminated calc-silicate horizon. Top GR 4636 1149. Bottom GR 4621 1143.|16-MAY-23
27338|Bijerkerno Beds|Extent|The unit is distributed over an area of ~20 km2 in the north central portion of the Broken hill Sheet (SH 54.14) north and west of Bijerkerno H.S.|16-MAY-23
27338|Bijerkerno Beds|Thickness range|Type section 900 metres. Range about 700-1200 m.|16-MAY-23
27338|Bijerkerno Beds|Lithology|Fine grained carbonaceous sequences of interbedded metamorphosed shales, siltstones and quartzites, ((?) cherts). Slump structures, transported and non-transported breccias occur in parts of the section.|16-MAY-23
27338|Bijerkerno Beds|Relationships and boundaries|Conformably overlies the Wookookaroo Beds. The top of which is defined by 2-3 m thick laminated calc-silicate horizon. Unconformably overlain by late Pre-Cambrian Adelaidean system sediments. Specifically the Pintapah sub-group (Cooper and Tuckwell, 1971).|16-MAY-23
27338|Bijerkerno Beds|Age reasons|Believed to belong to the Willyama Complex (1700 m.y.). If so, then would represent the youngest Willyama Complex yet exposed. Conformity with higher grade metamorphics beneath (Wookookaroo Beds), which are traditionally and historically considered part of Willyama Complex would attest to their age.|16-MAY-23
27338|Bijerkerno Beds|References|79/00937|16-MAY-23
26395|Birkenburn Beds|Name source|"Birkenburn", a property on the northeastern flank of the Sand Hills, GR 332005, Braidwood 1:100 000 Sheet.|16-MAY-23
26395|Birkenburn Beds|Unit history|Mount Fairy Series (in part), (Garretty, 1936); Mount Fairy Group (in part), (Joplin et al. 1953); Mount Fairy Beds (in part), (Best et al. 1964). The name "Mount Fairy Series" was given by Garretty to " a group of rocks covering an extensive area in the southern and eastern parts of the (Lake George) district." Garretty (op. cit) further stated "Shales form the chief rock type, but phyllites, sandstones, tuffs, limestones and minor intrusions also occur, some of which are certainly of Silurian age and all may well be".|16-MAY-23
26395|Birkenburn Beds|Constituents|Merigan Black Shale|16-MAY-23
26395|Birkenburn Beds|Type section locality|Representative sections: Eastern belt: along Sandhills Creek 1 km east of the dolomite quarries (GR 378024) to the point where the creek cuts the scarp of the Mulwaree Fault (GR 387028). Western Belt: Creek section along Sandhills Creek between GR 351018 and GR 363019.|16-MAY-23
26395|Birkenburn Beds|Extent|Occupies two parallel meridional belts. The eastern belt extends from near Tarago in the north to "Bengwen" property (GR 353915) in the south, and the western belt from west of "Woodlawn" property (GR 331170) in the north, to south of "Werriwa" property (GR 284006) in the south. As defined here the Birkenburn Beds do not extend further east than the Tarago-Braidwood road, or west of Bungendore.|16-MAY-23
26395|Birkenburn Beds|Thickness range|Unknown; the extent of the western belt suggests that the thickness may be of the order of 3000 m.|16-MAY-23
26395|Birkenburn Beds|Lithology|Buff to grey medium arenite, green and grey siltstone and shale, black graptolitic slaty shale, all metamorphosed to lower greenschist facies.|16-MAY-23
26395|Birkenburn Beds|Relationships and boundaries|Top and base not exposed. The eastern belt is faulted against the Early Devonian Boro Granite in the east and the Silurian Mount Fairy Group in the west. It is unconformably overlain by the Tarago Conglomerate (Early Devonian). The western belt is faulted against the Mount Fairy Group in the east and it is overlain unconformably by the Woodlawn Volcanics. Its western boundary is concealed by alluvium.|16-MAY-23
26395|Birkenburn Beds|Age reasons|Graptolites, found in both eastern and western belts, include the following genera: Climacograptus, Dicellograptus, Orthograptus, Dicranograptus, giving a Late Ordovician (Eastonian) age to the upper part of the unit.|16-MAY-23
26395|Birkenburn Beds|References|85/24687|16-MAY-23
24187|Black Ridge Tuff|Name source|Black Ridge Prospect, Parkes, GR 6192 9120 Forbes 1:250 000.|16-MAY-23
24187|Black Ridge Tuff|Type section locality|Prospect area at The Secrets Prospect. Traverse from road material quarry to west. Top and bottom exposed.|16-MAY-23
24187|Black Ridge Tuff|Extent|Crops out on eastern limb of anticline. Mapped over 5 km of strike.|16-MAY-23
24187|Black Ridge Tuff|Thickness range|About 200 m at type section and elsewhere.|16-MAY-23
24187|Black Ridge Tuff|Lithology|Fine to coarse andesitic tuffs.|16-MAY-23
24187|Black Ridge Tuff|Relationships and boundaries|Overlies The Secrets Andesite (flow andesite) and underlies the Cotton Siltstone.|16-MAY-23
24187|Black Ridge Tuff|Age reasons|Late Ordovician on stratigraphic evidence.|16-MAY-23
24733|Blayney Andesite|Name source|Township of Blayney, GR 2225 8557, Bathurst 1:250 000 Metallogenic Sheet.|16-MAY-23
24733|Blayney Andesite|Type section locality|GR 2234 8549 - GR 2275 8534, Bathurst 1:250 000 Sheet.|16-MAY-23
24733|Blayney Andesite|Extent|Where mapped, lies in a belt east of Blayney and extending for at least 30 km. Also lies between the Carcoar Granite and the Tertiary basalt.|16-MAY-23
24733|Blayney Andesite|Thickness range|Unknown|16-MAY-23
24733|Blayney Andesite|Lithology|Andesite consisting of blocky pyroxene phenocrysts (50%+ of rock) in a mid-green-grey groundmass. Plagioclase phenocrysts are more abundant in the upper 50 m.|16-MAY-23
24733|Blayney Andesite|Relationships and boundaries|Underlies and is faulted against the Cowriga Limestone nov. at Browns Creek and conformably underlies the Quigleys Hill Tuff nov. at Blayney. Further south unconformably underlies the Wombian Formation nov.|16-MAY-23
24733|Blayney Andesite|Age reasons|Late Ordovician, being a subdivision of the Angullong Group (previously Angullong Tuff) is Late Ordovician in age.|16-MAY-23
24733|Blayney Andesite|References|GOLD1661|16-MAY-23
2079|Bogalong Granodiorite|Name source|Bogalong School GR 614813, Forbes 1:250 000 Sheet.|16-MAY-23
2079|Bogalong Granodiorite|Unit history|Previously named Grenfell Granite (Forbes 1:250 000 Geological Sheet 1972). As it is a granodiorite while the Grenfell Granite is a true granite it has been separately named.|16-MAY-23
2079|Bogalong Granodiorite|Type section locality|GR 613813, on side of hill.|16-MAY-23
2079|Bogalong Granodiorite|Extent|300 km2 centred on GR 610823|16-MAY-23
2079|Bogalong Granodiorite|Lithology|Granodiorite (andesine>orthoclase>quartz, minor clinopyroxene, tourmaline).|16-MAY-23
2079|Bogalong Granodiorite|Relationships and boundaries|Intrusive into Late Ordovician sediments.|16-MAY-23
2079|Bogalong Granodiorite|Age reasons|Early Devonian (?) by analogy with the Grenfell Granite.|16-MAY-23
24741|Bogandillon Chert Member|Name source|Bogandillon Swamp.|16-MAY-23
24741|Bogandillon Chert Member|Type section locality|532874 (bottom) to 531874 (top) Forbes 1:250 000 |16-MAY-23
24741|Bogandillon Chert Member|Extent|Outcrops for 10 km along strike|16-MAY-23
24741|Bogandillon Chert Member|Thickness range|500 m.|16-MAY-23
24741|Bogandillon Chert Member|Lithology|Calcareous chert.|16-MAY-23
24741|Bogandillon Chert Member|Relationships and boundaries|Gradational|16-MAY-23
24741|Bogandillon Chert Member|Identifying features|For further details, see Weelah Formation.|16-MAY-23
24741|Bogandillon Chert Member|Proposed publication|Bulletin Australian Society of Exploration Geophysicists (v.7 No. 1)|16-MAY-23
27111|Boggy Plain Adamellite|Name source|Boggy Plain GR 435310 Tantangara 1:100 0000 Sheet area.|16-MAY-23
27111|Boggy Plain Adamellite|Type section locality|GR 429315 Tantangara 1:100 000 Sheet area.|16-MAY-23
27111|Boggy Plain Adamellite|Extent|Divided into two areas by a major fault: (1) Occupies the whole of Boggy Plain, an area of about 15 km2.  (2) Occupies most of the area between Tantangara Mountain, Sawyers Hill and Alpine Hill, on the Eucumbene River and in the Rocky Plain Creek basin, an area of aboaut 25 km2.|16-MAY-23
27111|Boggy Plain Adamellite|Lithology|Hornblende biotite adamellite, augite bearing hornblende-biotite granodiorite, two pyroxene diorite, alkali granite.|16-MAY-23
27111|Boggy Plain Adamellite|Relationships and boundaries|Intrudes the Middle Ordovician Bolton Beds, the Early Silurian Tantangara Beds and the probable Late Silurian Gang Gang Adamellite.|16-MAY-23
27111|Boggy Plain Adamellite|Age reasons|Early Devonian as it is geochemically related to the Early Devonian Coolamine Igneous Complex. Rb/Sr and K/Ar ages are concordant and give ages of 416 m.y.|16-MAY-23
2486|Braidwood Granite|Name source|Braidwood town, GR 740540, Braidwood 1:100 000 sheet.|16-MAY-23
2486|Braidwood Granite|Type section locality|Features of the Braidwood Granite can be observed along the Braidwood-Nowra road between 7 and 15 km from Braidwood. Rounded, tor-like outcrops are scattered through nearby paddocks and fresh rock is exposed at the roadside 100 m north of Durran Durra Creek, 13 km from Braidwood. Dykes intruding the Braidwood Granite can be observed in road cuttings about 10 km from Braidwood.|16-MAY-23
2486|Braidwood Granite|Extent|The Braidwood Granite forms a north-south trending body 50 km long and 15 km wide centred on the town of Braidwood.|16-MAY-23
2486|Braidwood Granite|Lithology|The main rock type in the Braidwood Granite is hornblende biotite granodiorite, although adamellite and minor granite are also present. A porphyritic microgranodiorite containing corroded quartz phenocrysts has also been noted (Kennedy, 1961). Biotite-rich igneous xenoliths of diorite composition up to 10 cm in diameter show reaction contacts with the enclosing rocks. Dykes rocks include aplite, quartz microdiorite and analcite microdiabase (Stevenson, 1970).|16-MAY-23
2486|Braidwood Granite|Relationships and boundaries|The granite intrudes undifferentiated Ordovician metasediments and Middle to Late Silurian Long Flat Volcanics. It is unconformably overlain by the Minuma Beds (Late Devonian).|16-MAY-23
2486|Braidwood Granite|Age reasons|On stratigraphic grounds the Braidwood Granite has an age of latest Silurian to Middle Devonian. It is regarded (Felton and Huleatt, 1975) as having been emplaced at about the same time as the nearby Ellenden and Boro Grnaites, which have similar field and petrographic characteristics.  The Braidwood Granite has been dated by the potassium/argon method at 385 m.y. (Evernden and Richards, 1962) (Early Devonian).|16-MAY-23
2486|Braidwood Granite|References|GOLD1671; 79/05413.|16-MAY-23
2522|Bredbo River Adamellite|Name source|After the Bredbo River which crosses the body.|16-MAY-23
2522|Bredbo River Adamellite|Unit history|The adamellite was previously unmapped and unnamed.|16-MAY-23
2522|Bredbo River Adamellite|Type section locality|Best exposure is along the river banks and in the river bed at GR 117167.|16-MAY-23
2522|Bredbo River Adamellite|Description at type locality|The adamellite has a typical bouldery mode of outcrop. Consists of a dominant phase of medium- to coarse-grained adamellite containing large pink subhedral crystals of microperthitic alkali feldspar (30%), quartz (25%), plagioclase (20%), and biotite with minor inclusions of muscovite, apatite, magnetite and zircon. A minor phase is formed at GR 111160; it is texturally heterogeneous with large white feldspars and slightly smaller quartz crystals set in a fine-grained biotite rich groundmass. A minor number of xenoliths have been found within the dominant adamellite phase. The adamellite has suffered mild alteration.|16-MAY-23
2522|Bredbo River Adamellite|Extent|The adamellite lies roughly 1.5 km to the west of the Jerangle Igneous Complex and appears both to the south and north of the Bredbo River, extending from GR 118182 to GR 120135. Michelago 1:100 000 Geological Sheet. Size: The adamellite covers an area of 2.5 km2, has an extremely elongate form and is approximately 5 km by 0.75 km wide.|16-MAY-23
2522|Bredbo River Adamellite|Relationships and boundaries|Generally a fault-bounded eastern side, with a band of Silurian volcanics and sediments adjacent to the adamellite (Kohinoor Volcanics). The adamellite invades Late Ordovician Foxlow Beds. A minor fault displaces the southern section of the mass by 100 m. No contact metamorphic aureole has been noted.|16-MAY-23
2522|Bredbo River Adamellite|Age reasons|The Bredbo River Adamellite was probably emplaced at the close of the Silurian Period.|16-MAY-23
25813|Brooklana Beds|Name source|Village of Brooklana (GR 5952 2506 Dorrigo 1:250 000).|16-MAY-23
25813|Brooklana Beds|Unit history|Brooklana Formation (Leitch et al. 1971). The status of this unit is changed from a formation to Beds because it is not possible to designate a type section. Part of the Coffs Harbour Beds of Voisey (1934) and Korsch (1971).|16-MAY-23
25813|Brooklana Beds|Type section locality|Type area: The Brooklana Beds are characteristically exposed around the village of Brooklana. The type area for the rocks previously called the Coffs Harbour Beds was quarry and cliffs on the south side of the town of Coffs Harbour. These rocks occur within the Brooklana Beds and must be regarded as the type area (GR 6254 2449 Coffs Harbour 1:250 000). Type section: None defined - see notes under THICKNESS.|16-MAY-23
25813|Brooklana Beds|Extent|This unit occupies a belt of approximately 1100 km2 trending northwest from the coast at Sawtell and Coffs Harbour, to west of the tunnel (GR 5473 3038 Grafton 1:250 000) on the Grafton to Newton Boyd road. A thin sliver of rocks with Brooklana Beds affinities occurs as a fault slice along the Demon Fault, about 10 km south of Newton Boyd School.|16-MAY-23
25813|Brooklana Beds|Thickness range|Unknown, but because bedding is dominantly steeply dipping to the north, a thick sequence of several thousand metres is suggested.|16-MAY-23
25813|Brooklana Beds|Lithology|Thinly-bedded siliceous mudstones and siltstones, with rarer volcanically-derived sandstones. Dark highly-cleaved mudstones in beds from 1 cm to several metres thick occur interbedded with lighter coloured more siliceous rocks which may be finely laminated. Sandstones are more common than in the Moombil Beds.|16-MAY-23
25813|Brooklana Beds|Fossils|None discovered.|16-MAY-23
25813|Brooklana Beds|Relationships and boundaries|No contacts were observed in the field but the conformable nature of the Brooklana Beds with the underlying Moombil Beds and overlying Coramba Beds was deduced from structural evidence. The Brooklana Beds is distinguished from the Moombil Beds by the absence of black massive argillite and from the Coramba Beds by the predominance of siliceous mudstones and siltstones over sandstones.|16-MAY-23
25813|Brooklana Beds|Age reasons|No fossils were discovered but a Late Palaeozoic age is postulated on the tenuous basis of lithological correlation with sediments of known Carboniferous age (e.g. Halliday's Point, Leitch and Mayer, 1969).|16-MAY-23
25813|Brooklana Beds|References|79/02435; 79/02550; 01/31630; Leitch E.C., and Mayer W., 1969. Mass-movement phenomena in an Upper Carboniferous greywacke-argillite sequence in North-eastern New South Wales. N.Z. Jl. Geol. Geophys., 12(1), 156-171.|16-MAY-23
39260|Bunaleer Rhyodacite Member|Name source|From Bunaleer homestead (02383340E 6607020N Willuri 1:25,000 sheet).|16-MAY-23
39260|Bunaleer Rhyodacite Member|Type section locality|Within section 408 between 30o36'53"S 150o17'15"E (0239970E 6609950N) adjacent to Mihi Creek and a saddle at 30o37'41"S 150o16'54"E (02394300E 6608470N Willuri 1:25,000 sheet).|16-MAY-23
39260|Bunaleer Rhyodacite Member|Extent|Large, lozenge-shaped body 5.3 km long and up to 2 km wide near the western margin of the Carroll-Nandewar block, north of the offset of the Mooki Thrust at Wean Gap.|16-MAY-23
39260|Bunaleer Rhyodacite Member|Thickness range|Maximum of 460 m.|16-MAY-23
39260|Bunaleer Rhyodacite Member|Lithology|Columnar in places. Extremely dense grey to brown rhyodacite (XRD sample 610-1 of Roberts et al. ms) with plagioclase, minor K-feldspar, thin, contorted lenses of quartz, biotite and, in a glassy marginal phase, minor hypersthene; usually strongly flow foliated but away from margins of the body groundmass micropoikilitic to rarely spherulitic; glassy at the base and margins.|16-MAY-23
39260|Bunaleer Rhyodacite Member|Age reasons|The SHRIMP AS3 age of the rhyodacite is 315.0+/-3.5 Ma (sample 432-7, Figure 10, Roberts et al. ms). Early Westphalian.|16-MAY-23
24794|Burburba Formation|Name source|"Burburba" property, GR 615223, Braidwood 1:100 000 Sheet.|16-MAY-23
24794|Burburba Formation|Type section locality|Not defined. Representative sections in quarry at GR 594221, Braidwood 1:100 000 sheet and in the bed of a track at GR 288678, Goulburn 1:250 000 sheet.|16-MAY-23
24794|Burburba Formation|Extent|Occupies about 10 km2 west and northwest of Burburba property.|16-MAY-23
24794|Burburba Formation|Thickness range|Minimum thickness (estimated) is 1200 metres.|16-MAY-23
24794|Burburba Formation|Lithology|Fine to coarse-grained fossiliferous tuffaceous arenite, quartz arenite, siltstone.|16-MAY-23
24794|Burburba Formation|Relationships and boundaries|The southern and eastern boundaries of the unit, where it adjoins the Windellama Limestone, are concealed by alluvium. Bedding in the Burburba Formation has a similar attitude to that in the Windellama Limestone and a conformable relationship, with the Burburba Formation overlying the Windellama Limestone, is inferred. The western boundary of the Burburba Formation is faulted against Silurian sediments. The extent of the unit northward is not known.|16-MAY-23
24794|Burburba Formation|Age reasons|The Burburba Formation contains, inter alia, the trilobite Cheirurus (Crotalocephalides) gaertneri (Alberti), which indicates a Praguian age (Mawson, 1975).|16-MAY-23
24794|Burburba Formation|References|79/02822|16-MAY-23
24801|Bushman Andesite|Name source|Named after the Bushman Mine in the town of Parkes (GR 622902, Forbes 1:250 000) (Bushman Mine Hilll is also named after the mine).|16-MAY-23
24801|Bushman Andesite|Unit history|Previously named Goonumbla Volcanics (Forbes 1:250 000 Geological Sheet 1972). When the Goonumbla Volcanics were redefined by Sherwin (Rec. Geol. Surv. NSW 15(1), 1973) a new name was required for this unit.|16-MAY-23
24801|Bushman Andesite|Type section locality|The rock crops out at the top of the hill (GR 622902).|16-MAY-23
24801|Bushman Andesite|Extent|Crops out in a narrow north-south belt up to 1 km wide and over 5 km long centered on the town of Parkes.|16-MAY-23
24801|Bushman Andesite|Lithology|Andesite|16-MAY-23
24801|Bushman Andesite|Relationships and boundaries|Occurs as a dyke intruding Late Ordovician sediments.|16-MAY-23
24801|Bushman Andesite|Age reasons|Assumed to be Late Ordovician by analogy with Goonumbla Andesite to the northwest.|16-MAY-23
28224|C.S.A. Siltstone Member|Name source|CSA Mine, GR 380114 Cobar 1:250 000 Sheet.|16-MAY-23
28224|C.S.A. Siltstone Member|Unit history|Andrews (1913) included these beds in his CSA Beds (part of his Amphitheatre Series). Thomson (1950) included them in his CSA Beds (which he incorporated in his Cobar Group). Joklik (1950), Iten and Carter (1951) and Thomson (1953) included in a CSA Group. Russell and Lewis (1965) included them in their CSA Siltstone (part of their Cobar Group).|16-MAY-23
28224|C.S.A. Siltstone Member|Type section locality|No type section of this member has been measured because of its poor exposure. The CSA mine is suggested as a type area. It is also exposed in gravel pits beside the Louth road 4 km NW of Cobar. The boundaries of the member are no where well exposed.|16-MAY-23
28224|C.S.A. Siltstone Member|Extent|The unit is exposed over about 15 km2 in a narrow meridional belt passing just west of Cobar.|16-MAY-23
28224|C.S.A. Siltstone Member|Thickness range|No measurement of the thickness has been made. A maximum of 500 m is suggested.|16-MAY-23
28224|C.S.A. Siltstone Member|Lithology|Claystone, siltstone, minor sandstone and quartzite. The sequence is finely laminated. Some rocks are carbonaceous and calcareous.|16-MAY-23
28224|C.S.A. Siltstone Member|Relationships and boundaries|Basal member of Amphitheatre Formation. Conformably overlies Great Cobar Slate.|16-MAY-23
28224|C.S.A. Siltstone Member|Age reasons|The underlying Great Cobar Slate has been dated as Late Silurian to Early Devonian (Sherwin, 1974a) and overlying sediments in undifferentiated Amphitheatre Formation as Early Devonian (Sherwin, 1974b). The age of the unit is therefore Late Silurian to Early Devonian.|16-MAY-23
28224|C.S.A. Siltstone Member|References|GOLD0014; 51/013; GOLD0957; GOLD1058.|16-MAY-23
24207|Cambalong Complex|Name source|Cambalong' property; GR 21564481 Bega 1:250 000 Sheet area.|16-MAY-23
24207|Cambalong Complex|Type section locality|A section across the complex is exposed along the Bombala River and up a small gully to the east, from 21114445 (west) to 21694458 (east).|16-MAY-23
24207|Cambalong Complex|Extent|The complex is exposed over an area of 110 km2 in the south-central portion of the Bega 1:250 000 Sheet area (SJ55-4). Its southern part is centered along the Bombala River.|16-MAY-23
24207|Cambalong Complex|Lithology|The complex contains low pressure-type, regional metamorphic rocks and associated igneous intrusions. Rock types include: phyllites, biotite- and andalusite-bearing schists, coarse grained mica schists, banded gneisses, tonalite, diorite, hornblendite, aplite and pegmatities.|16-MAY-23
24207|Cambalong Complex|Relationships and boundaries|The complex is developed within the Bombala Beds (Geol. Surv. s Victoria & NSW, 1976), a flysch sequence now composed of slates, phyllites, quartzites and cherts. The outer boundaries to the complex are marked by the development of fine-grained biotite-bearing schists, followed by a zone of distinctive knotted schists. To the north the complex is largely obscured by overlying Cainozoic basalts and sediments. It narrows to the south and eventually tapers out.|16-MAY-23
24207|Cambalong Complex|Age reasons|The Bombala Beds are probably Late Ordovician in age (McRoberts, 1948, Sherrard 1962). The age of the regional metamorphism in the Cambalong Complex is not yet known but by analogy with the similar Cooma Complex to the north is expected to be Silurian (Pidgeon & Compston 1965). Two granitic intrusions to the east of the complex have been radiometrically dataed using the potassium-argon method at 413 and 396 m.y. respectively (Evernden and Richards, 1962).|16-MAY-23
24207|Cambalong Complex|Proposed publication|Proceedings of the Linnean Society of NSW|16-MAY-23
24207|Cambalong Complex|References|01/31572; 01/31573.|16-MAY-23
3915|Charbon Sub-Group|Name source|Village of Charbon, south of Kandos, Western Coalfield.|16-MAY-23
3915|Charbon Sub-Group|Unit history|Goldbery (1972) defined this term as including all strata from the base of the Marrangaroo Conglomerate to th top of the Katoomba seam.|16-MAY-23
3915|Charbon Sub-Group|Constituents|Comprises the State Mine Creek Formation (at the top), Angus Place Sandstone, Baal Bone Formation, Glen Davis Formation, Newnes Formation, Irondale Coal and Long Swamp Formation (at base).|16-MAY-23
3915|Charbon Sub-Group|Type section locality|(1) Location: Elecom Lithgow-Newnes DDH 31 (221925 m E, 1310965 m N, Lithgow 1:50 000 sheet, 8931.111).  (2) Repository - Elecom core store, Lithgow.|16-MAY-23
3915|Charbon Sub-Group|Extent|Western Coalfield - Lithgow and Bungleboori 1:50 000 sheets. At least two units within the Sub-Group appear to be of basin-wide extent. Also occurs on parts of Hampton, Katoomba, Glen Davis and Glen Alice sheets.|16-MAY-23
3915|Charbon Sub-Group|General description|Contains arenaceous foraminifera and Acritarchs. Recognised by the interbedded, laminated and bioturbated nature of the argillaceous sediments and the fining downward sandstone units. The Angus Place Sandstone and Baal Bone Formation have lithological equivalents in the Southern Coalfield and in the Singleton Super-Group. The Baal Bone and Long Swamp Formations commonly contain "dropstones".|16-MAY-23
3915|Charbon Sub-Group|Thickness range|(1) Type section: From 228.86 m to 309.45 m. Thickness 80.59 m.  (2) Maximum recorded - 124.25 m.|16-MAY-23
3915|Charbon Sub-Group|Lithology|Mudstone, siltstone, claystone, sandstone, coal, oil shale, siliceous claystone|16-MAY-23
3915|Charbon Sub-Group|Relationships and boundaries|A largely coal-barren unit within the Illawarra Coal Measures.  Conformably underlies the Wallerawang Sub-Group and overlies the Cullen Bullen Sub-Group.|16-MAY-23
3915|Charbon Sub-Group|Proposed publication|Australian Coal Geology|16-MAY-23
4145|Cliefden Caves Limestone Group|General description|Definition: The original Cliefden Caves Limestone of Stevens (1952) is re-defined as a group consisting of three constituent formations (each redefined from their original member status - these are the Fossil Hill Limestone, the Belubula Limestone and the Vandon Limestone. This is necessitated by the detailed mapping of the limestone by Webby and Packham to be the subject of our forthcoming publication. The name of the Cliefden Caves Limestone Group derives from the Cliefden Caves on the south side of Belubula River (GR 758823*); it is now estimated to be about 460 m thick, and to be of upper Gisbornian to middle Eastonian age. It should be noted that the name 'Belubula Limestone Belt' which was introduced by Carne & Jones (1919, p.177) has remained unused for more than 50 years. It should not be reinstated at the expense of the well-established name, the 'Cliefden Caves Limestone' (Group), but redefined to include the middle, massive-bedded limestone formation. (see discussion of Belubula Limestone).   *Canowindra 1:50 000 sheet 8630 I & IV, edit 1 (1978).|16-MAY-23
4359|Colo Creek Formation|Name source|Colo Creek Township GR 227825 and Colo Creek between GR 223823 and 22628242 (Bathurst 1:250 000).|16-MAY-23
4359|Colo Creek Formation|Unit history|The Colo Creek Formation was differentiated from the Abercrombie Beds by Royle (1973).|16-MAY-23
4359|Colo Creek Formation|Type section locality|Along Colo Creek between GRs 22308230 and 22628242 (Bathurst 1:250 000).|16-MAY-23
4359|Colo Creek Formation|Extent|The formation occurs as a wedge-shaped tract about 21 km long and ranging from about 5 km wide in the south wedging out to zero in the northernmost extremity. The tract extends from near Colo Creek Township in the south towards Bathurst, from near GR 225823 to near GR 235843 (Bathurst 1:250 000).|16-MAY-23
4359|Colo Creek Formation|Thickness range|Range 100 m to 700 m.|16-MAY-23
4359|Colo Creek Formation|Lithology|Predominantly composed of grey quartz-rich siltstones containing occasional crinoid ossicles and brachiopods, with lesser amounts of pebbly siltstones low in the formation; and lesser amounts of fine to coarse feldspathic litharenites, lithic arkoses, with interbedded calcareous siltstones and arenites, and rare dolomitic limestones towards the top.|16-MAY-23
4359|Colo Creek Formation|Relationships and boundaries|The formation unconformably overlies the Ordovician Abercrombie Beds and Silurian Blayney Granite in the south, and unconformably overlies the Ordovician Angullong Tuff in the north (Royle, 1973, modified the Angullong Tuff/Abercrombie Beds contact, and differentiated an andesitic volcanic facies and a black slate facies in his "Blayney Andesite", the equivalent of the Angullong Tuff). The formation is fault-bounded in the east.|16-MAY-23
4359|Colo Creek Formation|Age reasons|The upper parts of the formation contain Mucophyllum cf. Crateroides Etheridge, ?Aegiria sp., Cyrtia sp., and ?Encrinurus sp. suggesting a middle to late Silurian age.|16-MAY-23
25862|Coramba Beds|Name source|Village of Coramba (GR 6122 2759 Coffs Harbour 1:250 000).|16-MAY-23
25862|Coramba Beds|Unit history|Leitch et al (1971) named this unit and indicated its aerial extent, but did not define it. Part of the Coffs Harbour Beds as described by Voisey (1934) and Korsch (1971). The term Coramba Granite (Kenny 1937) is here redefined to Coramba Beds as the rock described by Kenny is a very coarse-grained feldspathic sandstone and not a "granite".|16-MAY-23
25862|Coramba Beds|Type section locality|The Coramba Beds are typically exposed along the Coramba to Dorrigo Road immediately west of Coramba village (GR 6122 2557 Coffs Harbour 1:250 000). Type Section: None defined - see comments under Thickness.|16-MAY-23
25862|Coramba Beds|Extent|The Coramba Beds crop out as a broad arc surrounding the southern portion of the Clarence-Moreton Basin. The Beds occupy an area of approximately 2000 km2 reaching from Broomes Head (GR 6481 3303 Maclean 1:250 000) in the north to McCauleys Head (GR 6257 2492 Coffs Harbour 1:250 000) in the south and westwards past Dalmarton to the tunnel on the Grafton-Newton Boyd Road.|16-MAY-23
25862|Coramba Beds|Thickness range|Unknown because of lack of continuous outcrop, mesoscopic folding and small scale reverse faults. A regionally consistent steep dip to the north suggests a thickness of several thousand metres.|16-MAY-23
25862|Coramba Beds|Lithology|Volcanically-derived lithic and feldspathic greywackes, with minor siltstones siliceous siltstones and mudstones. Calcareous siltstones and acid and basic volcanics are rare.|16-MAY-23
25862|Coramba Beds|Fossils|The only fossil found to date was a fragment of a bryozoan (polyzoan) of unknown affinities. Attempts at conodont extractions from calcareous siltstones have been unsuccessful.|16-MAY-23
25862|Coramba Beds|Relationships and boundaries|Structural evidence indicates that the Coramba Beds conformably overlie the Brooklana Beds and are unconformably overlain by the Clarence-Moreton Basin. No contact was observed but the Coramba Beds are distinguished from the Brooklana Beds by the predominance of sandstones over siltstones and mudstones.|16-MAY-23
25862|Coramba Beds|Age reasons|It is postulated that the age of the Coramba Beds is late Palaeozoic, possibly Carboniferous.|16-MAY-23
25862|Coramba Beds|References|01/31639|16-MAY-23
4764|Cosgrove Porphyry|Name source|Cosgrove trig. Station (891 m) at GR 938151, Michelago 1:100 000 Geological Sheet.|16-MAY-23
4764|Cosgrove Porphyry|Unit history|Previously unnamed although mapped by Pillans (1974).|16-MAY-23
4764|Cosgrove Porphyry|Type section locality|at GR 935165|16-MAY-23
4764|Cosgrove Porphyry|Extent|South of Bredbo, between the junction of the Monaro Highway and the Bredbo River.  Size: 1 km2.|16-MAY-23
4764|Cosgrove Porphyry|Lithology|Quartz and feldspar phenocrysts are set in a dark, fine-grained groundmass.|16-MAY-23
4764|Cosgrove Porphyry|Relationships and boundaries|The porphyry is intrusive into the Colinton Volcanics; an intrusive contact is seen at GR 940164|16-MAY-23
4764|Cosgrove Porphyry|Age reasons|Late Silurian-Early Devonian.|16-MAY-23
25863|Cowal Member|Name source|Lake Cowal|16-MAY-23
25863|Cowal Member|Type section locality|537857 (bottom) to 536857 (top) Forbes 1:250 000.|16-MAY-23
25863|Cowal Member|Extent|Isolated outcrops for 16 km along strike.|16-MAY-23
25863|Cowal Member|Thickness range|1000 m.|16-MAY-23
25863|Cowal Member|Lithology|Rhyolite crystal lithic tuff.|16-MAY-23
25863|Cowal Member|Relationships and boundaries|Lithologically distinct from underlying/overlying rocks.|16-MAY-23
25863|Cowal Member|Proposed publication|Bulletin Australian Society of Exploration Geophysicists (v.7 No. 1)|16-MAY-23
25863|Cowal Member|Name first published by|Rees J.E., Taylor R.J., 1976|16-MAY-23
24231|Cowriga Limestone|Name source|Cowriga Creek which flows to the south at GR 21338543, Bathurst 1:250 000 Metallogenic Sheet.|16-MAY-23
24231|Cowriga Limestone|Type section locality|As above.|16-MAY-23
24231|Cowriga Limestone|Extent|Identified in the vicinity of the Browns Creek mine at GR 21338560, Bathurst 1:250 000 Sheet.|16-MAY-23
24231|Cowriga Limestone|Thickness range|Unknown because of faulted nature of boundaries.|16-MAY-23
24231|Cowriga Limestone|Lithology|Limestone, minor tuffs and sediments. The limestone is crystalline, white to light grey. Darker grey limestones and thin tuffs occur in sections with the tuffaceous mud. The lithologies interbedded with the limestone consist either of mud-grey to green-grey mudstones or calcareous fine to medium-grained tuffs and volcanic sandstones. Broken plagioclase and pyroxene crystals predominate in the sandstones. The tuffs are generally much thicker than the muds.|16-MAY-23
24231|Cowriga Limestone|Relationships and boundaries|Overlies the Blayney Andesite with a faulted contact. Possibly correlates with the Quigleys Hill Tuff nov. to the east.|16-MAY-23
24231|Cowriga Limestone|Age reasons|Late Ordovician. Subdivision of the Angullong Group (previously Angullong Tuff) which is Late Ordovician in age.|16-MAY-23
24231|Cowriga Limestone|References|GOLD1661|16-MAY-23
24234|Cumnock Limestone|Name source|Township of Cumnock|16-MAY-23
24234|Cumnock Limestone|Unit history|Incorrectly mapped on Dubbo 1:250 000 as equivalent to the Burrawong Limestone. Corrected relationships set out in map to be published.|16-MAY-23
24234|Cumnock Limestone|Type section locality|Occurs on Brookvale Property about 500 m east of Homestead and about 1 km NE of the northern limits of the township of Cumnock.  Type Section: Dubbo 1:250 000 GR 17159300.|16-MAY-23
24234|Cumnock Limestone|Extent|Restricted outcrop of limestone in the core of an anticline.|16-MAY-23
24234|Cumnock Limestone|Thickness range|Whole thickness not exposed, about 10 m+ exposed.|16-MAY-23
24234|Cumnock Limestone|Lithology|Dark black limestone.|16-MAY-23
24234|Cumnock Limestone|Fossils|Ordovician algae.|16-MAY-23
24234|Cumnock Limestone|Relationships and boundaries|Conformably underlying the Sourges Shale. Base not exposed - formation outcrops in the core of a tight anticline on Brookvale Property.|16-MAY-23
24234|Cumnock Limestone|Age reasons|Latest Ordovician based on presence of Odovician algae; and early Llandovery graptolites in the overlying Sourges Shale.|16-MAY-23
31406|Curra Keith Ignimbrite Tongue|Name source|Named after Curra Keith Creek on the eastern side of Lake Glenbawn (015303 to 035320 Woolooma 1:63 360 Sheet).|16-MAY-23
31406|Curra Keith Ignimbrite Tongue|Type section locality|Eastern side of Lake Glenbawn.  Location of Type Section: The section incorporating the type localities of both the Curra Keith and Oakfields Ignimbrite Tongues is measured near Curra Keith Creek from 015307 to 051329, Woolooma 1:63 360 Sheet. Type locality 028318.|16-MAY-23
31406|Curra Keith Ignimbrite Tongue|Extent|Dangarfield north to Gundy. Extends eastwards as far as Woolooma Range and Scrumlo.|16-MAY-23
31406|Curra Keith Ignimbrite Tongue|Thickness range|a) At Type Section:  70 m.  B) Maximum known:  80 m near Native Dog Gully.|16-MAY-23
31406|Curra Keith Ignimbrite Tongue|Lithology|Buff devitrified ignimbrite.|16-MAY-23
31406|Curra Keith Ignimbrite Tongue|Relationships and boundaries|North and East of Dangarfield, the Curra Keith Tongue splits off from the lower part of the Native Dog Ignimbrite Member. Overlies the Ayr Conglomerate Member, and is overlain by coarse-grained zeolitic lithic sandstone. The Curra Keith Ignimbrite Tongue is within the Isismurra Formation.|16-MAY-23
31406|Curra Keith Ignimbrite Tongue|Age reasons|Lower Carboniferous (Visean). Occurs between units containing the Pustula gracilis Zone and the Orthotetes australis Zone.|16-MAY-23
31406|Curra Keith Ignimbrite Tongue|Comments|Mention, pub. As Curra Keith Tongue|16-MAY-23
5203|Darby Conglomerate Member|Name source|Darby's Range.|16-MAY-23
5203|Darby Conglomerate Member|Type section locality|524885 (bottom) to 520885 (top) Forbes 1:250 000.|16-MAY-23
5203|Darby Conglomerate Member|Extent|10 km along strike.|16-MAY-23
5203|Darby Conglomerate Member|Thickness range|2000 m.|16-MAY-23
5203|Darby Conglomerate Member|Lithology|Conglomerate.|16-MAY-23
5203|Darby Conglomerate Member|Relationships and boundaries|Lithologically distinct.|16-MAY-23
5203|Darby Conglomerate Member|Proposed publication|Bulletin Australian Society of Exploration Geophysicists (v.7 No. 1)|16-MAY-23
28311|Divide Basalt|Name source|The Great Dividing Range, South of Crookwell, NSW, GR 24507080 Goulburn 1:250 000 Sheet area (Sl 55-12).|16-MAY-23
28311|Divide Basalt|Unit history|On field criteria, this basalt may have been formerly continuous with the Wheeo Basalt.|16-MAY-23
28311|Divide Basalt|Type section locality|60 m of volcanic rocks exposed on the divide from 24657090 (bottom) to 24557120 (top). Very poorly exposed.|16-MAY-23
28311|Divide Basalt|Extent|The unit is exposed over about 40 km2 along the crest of the Australian continental drainage divide in the central portion of the Goulburn 1:250 000 Sheet area.|16-MAY-23
28311|Divide Basalt|Thickness range|About 60 m.|16-MAY-23
28311|Divide Basalt|Lithology|Coarse-grained ("doleritic"), uniform fine-grained to porphyritic, and brecciated basanite.|16-MAY-23
28311|Divide Basalt|Relationships and boundaries|Disconformably overlies undifferentiated Ordovician phyllite. Upper surface is the sub-aerial top of the basalt.|16-MAY-23
28311|Divide Basalt|Age reasons|Early to Middle Miocene on basis of one K-Ar age determination (15.8 m.y.) by I. McDougall (pers. comm.). Uncertainties about loss of radiogenic argon (I. McDougall, pers. comm.) suggest that the true age may be closer to approximately 20 m.y., the age of the Wheeo Basalt of which the Divide Basalt may be a lateral equivalent.|16-MAY-23
28311|Divide Basalt|Defn approved by|NSW Stratigraphic Nomenclature Sub-Committee|16-MAY-23
28311|Divide Basalt|Reserved? Yes/No|Variation List 65|16-MAY-23
5871|Durandal Adamellite|Name source|The property "Durandal" (near Yetholme, NSW), used by Mackay (1964) and Watts (1969) as the Durandal Stock.|16-MAY-23
5871|Durandal Adamellite|Unit history|Formerly known but not formalised, as the Yetholme Granite (Durandal Stock) (Mackay, 1964); the Durandal Stock (Watts, 1969); and the Yetholme adamellite (Phillips & Carr, 1973).|16-MAY-23
5871|Durandal Adamellite|Type section locality|Road cutting 0.3 km long at GR 278866 Bathurst 1:250 000 Sheet area (latitude 33o27'S, longitude 149o49'E).|16-MAY-23
5871|Durandal Adamellite|Extent|The adamellite is exposed over approximately 25 km2 as a stock just west of Yetholme.|16-MAY-23
5871|Durandal Adamellite|Lithology|Adamellite, massive, coarse-grained grey with large pink potash feldspar megacrysts; contains xenoliths; minor pegmatite lenses; cut by aplite veins and dolerite (?) and microdiorite dykes; minor sulphide minerals, including Molybdenite.|16-MAY-23
5871|Durandal Adamellite|Relationships and boundaries|Thought to be related to, or part of, the Bathurst batholith which outcrops approximately 2 km south of the adamellite (Mackay, 1964; Watts, 1969; Facer, 1976). Intrudes Silurian and Devonian rocks of the Hill End Trough and Capertee Rise, and cuts across structures within those rocks. May be a separate exposure of the one rock body represented by the Durandal Adamellite and the Eusdale Adamellite (q.v. - new name).|16-MAY-23
5871|Durandal Adamellite|Age reasons|Adamellite dated by K-Ar technique (biotite) at 309 +/- 8 Ma, and 312 +/- 8 Ma; aplite and contact adamellite dated by Rb-Sr technique (whole rock) at 325 +/-17 Ma; (Rb^87 decay constant = 1.39 x 10^-11/y) "dolerite" (microdiorite) dated by K-Ar technique (whole rock) at 298 +/-10 Ma. Reference: Facer (1976). (Palaeomagnetic evidence supports this age).   cf. Mt Tennyson (Yetholme) molybdenite dated at 330 +/- 40 Ma by Re-Os technique (Hirt et al., 1963) and granite at Hartley (part of Bathurst batholith) dated at 310 & 320 Ma by K-Ar technique (Evernden & Richards, 1962; recalculated by Cas et al., 1976).|16-MAY-23
5871|Durandal Adamellite|Comments|Notes:  The rock, although "granitic", contains approximately equal proportions of potash feldspar and plagioclase - hence the proposed name Adamellite (equivalent to a quartz monzonite). (In the sense that the Durandal Stock (Yetholme granite) does not include a rock type, the term "Durandal Adamellite" is considered to be at least a variation of a published name, and is perhaps a new name).  - This rock is mistakenly shown on the Bathurst 1:250 000 geological map as Duronal stock.|16-MAY-23
5871|Durandal Adamellite|References|79/00768;79/01414; 79/05442.|16-MAY-23
25889|Dyamberin Beds|Name source|Dyamberin Homestead (GR 5259 2568 Dorrigo 1:250 000).|16-MAY-23
25889|Dyamberin Beds|Unit history|Binns (1966). Granitic intrusions and regional metamorphic rocks of Permian age from the Wongwibinda Fault the Dyamberin Beds but did not define the unit.|16-MAY-23
25889|Dyamberin Beds|Type section locality|Kangaroo Creek from GR 5232 2568 (Dorrigo 1:250 000) to its junction with the Aberfoyle River. Type Section: None designated - see comments in THICKNESS.|16-MAY-23
25889|Dyamberin Beds|Extent|The Dyamberin Beds occupy an area of approximately 800 km2 in the southern part of the region between the Demon Fault and the Wongwibinda Fault.|16-MAY-23
25889|Dyamberin Beds|Thickness range|The presence of folding and slaty cleavage, and the absence of continuous outcrop hinders determination of thickness, but the steep dip of bedding planes to the north suggests a thickness of several thousand metres.|16-MAY-23
25889|Dyamberin Beds|Lithology|Interbedded greywackes, siltstones and mudstones with horizons of diamictite. In places a well developed cleavage occurs in slates. Diamictite with either a sandy or muddy matrix is more abundant than orthoconglomerates. Voisey (1950) also recorded tuff and acid lava flows.|16-MAY-23
25889|Dyamberin Beds|Fossils|Deltopecten illawarensis (Morris) fenestrate polyzoans. Trigonotreta sp. A Fletcherithyris sp. Ind   Described by Runnegar (1970).|16-MAY-23
25889|Dyamberin Beds|Relationships and boundaries|The Dyamberin Beds are bounded on the west by the Wongwibinda Fault, and on the east by the Demon Fault. To the south they are intruded by the Round Mountain Leucoadamellite and overlain by the Cainozoic Ebor basalts. To the north they are conformably overlain by the Sara Beds. Example contact of Sara and Dyamberin Beds occurs at GR 5347 2732 Dorrigo 1:250 000.|16-MAY-23
25889|Dyamberin Beds|Age reasons|Runnegar (1970) listed the above fossils from Kangaroo Creek (GR 5249 2622) as being indicative of an Early Permian age.|16-MAY-23
25889|Dyamberin Beds|References|79/03754; |16-MAY-23
21727|Easter Monday beds|Name source|Easter Monday Goldfield, centred on GR 594700E 6743400N, Olive Downs 1:100 000 sheet (7239).|16-MAY-23
21727|Easter Monday beds|Type section locality|REFERENCE SECTION : Neither the top nor the base of the unit are exposed, hence the rocks are referred to as 'beds'., and no type section can be nominated.  A cross-section of all the identified facies exists between GR 592200E 6744800N and 5980000E 6746600N, Olive Downs 1:100 000 sheet (7239).|16-MAY-23
21727|Easter Monday beds|Extent|Occupies the whole of Tibooburra Inlier, part from the Tiboburra Granodiorite.|16-MAY-23
21727|Easter Monday beds|Thickness range|Uncertain; estimated to be 2-3km.|16-MAY-23
21727|Easter Monday beds|Lithology|Phyllitic pelite, metasiltstone and siliciclastic metasandstone, with minor conglomerate and calcareous sandstone.  Contains one thick (25-30m) unit of reworked acid tuff and two thin (0.1-2.5m) basaltic sills or flows.|16-MAY-23
21727|Easter Monday beds|Age reasons|Cambrian or Early Ordovician|16-MAY-23
21727|Easter Monday beds|Defn Reference|SOURCE OF DEFINITION: Thalhammer, O.A.R., Stevens, B.P.J., Gibson, J.H., and Grum, W. 1998. Tibooburra granodiorite, western New South Wales: emplacement history and geochemistry. Australian Journal of Earth Sciences 45, 775-787,  Appendix.|16-MAY-23
27147|Emerald Beach Adamellite|Name source|Coastal Resort of Emerald Beach (GR 6305 2619 Coffs Harbour 1:250 000).|16-MAY-23
27147|Emerald Beach Adamellite|Unit history|New name, has been described but not defined, by Korsch (1971).|16-MAY-23
27147|Emerald Beach Adamellite|Type section locality|Unnamed headland between Bare Bluff and Signal Hill (GR 6311 2630 Coffs Harbour 1:250 000)|16-MAY-23
27147|Emerald Beach Adamellite|Extent|A small intrusion occurring only on an unnamed headland between Bare Bluff and Signal Hill at GR 6311 2630 (Coffs Harbour 1:250 000).|16-MAY-23
27147|Emerald Beach Adamellite|Lithology|Slightly-porphyritic medium-grained adamellite.|16-MAY-23
27147|Emerald Beach Adamellite|Relationships and boundaries|The stock intrudes the Coramba Beds producing biotite-grade hornfels.|16-MAY-23
27147|Emerald Beach Adamellite|Age reasons|Unknown, possibly Late Palaeozoic-Early Mesozoic. It intrudes the Coramba Beds of probable Late Palaeozoic, possibly Carboniferous age.|16-MAY-23
27147|Emerald Beach Adamellite|References|79/02435|16-MAY-23
6353|Euglo Formation|Name source|Euglo Trig Station.|16-MAY-23
6353|Euglo Formation|Type section locality|Burcher-Ungarrie road. Lower contact does not outcrop. Upper contact sharp with Ugalong Dacite. 515859 (bottom) to 510859 (top) Forbes 1:250 000.|16-MAY-23
6353|Euglo Formation|Extent|Several km2 along Burcher-Ungarrie road.|16-MAY-23
6353|Euglo Formation|Thickness range|About 3000 m.|16-MAY-23
6353|Euglo Formation|Lithology|Sandstones, fine siltstones, possibly rhyolitic tuffs. Uniform, without prominent bedding.|16-MAY-23
6353|Euglo Formation|Relationships and boundaries|Lower boundary does not outcrop. Upper contact with Ugalong Dacite structurally unclear.|16-MAY-23
6353|Euglo Formation|Age reasons|Probably Early Devonian from regional considerations.|16-MAY-23
6353|Euglo Formation|Proposed publication|Bulletin Australian Society of Exploration Geophysicists (v.7 No. 1).|16-MAY-23
6353|Euglo Formation|References|79/00768; 79/01414; 79/05442.|16-MAY-23
37309|Eulowrie Pyroclastics|Name source|The name is derived from the Parish of Eulowrie, south of the junction of Rocky Creek and the Horton River (Eulowrie 1:25,000 sheet).|16-MAY-23
37309|Eulowrie Pyroclastics|Unit history|Eulowrie Pyroclastics (Opdyke et al. 2000).|16-MAY-23
37309|Eulowrie Pyroclastics|Geomorphic expression|Recessed because of the soft nature of the siltstone.|16-MAY-23
37309|Eulowrie Pyroclastics|Type section locality|The type section is located on the northern bank of Rocky Creek (GR407744 to 405744 Eulowrie 1:25,000 sheet), on the eastern limb of the Rocky Creek Syncline.|16-MAY-23
37309|Eulowrie Pyroclastics|Extent|Around the closure of the Rocky Creek Syncline at Rocky Creek with an extension along the western limb of the syncline southwards to the Llangollen Fault. In the Darthula block the pyroclastics have been mapped between GR283769 and 297739 (Grattai 1:25,000 sheet) on Gulf Creek in Berrygil State Forest, on and adjacent to the faulted axis of the Berrygil Anticline. Minor outcrops are also present in the southeastern part of the Dathula block in the vicinity of GR359574 Horton 1:25,000 sheet.|16-MAY-23
37309|Eulowrie Pyroclastics|Thickness range|23 m in the type section to >65 m in the sequence exposed on the western limb of the syncline along Rocky Creek.|16-MAY-23
37309|Eulowrie Pyroclastics|Lithology|The pyroclastics are a grey, green, pink or beige, laminated to thickly bedded, cherty, ash-rich siltstone. Constituents of the siltstone include remnants of shards, and scattered fine grains of feldspar, quartz and pumice. The groundmass can be either silty or have a micropoikilitic texture, reflecting an original glassy nature. Slumps and sandstone dykes characterise the upper part of the section on the western limb of the syncline at Rocky Creek. Small scale ripples and preferential distribution of larger grains within certain laminations indicate transport by water.|16-MAY-23
37309|Eulowrie Pyroclastics|Depositional environment|Fluvial resedimented siltstone|16-MAY-23
37309|Eulowrie Pyroclastics|Relationships and boundaries|The Eulowrie Pyroclastics constitute the basal unit within part of the Lark Hill Formation.|16-MAY-23
37309|Eulowrie Pyroclastics|Age reasons|Carboniferous (Namurian). A SHRIMP (SL13) age for the pyroclastics is 310.6+/-4.0 Ma (Opdyke et al. 2000).|16-MAY-23
37309|Eulowrie Pyroclastics|References|OPDYKE N.D., ROBERTS J., CLAOUE-LONG J., IRVING E. & JONES P.J. 2000. Base of the Kiaman: Its definition and global stratigraphic significance. Geological Society of America Bulletin 112, 1315-1341.|16-MAY-23
25902|Eusdale Adamellite|Name source|The property "Eusdale" (near Yetholme, NSW), used by Mackay (1964).|16-MAY-23
25902|Eusdale Adamellite|Unit history|Formerly known but not formalised, as the Yetholme Granite (Eusdale Stock) (Mackay, 1964).|16-MAY-23
25902|Eusdale Adamellite|Type section locality|Road cutting 0.3 km long at GR 278866 Bathurst 1:250 000 Sheet area (latitude 33o27'S, longitude 149o49'E. (This is an associated satellite body).|16-MAY-23
25902|Eusdale Adamellite|Extent|The adamellite is exposed over approximately 15 km2 as a stock just east of Yetholme.|16-MAY-23
25902|Eusdale Adamellite|Lithology|Adamellite, massive, coarse-grained grey with large pink potash feldspar megacrysts; contains xenoliths; minor pegmatite lenses; cut by aplite veins (and dolerite (?) and microdiorite dykes). Minor sulphide mienrals, including molybdenite, are present in the Durandal Adamellite.|16-MAY-23
25902|Eusdale Adamellite|Relationships and boundaries|Thought to be related to, or part of, the Bathurst batholith which outcrops approximately 2 km south of the adamellite (Mackay, 1964; Watts, 1969; Facer, 1976). Intrudes Silurian and Devonian rocks of the Hill End Trough and Capertee Rise, and cuts across structures within those rocks. May be a separate exposure of the one rock body represented by the Durandal Adamellite (q.v. - new name) and the Eusdale Adamellite.|16-MAY-23
25902|Eusdale Adamellite|Age reasons|Durandal Adamellite dated by K-Ar technique (biotite) at 309 +/- 8 Ma, and 312 +/- 8 Ma; aplite and contact adamellite dated by Rb-Sr technique (whole rock) at 324 +/- 17 Ma; (Rb87  = 10-11/y) "Dolerite" (microdiorite) within Durandal Adamellite dated by K-Ar technique (whole rock) at 298 +/- 10 Ma. Reference: Facer (1976). (Palaeomagnetic evidence supports this age).   cf. Mt Tennyson (Yetholme) molybdenite dated at 330 +/- 40 Ma by Re-Os technique (Hirt et al., 1963) and granite at Hartley (part of Bathurst batholith) dated at 310 & 320 Ma by K-Ar technique (Evernden & Richards, 1962; recalculated by Cas et al., 1976).|16-MAY-23
25902|Eusdale Adamellite|Proposed publication|Proceedings of the Linnean Society of New South Wales|16-MAY-23
25902|Eusdale Adamellite|Comments|Notes: The rock, although "granitic", contains approximately equal proportions of potash feldspar and plagioclase - hence the proposed name Adamellite (equivalent to a quartz monzonite). (In the sense that the Eusdale Stock (Yetholme granite) of Mackay (1964) does not include a rock type and has not been published the term "Eusdale Adamellite" is a new name).    -  This rock is mistakenly shown on the Bathurst 1:250 000 geological map as Eusdah stock.|16-MAY-23
24976|Fencers Creek Conglomerate|Name source|Fencers (or Splitters) Creek exposes the most accessible section of the conglomerate, and is near to a typical section. Access from track paralleling Creek from Hume Highway.|16-MAY-23
24976|Fencers Creek Conglomerate|Type section locality|East-west section GR 094822 to GR 112822, 1.4 km north of Ginger Beer Creek. Full sequence exposed. Access via "Strathallan" homestead off Hume Highway.|16-MAY-23
24976|Fencers Creek Conglomerate|Extent|North-South trend. Extends from GR 102938, 2.8 km NW of Wambidgee Siding in the north to GR 10076, within 0.1 km of the southern boundary of the sheet, a distance of 15.8 km. Maximum thickness of 1.7 km west of Mingay. (GRs in yards - Coolac 1:50 000 sheet).|16-MAY-23
24976|Fencers Creek Conglomerate|Thickness range|a) At type section: 1.65 km;  b) Maximum known: 1.7 km (west of Mingay) 0.4 km north of type section.|16-MAY-23
24976|Fencers Creek Conglomerate|Lithology|Stretch pebble conglomerate (mainly in the south), cobble conglomerate, chert pebble conglomerate, granule conglomerate, with minor interbedded lithic sandstone, phyllite and claystone.|16-MAY-23
24976|Fencers Creek Conglomerate|Fossils|Crinoidal Limestone occurs at GR 104760 within phyllites interbedded with conglomerate.|16-MAY-23
24976|Fencers Creek Conglomerate|Relationships and boundaries|Boundaries usually sharply defined by presence of conglomerate which forms strong strike ridges, topographically higher than enclosing undifferentiated volcanic sediments, sediments and foliated and altered acid to acid intermediate porphyries of the western Blowering Beds.|16-MAY-23
24976|Fencers Creek Conglomerate|Age reasons|Middle to Late Silurian. (Same age as for the Blowering Beds which unconformably overlie the Jindalee Beds [Late Cambrian to Late Ordovician] and are overlain unconformably by the Devonian Hervey Group).|16-MAY-23
24976|Fencers Creek Conglomerate|Proposed publication|Geology of the Cootamundra 1:100 000 (Geological Survey of NSW in prep.)|16-MAY-23
24976|Fencers Creek Conglomerate|Name first published by|Geological Survey of NSW, 1975.|16-MAY-23
26548|Fernleigh Group|Name source|"Fernleigh" property, GR 583225, Braidwood 1:100 0000 sheet.|16-MAY-23
26548|Fernleigh Group|Constituents|Burburba Formation (Felton & Huleatt, 1975) Windellama Limestone (Pickett & Huleatt, 1971) Jacqua Formation (Felton & Huleatt, 1975).|16-MAY-23
26548|Fernleigh Group|Extent|The unit is exposed over about 20 km2 in the northeast part of the Braidwood 1:100 000 sheet and the southeast part of the Goulburn 1:100 000 sheet, in the vicinity of Windellama school (GR 585220, Braidwood 1:100 000 sheet).|16-MAY-23
26548|Fernleigh Group|Thickness range|At least 1700 m.|16-MAY-23
26548|Fernleigh Group|Lithology|Quartz arenite and siltstone (Burburba and Jacqua Formations); fine to coarse tuffaceous arenite (Burburba Formation), dolomitic and siliceous fossiliferous limestone (Windellama Limestone).|16-MAY-23
26548|Fernleigh Group|Relationships and boundaries|The unit is faulted against Silurian sediments to the west. Its southern and eastern boundaries with terrigenous sediments of Silurian or Ordovician age are concealed by alluvium but faulting along these boundaries is inferred (see Mawson, 1975). The extent of the unit northwards is not known.|16-MAY-23
26548|Fernleigh Group|Age reasons|The Windellama Limestone contains rich macro- and micro-faunas of Late Siegenian to early Emsian age (Early Devonian) (see Pickett & Huleatt, 1971; Mawson 1975 for complete faunal lists). The Burburba Formation contains, inter alia, the trilobite Cheirurus (Crotalocephalides) gaertneri (Alberti) whose age is Praguian (Mawson, 1975).|16-MAY-23
26548|Fernleigh Group|Proposed publication|Felton E.A. and Huleatt M.B., 1975. Geology of the Braidwood 1:100 000 Sheet. Geol. Survey NSW Sydney.|16-MAY-23
26548|Fernleigh Group|References|79/02822; 79/03409.|16-MAY-23
26548|Fernleigh Group|Name first published by|Felton E.A., Huleatt M.B., 1977.|16-MAY-23
25003|Gibraltar Adamellite|Name source|From Gibraltar Hill (897m), 3 km east of Bungendore.|16-MAY-23
25003|Gibraltar Adamellite|Unit history|None.|16-MAY-23
25003|Gibraltar Adamellite|Type section locality|Bouldery and pavement outcrops of foliate adamellite at and near Gibraltar Hill GR 255/945 (Canberra 1:100 000 sheet 8727).|16-MAY-23
25003|Gibraltar Adamellite|Extent|Crops out over an area of about 2 km2.  The intrusion is elongated meridionally and forms a prominent wooded ridge extending about 3km south from the Kings Highway.|16-MAY-23
25003|Gibraltar Adamellite|Lithology|The main rock type is a medium to coarse grained biotite adamellite with discoidal mafic-rich xenoliths. A strong foliation is concordant with the regional cleavage in surrounding country rocks. The adamellite is composed of plagioclase, perthitic K-feldspar, aggregates of polygonal fine-grained quartz and laths of fresh biotite. A few brown euhedral grains of allanite confirm the intrusion is I-type.|16-MAY-23
25003|Gibraltar Adamellite|Age reasons|Intrudes Late Ordovician metasediments. It is probably related to and therefore of a similar age as the strongly foliated Early Devonian Ellenden Granite and Rossi Granodiorite.|16-MAY-23
7218|Gilgai Granite|Name source|Township of Gilgai; Inverell 1:250 000 sheet, GR 4127 3023).|16-MAY-23
7218|Gilgai Granite|Type section locality|A type area is represented at GR 4129 2959 and a reference area is at GR 4037 2851, Inverell 1:250 000 Sheet. Overall the body is the most resistant pluton in the area and has a rough topography with exposures of sheets and tors.  |16-MAY-23
7218|Gilgai Granite|Extent|This unit is exposed on the Inverell and Manilla 1:250 000 Sheets. It has a crescent shape covering an outcrop area 30,900 ha and is centered about the township of Gilgai.|16-MAY-23
7218|Gilgai Granite|Lithology|Granite, equigranular; leucocratic (Modal Colour Index average 1.9). The full Chayes description is b11 (213)4 . Alkali feldspars>quartz>plagioclase. Mafic minerals include biotite and chlorite. Accessory minerals include apatite, iron oxides, monzonite, white mica. No hornblende or sphene.|16-MAY-23
7218|Gilgai Granite|Relationships and boundaries|Gilgai Granite underlies and intrudes the Tingha Adamellite. The Oakey Creek Granite forms the western boundary and an undifferentiated leucoadamellite forms the southern boundary.|16-MAY-23
7218|Gilgai Granite|Age reasons|Gilgai Granite date by Rb/Sr methods as 230 x 106 y. (Late Permian).|16-MAY-23
7218|Gilgai Granite|Proposed publication|Molybdenum in NSW (Mineral Resources 43, geol. Survey NSW) Weber C.R., Paterson I.B.L., and Townsend D.J.|16-MAY-23
7218|Gilgai Granite|Defn Reference|80/21173|16-MAY-23
7218|Gilgai Granite|Name first published by|Korsch R.J., 1977|16-MAY-23
25011|Girrakool Beds|Name source|Girrakool Homestead (GR 5008 2408 Dorrigo 1:250 000).|16-MAY-23
25011|Girrakool Beds|Unit history|Lyndhurst Beds (Binns 1966; Packham 1969). The name Lyndhurst is invalid because the Lyndhurst Formation in South Australia has priority and hence the alteration to Girrakool Beds.|16-MAY-23
25011|Girrakool Beds|Type section locality|The Girrakool Beds are well exposed along Rockvale Creek from GR 4954 2449 to where the sediments are intruded by the Rockvale Adamellite-Granodiorite at GR 5000 2386. Type section not designated.|16-MAY-23
25011|Girrakool Beds|Extent|The Girrakool Beds occupy an area of approximately 600 km2 to the north and east of Armidale extending to Wollomombi in the east.|16-MAY-23
25011|Girrakool Beds|Thickness range|A large area of the Girrakool Beds has been overturned and has suffered two to three deformations. The intense folding has made the measuring of a section impracticable and hence no estimate of the thickness can be given.|16-MAY-23
25011|Girrakool Beds|Lithology|Indurated mudstones, siltstones and lithic to feldspathic greywackes of volcanic derivation.|16-MAY-23
25011|Girrakool Beds|Fossils|Atomodesma sp.|16-MAY-23
25011|Girrakool Beds|Relationships and boundaries|The Girrakool Beds are intruded by the Hillgrove Adamellite in the south and by the Tobermory Adamellite and associated granitic plutons  in the north. The beds become increasingly metamorphosed to the east until the Glen Bluff Fault is reached. To the west unsuccessful efforts have been made by the author and others to define the contact between the Girrakool Beds and the Sandon Beds in the vicinity of Armidale. The line of contact seems to be defined only by gross changes in lithology, notably a rapid decrease in the amount of chert in passing from the Sandon Beds to the Girrakool Beds.|16-MAY-23
25011|Girrakool Beds|Age reasons|R.J. Gunthorpe found fossil fragments near Rockvale Homestead which were determined by Runnegar (1970) as Atomodesma sp. indicating a Permian age.|16-MAY-23
25011|Girrakool Beds|Defn author|Korsch R.J., 1978|16-MAY-23
25011|Girrakool Beds|References|01/31574; 79/03754|16-MAY-23
37305|Glen Idle Rhyolite|Name source|The property `Glen Idle' GR372657 Eulowrie 1:25,000 sheet|16-MAY-23
37305|Glen Idle Rhyolite|Unit history|Named informally by Hocking (1973)|16-MAY-23
37305|Glen Idle Rhyolite|Type section locality|GR381652 Eulowrie 1:25,000 sheet on the lower western slope of Round Mountain (GR426656 Eulowrie 1:25,000 sheet).|16-MAY-23
37305|Glen Idle Rhyolite|Extent|Crops out for 1.25 km on the western limb of the Rocky Creek Syncline, mid-way between Trevallyn (GR374563 Horton 1:25,000 sheet) and Rocky Creek.|16-MAY-23
37305|Glen Idle Rhyolite|Thickness range|7 m|16-MAY-23
37305|Glen Idle Rhyolite|Lithology|Buff unwelded ignimbrite with scattered plagioclase, biotite, rare opaque minerals and glassy or brown volcanic rock fragments; groundmass micropoikilitic and containing coarse, zeolitised shards and bubble walls.|16-MAY-23
37305|Glen Idle Rhyolite|Depositional environment|Ignimbrite|16-MAY-23
37305|Glen Idle Rhyolite|Relationships and boundaries|Underlies the Peri Rhyolite within this limited part of the Clifden Formation.|16-MAY-23
37305|Glen Idle Rhyolite|Age reasons|Carboniferous (Namurian).|16-MAY-23
37305|Glen Idle Rhyolite|References|HOCKING R.M. 1973. The Carboniferous Back Creek-Pound Creek sequence, southwest of Caroda, New South Wales. BSc (Hons) thesis, University of new England, Armidale (unpubl.).|16-MAY-23
7543|Good Good Adamellite|Name source|Good Good homestead GR 098212, Michelago 1:100 000 Geological Sheet.|16-MAY-23
7543|Good Good Adamellite|Unit history|Both Richards (1967) and Slepecki (1973) mapped the adamellite but did not name it.|16-MAY-23
7543|Good Good Adamellite|Type section locality|No type area is defined.|16-MAY-23
7543|Good Good Adamellite|Description at type locality|It is a medium-grained adamellite consisting of microperthite, plagioclase, quartz, abundant tourmaline (schorlite) and minor muscovite.|16-MAY-23
7543|Good Good Adamellite|Extent|The adamellite consists of two small bodies which lie at the head of a tributary creek of Ryans (Wangrah) Creek at approximately GR 088238. The adamellite lies 1.6 km west of the Sapling Flat Igneous Complex and 3.2 km east of the southern Michelago granitic body.  Size: The larger western body covers some 0.27 km2 and the eastern body some 0.08 km2.|16-MAY-23
7543|Good Good Adamellite|Relationships and boundaries|Late Ordovician Foxlow Beds completely surround the adamellite.|16-MAY-23
7543|Good Good Adamellite|Age reasons|The adamellite would appear to be emplaced at the close of the Silurian Period.|16-MAY-23
7543|Good Good Adamellite|Proposed publication|Geological Survey of NSW 1:100 000 Note Series.|16-MAY-23
7556|Googong Adamellite|Name source|From old 'Googong homestead' now covered by the Googong Reservoir.|16-MAY-23
7556|Googong Adamellite|Unit history|Googong Granite (Stauffer, 1967).|16-MAY-23
7556|Googong Adamellite|Type section locality|Moderately weathered buff coloured adamellite is well exposed in cuttings on the road between the Googong Foreshore office and the dam (Canberra 1:100 000 sheet 8727). There is a sharp dipping contact at GR 048/781 where the adamellite has veined and silicified dark-grey foliated dacitic ignimbrite.|16-MAY-23
7556|Googong Adamellite|Extent|Covers an area of about 3 km2 west of Googong Dam. It has an inverted U-shaped outcrop pattern making a negative topographic feature since it is fully enclosed by more resistant dacitic ignimbrite.|16-MAY-23
7556|Googong Adamellite|General description|It is a medium to coarse-grained porphyritic adamellite. The rock contains phenocyrsts of quartz, perthitic potash feldspar, plagioclase, biotite with accessory apatite, epidote, zircon and allanite. Dacitic xenoliths are found within the intrusion; pegmatite and quartz-epidote veins occur in the surrounding country rock.|16-MAY-23
7556|Googong Adamellite|Age reasons|A Late Silurian (possibly post Ludlovian) age for the Googong Adamellite is evident from an intrusive and faulted relationship with the Colinton Volcanics. the presence of hornblende (Stauffer 1964) and allanite suggest I-type affinities.  The intrusion is probably co-magmatic with the Barracks Creek Adamellite.|16-MAY-23
7890|Gundamulda Creek Beds|Name source|Gundamulda Creek; GR 3800 2850 to 3775 2775 (Manilla 1:250 000 Sheet, SH 56-9).|16-MAY-23
7890|Gundamulda Creek Beds|Unit history|The Gundamulda Creek Beds are equivalent to the "Brandy Springs Beds" (Heugh, 1971), the "Bundarra Beds" (Lusk, 1964) and the unnamed "O-Dz" unit of Pogson and Hitchins, 1973).|16-MAY-23
7890|Gundamulda Creek Beds|Type section locality|In a NNW-trending tributary of Gundamulda Creek which meets the Keera Road about 1.5 km from the Gulf Creek-Bundarra Road turnoff, near GR 3790 2600 (Manilla 1:250 000).|16-MAY-23
7890|Gundamulda Creek Beds|Extent|The unit occurs in a belt approximately 150 km long and up to 13 km wide extending from about 20 km S of Warialda to about 20 km N of Tamworth; and in a fault block about 80 km x 20 km extending from about 20 km W to 70 km S of Walcha.|16-MAY-23
7890|Gundamulda Creek Beds|Thickness range|In excess of 1500 m are represented at the type section, and a maximum of 12 000 m apparent thickness with no allowance made for the bedding plane slippage and imbricate thrusting likely in the structural setting of the formation.|16-MAY-23
7890|Gundamulda Creek Beds|Lithology|Predominantly composed of laminated siltstones with thin chert and graded arenaceous bands, greywackes, and minor argillite, chert and jasper.|16-MAY-23
7890|Gundamulda Creek Beds|Relationships and boundaries|The Gundamulda Creek Beds conformably underlie the Woolomin Beds. The top of the Gundamulda Creek Beds is defined by the first appearance of abundant jasper or metabasalt of the redefined Woolomin Beds ocean basin sequence (see Pogson & Hitchins, 1973; and NSW Geological Survey Silurian Lexicon). This definition does not agree with the tectonic interpretation of Scheibner (1973) who proposed that the flysch sequence (Gundamulda Creek Beds) should overlie the ocean basin sequence (Woolomin Beds). The relationship observed by Lusk (1961 and 1964) may be due to transgression and regression of the flysch and ocean basin deposits, with Lusk fortuitously only observing contact relationships at the base of transgressions of ocean basin sediment over flysch. More detailed fieldwork is necessary to test this hypothesis.|16-MAY-23
7890|Gundamulda Creek Beds|Age reasons|Faunas of significance are restricted to rare limestone lenses. Lusk (1964) listed favositids, bryozoans, stromatoporoids, Spongophyllum sp., and Halysites sp. indicating a Silurian age, at least in part. The limestones are probably blocks slumped into the deeper water flysch sequence, and the unit may be younger than the enclosed fossils. The unit also contains radiolarians and rare carbonaceous plant remains.|16-MAY-23
7890|Gundamulda Creek Beds|Proposed publication|NSW Geological Survey Silurian Lexicon to be published as a Record of the Geological Survey of NSW (in prep.).|16-MAY-23
7890|Gundamulda Creek Beds|Name first published by|Scheibner E., 1976.|16-MAY-23
7907|Gungoandra Siltstone Member|Name source|Gungoandra Gap; GR 976245, Michelago 1:100 000 Sheet area.|16-MAY-23
7907|Gungoandra Siltstone Member|Unit history|Previously unnamed.|16-MAY-23
7907|Gungoandra Siltstone Member|Type section locality|Basal unit in type section of Ryrie Formation.|16-MAY-23
7907|Gungoandra Siltstone Member|Extent|As for the Ryrie Formation.|16-MAY-23
7907|Gungoandra Siltstone Member|Thickness range|150 m near Colinton Hill.|16-MAY-23
7907|Gungoandra Siltstone Member|Lithology|Fine-grained, yellow-brown to grey-brown siltstone frequently with conchoidal fracturing and iron staining. It has relatively few sedimentary structures with only a minor amount of cross-bedding and ripple marking.|16-MAY-23
7907|Gungoandra Siltstone Member|Relationships and boundaries|The siltstone member unconformably overlies Late Ordovician Foxlow Beds. It is conformable with the remainder of the Ryrie Formation.|16-MAY-23
7907|Gungoandra Siltstone Member|Age reasons|As for the Ryrie Formation.|16-MAY-23
7907|Gungoandra Siltstone Member|Proposed publication|Geological Survey of NSW 1:00 000 Note Series.|16-MAY-23
24308|Hell Hole Creek Adamellite|Name source|Hell Hole Creek; GR 450420, Tantangara 1:100 000 Sheet area.|16-MAY-23
24308|Hell Hole Creek Adamellite|Type section locality|A grassy area on Hell Hole Creek at GR 449418. Scattered boulders of granite up to 2 m diameter crop out.|16-MAY-23
24308|Hell Hole Creek Adamellite|Extent|A sub-circular intrusion about 1 km across within the Hell Hole Creek drainage basin.|16-MAY-23
24308|Hell Hole Creek Adamellite|Lithology|Hornblende-biotite granodiorite.|16-MAY-23
24308|Hell Hole Creek Adamellite|Relationships and boundaries|Intrudes and hornfelses the Early Silurian Tantangara Beds.|16-MAY-23
24308|Hell Hole Creek Adamellite|Age reasons|Early Devonian because of similarity with the Early Devonian Coolamine Igneous Complex.|16-MAY-23
24308|Hell Hole Creek Adamellite|Defn Reference|80/21203, 83/24087|16-MAY-23
24308|Hell Hole Creek Adamellite|Proposer|Owen M., Wyborn D.|16-MAY-23
25960|Jacqua Formation|Name source|Jacqua Creek, GR 670306, Goulburn 1:100 000 sheet, a tributary of Nerrimunga Creek, GR 661220, Braidwood 1:100 000 sheet.|16-MAY-23
25960|Jacqua Formation|Type section locality|200 m of fine-grained thinly bedded quartz arenite and siltstone, minor tuffaceous arenite, exposed in Windellama Creek between GR 630227 and GR 633227, Braidwood 1:100 000 sheet.|16-MAY-23
25960|Jacqua Formation|Extent|Exposed over about 0.5 km2 west of the Bungonia-Windellama road, about 3 km north of Windellama Hall (GR 622205, Braidwood 1:100 000 sheet).|16-MAY-23
25960|Jacqua Formation|Thickness range|Maximum exposed thickness 220 m.|16-MAY-23
25960|Jacqua Formation|Lithology|Grey to buff fine-grained quartz arenite and siltstone, cream tuffaceous arenite.|16-MAY-23
25960|Jacqua Formation|Relationships and boundaries|All boundaries of this unit are concealed by alluvium. Attitude of the beds is similar to that of the Windellama Limestone, which is inferred to conformably overlie this unit. Undifferentiated sediments of Ordovician to Silurian age, with markedly different bedding attitudes and degree of deformation to the Jacqua Formation, may be faulted against the formation (Mawson, 1975).|16-MAY-23
25960|Jacqua Formation|Age reasons|The Jacqua Formation contains Howellella sp. and other indeterminate brachiopods, corals and crinoid stems (Mawson, 1975). Its age is therefore Early Devonian.|16-MAY-23
25960|Jacqua Formation|Proposed publication|Felton E.A., Huleatt M.B., 1975. Geology of the Braidwood 1:100 000 sheet. Geol. Surv. NSW, Sydney.|16-MAY-23
25960|Jacqua Formation|Name first published by|Felton E.A., Huleatt M.B., 1977|16-MAY-23
24320|Jinden Adamellite|Name source|The name comes from Jinden Creek which crosses the centre of the adamellite and flows into the Shoalhaven River at GR 383299.|16-MAY-23
24320|Jinden Adamellite|Unit history|Included as part of the Boro Granite by previous workers, however the Boro mass is a separate body in the Braidwood 1:100 000 sheet area to the north.|16-MAY-23
24320|Jinden Adamellite|Type section locality|Exposures in the bed of Jinden Creek at GR 364268.|16-MAY-23
24320|Jinden Adamellite|Extent|Between Jerrabattgulla Creek and the upper reaches of the Shoalhaven River, east of the Shoalhaven Fault. Occupies about 185 km2.|16-MAY-23
24320|Jinden Adamellite|Lithology|Quite a large variation in rock types, but this variation can be explained in terms of crystal fractionation and local magma segregation of a single magma body. The intrusion is an adamellite with about 10% mafic minerals near its margin, and carries distinctive hornblende phenocrysts. Further from the margins the rock is lighter (5-6% mafics) and even grained (2-3 mm). Aplitic dykes and leucogranite bodies are common throughout the Jinden Adamellite. In places the leucogranites grade into the normal adamellite. Elsewhere there are sharp contacts.B2|16-MAY-23
24320|Jinden Adamellite|Age reasons|Early Devonian - intrudes the co-magmatic Late Silurian Long Flat Volcanics. K/Ar biotite age 406 +/- 6 Ma, Rb/Sr biotite/whole rock isochron age of 402 +/- 6 Ma with initial ratio of 0.7071.|16-MAY-23
24320|Jinden Adamellite|Resdate|26-MAY-1982|16-MAY-23
24320|Jinden Adamellite|Reserved? Yes/No|Yes|16-MAY-23
25691|Kain Porphyry|Name source|Kain homestead - GR 325423|16-MAY-23
25691|Kain Porphyry|Type section locality|Tors west of the road at GR 348413.|16-MAY-23
25691|Kain Porphyry|Extent|Between Gundillion and Nithsdale in the Shoalhaven River valley.|16-MAY-23
25691|Kain Porphyry|Lithology|A strongly porphyritic (50-60% phenocrysts) high level intrusion within the Long Flat Volcanics. Phenocrysts of plagioclase quartz and widely scattered pink alkali feldspar are up to 10 mm across. Mafic phenocrysts up to 2 x 1 mm include biotite, pyroxene and a little brown or greenish brown hornblende. Microgranitic groundmass ranges in grain size from 0.05 mm to 0.3 mm.|16-MAY-23
25691|Kain Porphyry|Age reasons|Late Silurian or possibly early Devonian - intrudes the Long Flat Volcanics and is in turn intruded by the Jinden Adamellite.|16-MAY-23
25691|Kain Porphyry|Comments|Metamorphism: Most of the Kain Porphyry has been altered by low grade burial metamorphism, the most prominent effect being the albitization of plagioclase phenocrysts.|16-MAY-23
25691|Kain Porphyry|Resdate|17-JUN-1982|16-MAY-23
25691|Kain Porphyry|Reserved? Yes/No|Yes|16-MAY-23
9400|Kellys Creek Leucoadamellite|Name source|Kelleys Creek, which enters the Nymboida River in the western half of the pluton at GR 5819 2724 (Dorrigo 1:250 000).|16-MAY-23
9400|Kellys Creek Leucoadamellite|Unit history|Previously undescribed.|16-MAY-23
9400|Kellys Creek Leucoadamellite|Type section locality|The vicinity of Kellys Creek where it cuts the intrusion.|16-MAY-23
9400|Kellys Creek Leucoadamellite|Extent|A subcircular intrusion cropping out over an area of about 35 km2 approximately 30 km south of Nymboida.|16-MAY-23
9400|Kellys Creek Leucoadamellite|Lithology|Two textural variants of leucoadamellite: 1) coarse-grained porphyritic rock with phenocrysts up to 10 mm in a fine-grained groundmass; 2) coarse (5-8 mm) to fine (0.5-1 mm) even-grained leucoadamellite.|16-MAY-23
9400|Kellys Creek Leucoadamellite|Relationships and boundaries|The pluton occurs completely within the Coramba Beds and has produced a contact aureole of biotite-cordierite hornfels.|16-MAY-23
9400|Kellys Creek Leucoadamellite|Age reasons|Unknown, but intrudes the Coramba Beds which is postulated to be Late Palaeozoic, possibly Carboniferous.|16-MAY-23
9400|Kellys Creek Leucoadamellite|Defn author|Korsch R.J., 1978.|16-MAY-23
29223|Kennedy Range Adamellite|Name source|Kennedy Range, GR 15555 6040 Currango 1:50 000 sheet area. Map no. 8626-IV.|16-MAY-23
29223|Kennedy Range Adamellite|Type section locality|6 km W of Peppercorn Hill at GR 402638 (Tantangara 1:100 000 sheet area).|16-MAY-23
29223|Kennedy Range Adamellite|Extent|The headwaters of Feints Creek over an area of about 4 km2.|16-MAY-23
29223|Kennedy Range Adamellite|Lithology|Hornblende-biotite adamellite and granite, aplite, hornfelsed granite.|16-MAY-23
29223|Kennedy Range Adamellite|Relationships and boundaries|Intrudes Goobarragandra Beds, intruded by a stock in the Micalong Swamp Basic Igneous Complex.|16-MAY-23
29223|Kennedy Range Adamellite|Age reasons|Late Silurian, bracketed by the Middle Silurian Goobarragandra Beds and the Late Silurian Micalong Swamp Basic Igneous Complex.|16-MAY-23
29223|Kennedy Range Adamellite|Defn Reference|83/24087|16-MAY-23
29223|Kennedy Range Adamellite|Proposer|Owen M., Wyborn D.|16-MAY-23
9616|Kingsfield Beds|Name source|Named after the property "Kingsfield", 982280, Scone 1:31 680 Sheet.|16-MAY-23
9616|Kingsfield Beds|Type section locality|Glenbawn area.  Location of Type Section: Measured along the bank of the Hunter River immediately downstream from Glenbawn Dam from 997278 to 998290, Scone 1:31 680 sheet.|16-MAY-23
9616|Kingsfield Beds|Extent|Known only from the core of the Brushy Hill Anticline west of Lake Glenbawn.|16-MAY-23
9616|Kingsfield Beds|Thickness range|a) At type Section: 130 m.  b) Maximum known:   130 m.|16-MAY-23
9616|Kingsfield Beds|Lithology|Crystal lithic tuffs, sporadic devitrified volcanics, probably originally ignimbrites, lithic sandstone, and purple shale.|16-MAY-23
9616|Kingsfield Beds|Relationships and boundaries|Base of unit unknown. The Kingsfield Beds are overlain, possibly unconformably, by the Dangarfield Formation; the boundary between the two formations is placed between unfossiliferous purple shale assigned to the Kingsfield Beds, and brown shale and thin-bedded sandstone with marine fossils assigned to the Dangarfield Formation.|16-MAY-23
9616|Kingsfield Beds|Age reasons|?Upper Devonian or lowermost Carboniferous. Fossils in the lower part of the overlying Dangarfield Formation are early Tournaisian in age.|16-MAY-23
9616|Kingsfield Beds|Defn author|Roberts J., Oversby B.S., 1974;  Mory A.,. 1978|16-MAY-23
9616|Kingsfield Beds|Proposed publication|BMR Bulletin|16-MAY-23
9616|Kingsfield Beds|Defn approved by|Copied from xerox sent by NSW Stratigraphic Nomenclature Sub-Committee|16-MAY-23
9616|Kingsfield Beds|Reserved? Yes/No|Roberts J., Oversby B.S.|16-MAY-23
24612|Kirribilli beds|Name source|Origin of name: The unit is named after "Kirribilli" station (GR 117064), 18 km east of Forbes.|16-MAY-23
24612|Kirribilli beds|Type section locality|Type Area and Distribution: The Kirribilli beds comprise a turbidite sequence which forms a broad belt of poor outcrops, 3-8 km wide, between Back Yamma State Forest (GR 130080) and Beargamil (GR 270450). The distance along strike is approximately 40 km.|16-MAY-23
24612|Kirribilli beds|Lithology|This unit consists of creamy brown, creamy olive green, pale-purple, and light-grey fine to medium-grained shales, slate, meta-psammite, and meta-greywacke (Mortimer 1981).|16-MAY-23
24612|Kirribilli beds|Relationships and boundaries|No contacts with other formations have been seen, other than a sheared contact with the Mugincoble Chert (Krynen et al. 1986), suggesting a faulted western boundary. The deformation of this unit is greater than that seen in other units in this area. Large exposures show chevron folding (GR 171201) and intense crenulation (GR 139185).|16-MAY-23
24612|Kirribilli beds|Age reasons|No internal evidence for age has been found, and the intense deformation is not favourable for preservation of fossils. Even an age relative to other units in the area is not definable because of the lack of any clear boundaries.|16-MAY-23
24612|Kirribilli beds|Proposer|Sherwin, Clarke & Krynen|16-MAY-23
24612|Kirribilli beds|Resdate|16-SEP-1987|16-MAY-23
24340|Koolambah Adamellite|Name source|Koolambah homestead at GR 020224, Michelago 1:100 000 Geological Sheet.|16-MAY-23
24340|Koolambah Adamellite|Unit history|Previously regarded as part of the Michelago Granite.|16-MAY-23
24340|Koolambah Adamellite|Type section locality|Typical representation to the southeast of Bundarra homestead, at GR 027235.|16-MAY-23
24340|Koolambah Adamellite|Description at type locality|Pale grey to white adamellite, coarse to medium-grained, enriched in quartz, hornblende and biotite; typically contains quartz, plagioclase, microcline, biotite and hornblende as well as minor opaques. Some varieties are subporphyritic. Some mafic-rich xenoliths, between 2.5 and 5 cms.|16-MAY-23
24340|Koolambah Adamellite|Extent|This is the major phase of the southern body of the Michelago Igneous Complex; it lies both to the north and south of the Bredbo-Jerangle road.  Size: 26 km2.|16-MAY-23
24340|Koolambah Adamellite|Relationships and boundaries|Intrudes Late Ordovician Foxlow Beds; Collingwood Fault displaces the adamellite from the northern body of the Michelago Igneous Complex.|16-MAY-23
24340|Koolambah Adamellite|Age reasons|Intruded at the close of the Silurian Period.|16-MAY-23
27177|Kowmung Volcaniclastics|Name source|Kowmung River (see Yerranderie 1:31 800 Topographic Sheet 8929-IV-N).|16-MAY-23
27177|Kowmung Volcaniclastics|Type section locality|The type section is along the Kowmung River from GR 075 889 to GR 053 902 (1:31 800 Yerranderie Topographic sheet). Another well-exposed representative section occurs in Cobra Creek, from GR 991 842 (1:31 800 Bindook Topographic Sheet 8929-IV-S) to 762 201 (1:25 000 Gurnang Topographic Sheet 8829-1-N).|16-MAY-23
27177|Kowmung Volcaniclastics|Extent|The unit is exposed over approximately 20 km2 as a triangular wedge beneath the Late Devonian Lambie Group in the Kowmung River and Murruin Creek area.|16-MAY-23
27177|Kowmung Volcaniclastics|Thickness range|Type section 770 m; Cobra Creek section 820 metres. Maximum preserved thickness is probably a little more than 1 km.|16-MAY-23
27177|Kowmung Volcaniclastics|Lithology|The formation is composed dominantly of coarse quartzo-feldspathic sandstones from a dacitic volcanic source. Boulder detritus and mudstones are lesser components. The grain size and sedimentation-unit size increase upwards to single sedimentation units more than 100 m thick containing boulders. Altered volcanic glass lenticles and allochthonous limestone blocks are also present.|16-MAY-23
27177|Kowmung Volcaniclastics|Relationships and boundaries|Overlies conformably mudstones and graded-bedded arenites equivalent to the Late Silurian Taralga Group (Scheibner, 1973). Its base is identifiable by the incoming of the first massive feldspathic sandstones above the mudstones and sandstones of the Taralga Group. It is overlain with medium-angle unconformity by the Late Devonian Lambie Group. The formation is thought to be related genetically to the Bindook Volcanic Complex (Scheibner, 1973). Revision of old terms:  The Kowmung Volcaniclastics is a mappable formation, formerly classified within the Bindook Volcanic Complex. Four informal members have been mapped, viz (bottom to top) the feldspathic-sandstone member, the silicic volcanic-breccia member, the boulder-conglomerate member and the lenticle-tuff member. The formation is composed dominantly of detritus likely to have been derived from the rhyodacitic to dacitic volcanic complexes near Yerranderie and Bindook, but as this relation needs to be demonstrated further, it is best mapped as a separate unit.|16-MAY-23
27177|Kowmung Volcaniclastics|Age reasons|Early to possibly Middle Devonian. Conodonts from limestone boulders from the base of the boulder conglomerate member are of earliest Devonian age (Quilty, pers. Comm). The overlying Lambie Group elsewhere contains brachiopods of Late Devonian, probably Frasnian age (Roberts et al., 1972), and conodonts of Frasnian age (Pickett, 1972). No other fossils have yet been recovered from the Kowmung Volcaniclastics.|16-MAY-23
27177|Kowmung Volcaniclastics|Proposed publication|Journal and Proceedings, Royal Society of NSW.|16-MAY-23
37196|Liscombe Pools Shale|Name source|Liscombe Pools Homestead.|16-MAY-23
37196|Liscombe Pools Shale|Unit history|Equivalent to "lower" Avoca Valley Shale of Ryall (1965) ("Upper" Avoca Valley Shale of Ryall (1965) is also modified to "Avoca Valley Shale").|16-MAY-23
37196|Liscombe Pools Shale|Type section locality|Licking Hole Creek, south of Liscombe Pools Homestead GR 1805 8450 Bathurst 1:150 000. On Liscombe Pools Property. |16-MAY-23
37196|Liscombe Pools Shale|Extent|Three separate tracts in the area bounded by 20-km SE, 15-km NE and 10-km W of Canowindra.|16-MAY-23
37196|Liscombe Pools Shale|Thickness range|a) At type section: 105 m.   B) Maximum known: 105 m.|16-MAY-23
37196|Liscombe Pools Shale|Lithology|Red, brown and green shales with a prominent buff graptolitic siltstone.|16-MAY-23
37196|Liscombe Pools Shale|Fossils|Monograptus priodor, M. aff vomerinus, ?M. spiralis, Retiolites geinitizianus.|16-MAY-23
37196|Liscombe Pools Shale|Relationships and boundaries|Conformably underlying Canowindra Porphyry and overlying Millambri Formation with conformity or minor disconformity.|16-MAY-23
37196|Liscombe Pools Shale|Age reasons|Late Llandovery to Early Wenlock based on fossils.|16-MAY-23
37196|Liscombe Pools Shale|Proposed publication|NSW Geological Survey Silurian Lexicon|16-MAY-23
37196|Liscombe Pools Shale|Defn approved by|Copied from xerox from NSW Sub-Committee.|16-MAY-23
37196|Liscombe Pools Shale|Name first published by|Percival I.G., 1976.|16-MAY-23
24362|Long Hill Diorite|Name source|Long Hill' homestead, GR 0045 8820 Blayney 1:50 000 (8730 - I & IV).|16-MAY-23
24362|Long Hill Diorite|Type section locality|In the vicinity of the Browns Creek mine GR 2133 8560, Bathurst 1:250 000. Area: Unit only mapped around the Browns Creek mine. Extent not determined.|16-MAY-23
24362|Long Hill Diorite|Description at type locality|Holocrystalline, medium-grained mesocratic rock consisting of sub-equal alkali feldspar/microcline and oligoclase. Hornblende is about 10% of the rock. Sericite alteration common. The rock grades to syenite in some localities. Small outcrops are developed to the southeast of the mine within the diorite.|16-MAY-23
24362|Long Hill Diorite|Extent|The Long Hill Diorite occupies the northwest portion of the Carcoar Granite.|16-MAY-23
24362|Long Hill Diorite|Relationships and boundaries|The diorite is a phase of the Caracoar Granite(?). It lies at the northwestern corner, intruding the Angullong Group (previously Angullong Tuff) subunits viz. the Blayney Andesite and the Cowriga Limestone. Skarns are developed at the contact with the Cowriga Limestone.|16-MAY-23
24362|Long Hill Diorite|Age reasons|Thought to be of Late Silurian-Early Devonian age by correlation with age dating done for the rest of the Carcoar Granite (A. Chivas 415 +/- 8 m.y. in Burnham, 1977).|16-MAY-23
24362|Long Hill Diorite|Proposed publication|Geological Survey of NSW|16-MAY-23
24362|Long Hill Diorite|Proposer|Richardson S., Bowman H.|16-MAY-23
24362|Long Hill Diorite|Reserved? Yes/No|Yes|16-MAY-23
29224|Lumley Adamellite|Name source|Lumley Creek, a north flowing tributary which joins Bungonia Creek 2 km W of Bungonia; GR 671385, Bungonia 1:25 000 Topographic Sheet (8828-II-N).|16-MAY-23
29224|Lumley Adamellite|Unit history|Synonymous in part with the Bungonia Granite (Garretty, 1937).|16-MAY-23
29224|Lumley Adamellite|Extent|The unit extends over 15 km2 as a 0.5 to 2 km wide north-south belt just west of Bungonia from 'Oakview' (GR 642323 - Kooringaroo 1:25 000 Topographic Sheet) to 'Springponds' (GR 694414 - Bungonia 1:25 000 Topographic Sheet).|16-MAY-23
29224|Lumley Adamellite|Lithology|Adamellite.|16-MAY-23
29224|Lumley Adamellite|Relationships and boundaries|A pluton of the Marulan Batholith (Naylor, 1939). It intrudes the Tangerang Volcanics, Wylora Quartz Gabbro and the Springponds Granodiorite. It is overlain in part by Tertiary basalt and surficial deposits.|16-MAY-23
29224|Lumley Adamellite|Age reasons|393 +/- 7 m.y., K-Ar age determination on a biotite separate (Carr, Jones & Wright, 1980).|16-MAY-23
29224|Lumley Adamellite|Proposed publication|Proceedings of the Linnean Society of New South Wales|16-MAY-23
29224|Lumley Adamellite|Proposer|Carr P.F., Jones B.G., Kantsler A.J., Moore P.S., Cook A.C.|16-MAY-23
24379|Micaligo Adamellite|Name source|Micaligo homestead at GR 000400, Michelago 1:100 000 Geological Sheet.|16-MAY-23
24379|Micaligo Adamellite|Unit history|Previously regarded as part of the Michelago Granite.|16-MAY-23
24379|Micaligo Adamellite|Type section locality|In the vicinity of Micaligo homestead.|16-MAY-23
24379|Micaligo Adamellite|Description at type locality|Biotite hornblende adamellite; contains oligoclase mantled with albite, biotite and perthitic alkali feldspar set in a matrix of quartz, biotite, perthitic alkali feldspar, plagioclase, hornblende and minor magnetite and muscovite. Mild alteration. No xenoliths.|16-MAY-23
24379|Micaligo Adamellite|Extent|In the northern half of the Michelago Igneous Complex, south of the Tinderry Road and to the southeast of Michelago.   Size: 35 km2.|16-MAY-23
24379|Micaligo Adamellite|Relationships and boundaries|The adamellite is a major phase of the Michelago Igneous Complex. Its age relationship with the other phases is unknown. It intrudes Late Ordovician Foxlow Beds.|16-MAY-23
24379|Micaligo Adamellite|Age reasons|The adamellite was intruded towards the close of the Silurian Period.|16-MAY-23
24379|Micaligo Adamellite|Proposed publication|Geological Survey of NSW 1:100 000 Note Series|16-MAY-23
26031|Milpose Volcanics|Name source|Milpose Creek GR 599915, Forbes 1:250 000 Sheet.|16-MAY-23
26031|Milpose Volcanics|Type section locality|GR 592902 on hillside. The bottom of this sequence occurs here. The top occurs near the top of the hill at GR 580841.|16-MAY-23
26031|Milpose Volcanics|Extent|This unit crops out in north-south belts over the whole of the central portion of the Forbes 1:250 000 sheet.|16-MAY-23
26031|Milpose Volcanics|Thickness range|Uncertain, probably about 1000 m.|16-MAY-23
26031|Milpose Volcanics|Lithology|Dacitae, rhyolite, trachyandesite, andesite.|16-MAY-23
26031|Milpose Volcanics|Relationships and boundaries|Uncertain. Unconformably overlain by Hervey Group, underlain by Late Ordovician andesites in some areas.|16-MAY-23
26031|Milpose Volcanics|Age reasons|Early Devonian (?) by analogy with the Illunie Rhyolite near Cowra. No fossils have been found in the unit.  The unit has formational status.|16-MAY-23
26031|Milpose Volcanics|Defn author|Bowman H.N., 1977|16-MAY-23
26031|Milpose Volcanics|Proposed publication|Forbes 1:250 000 Metallogenic Map|16-MAY-23
26031|Milpose Volcanics|Name first published by|Bowman H.N., 1977|16-MAY-23
28227|Mingelo Dacite|Name source|Parish Mingelo, County Narromine.|16-MAY-23
28227|Mingelo Dacite|Unit history|Referred to by H.N. Bowman and S.J. Richardson 1978 (unpubl.) as the dacites at Peak Hill.|16-MAY-23
28227|Mingelo Dacite|Type section locality|In the area of the Peak Hill Pty mine the whole of the unit is exposed, GR 6248 9526, Narromine 1:250 000 towards the base. Possible lavas and dyke rocks are also present.|16-MAY-23
28227|Mingelo Dacite|Extent|Mapped in a north-south trending zone 3.5 km by 1 km wide centred to the east of Peak Hill.|16-MAY-23
28227|Mingelo Dacite|Thickness range|Maximum thickness 450 m in the vicinity of the Peak Hill opencuts. It thins rapidly to the north and south.|16-MAY-23
28227|Mingelo Dacite|Relationships and boundaries|Overlies the Late Ordovician Nash Hill Andesite unconformably (?). The contact is obscured by alluvium. The Mingelo Volcanics are overlain by shales, siltstones and fine sandstones of the Early (?) Devonian Trewilga Formation.|16-MAY-23
28227|Mingelo Dacite|Age reasons|Thought to be Late Silurian-Early Devonian(?) by relationship with other formations.|16-MAY-23
28227|Mingelo Dacite|Defn author|Bowman H.N., Richardson S.J., Dolanski J., 1982|16-MAY-23
28227|Mingelo Dacite|Proposed publication|A metallogenic study of the Narromine sheet 1:250 000|16-MAY-23
28227|Mingelo Dacite|Defn Reference|86/25274 Defined p.327.|16-MAY-23
28227|Mingelo Dacite|Proposer|Bowman H., Richardson S., Dolanski J.|16-MAY-23
28227|Mingelo Dacite|Reserved? Yes/No|Yes|16-MAY-23
24383|Mongamula Adamellite|Name source|Mongamula Mountain GR 527309 - about 4 km west of the western boundary of the pluton.|16-MAY-23
24383|Mongamula Adamellite|Unit history|Referred to in earlier works as the Coondella Creek Granite, but that pluton forms a separate body.|16-MAY-23
24383|Mongamula Adamellite|Extent|In the upper catchments of Woolla and Burra Creeks. Total outcrop area is about 21 km2.|16-MAY-23
24383|Mongamula Adamellite|Lithology|Medium grained biotite adamellite and granite (S.S.). Colour index is mostly around 3 to 5, though in places it is up to 10. Fluorite and secondary muscovite are present in most samples.|16-MAY-23
24383|Mongamula Adamellite|Age reasons|Uncertain, either early devonian or late Devonian. Petrographically the body is similar to late Devonian Granitaes nearby (Monga Granite).|16-MAY-23
24383|Mongamula Adamellite|Defn author|Wyborn D., Owen M., 1986|16-MAY-23
24383|Mongamula Adamellite|Proposed publication|BMR map commentary - Araluen 1:100 000 sheet.|16-MAY-23
24383|Mongamula Adamellite|Proposer|Wyborn D.|16-MAY-23
24383|Mongamula Adamellite|Resdate|17-JUN-1982|16-MAY-23
24383|Mongamula Adamellite|Reserved? Yes/No|Yes|16-MAY-23
12208|Moombil Beds|Name source|Mount Moombil GR 5927 2448 (Dorrigo 1:250 000 sheet).|16-MAY-23
12208|Moombil Beds|Unit history|Leitch et al (1971) named this unit and indicated its areal extent, but did not define it. Part of the Coffs Harbour beds of Voisey (1934), Korsch (1971).|16-MAY-23
12208|Moombil Beds|Type section locality|Type Area: Typical rocks are well exposed along the road leading to the summit of Mount Moombil (GR 5927 2448, Dorrigo 1:250 000).  Type Section: None defined - see comments under Thickness.|16-MAY-23
12208|Moombil Beds|Extent|The Moombil Beds crop out over an area of approximately 750 km2 stretching in a broad arc from east of Crossmaglen (GR 6098 2386) to the Demon Fault south of the Chaelundi Complex.|16-MAY-23
12208|Moombil Beds|Thickness range|Indeterminate because of massive nature of lithologies and discontinuous outcrop. Where present bedding mainly dips steeply to the north and this suggests that several thousand metres of sediment may occur.|16-MAY-23
12208|Moombil Beds|Lithology|Black massive argillite with minor volcanically-derived sandstones and siltstones. Bedding is rarely present and other sedimentary structures were not observed.|16-MAY-23
12208|Moombil Beds|Relationships and boundaries|The lowermost exposed part of this unit faulted against the Nambucca Fold Belt. Structural evidence indicates a conformable relationship with the overlying Brooklana Beds, and the boundary between these units has been displaced in numerous localities by faulting.|16-MAY-23
12208|Moombil Beds|Age reasons|Unknown but postulated to be Late Palaeozoic.|16-MAY-23
12208|Moombil Beds|Defn author|Korsch R.J., 1978|16-MAY-23
12208|Moombil Beds|References|79/02435; 79/02550; 01/31630|16-MAY-23
12208|Moombil Beds|Status|1|16-MAY-23
12238|Mooney Mooney Serpentinite|Name source|Mooney Mooney Creek passes through the type section (see below).|16-MAY-23
12238|Mooney Mooney Serpentinite|Type section locality|Northern section exposed by Mooney Mooney Creek. Location of Type Section: GR 179878 to 194889 - Coolac 1:50 000 sheet (yarads). Section where cut by Mooney Mooney Creek.|16-MAY-23
12238|Mooney Mooney Serpentinite|Extent|From 2.2 km east of Muttama Trig Station (GR 200002) in the north to 1.9 km northeast of Pettitts (GR 183832) in the south. A distance of 16 km trending north-south. GRs in yards - Coolac 1:50 000 sheet.|16-MAY-23
12238|Mooney Mooney Serpentinite|Thickness range|a) At type seaction: 1.6 km.  B) Maximum known: 1.6 km.|16-MAY-23
12238|Mooney Mooney Serpentinite|Lithology|Serpentinite and talc-carbonate rocks. Contains some fault slices of basic igneous complex including gabbro pegmatite and meta gabbro.|16-MAY-23
12238|Mooney Mooney Serpentinite|Relationships and boundaries|Boundaries defined by the Mooney Mooney Thrust System. Thrust steeply dipping to east. To west, contact with Flowering Beds and other units of the Honeysuckle Beds. Northeastern half-contact with Young granodiorite. East of type section, contact with North Mooney Complex. South-western half-contact with granite and other units of the Honeysuckle Beds.|16-MAY-23
12238|Mooney Mooney Serpentinite|Age reasons|Formation within the Honeysuckle Beds which are of Early Silurian age.|16-MAY-23
12238|Mooney Mooney Serpentinite|Proposed publication|Geology of the Cootamundra 1:100 000 (Geology Survey of NSW in preparation)|16-MAY-23
12238|Mooney Mooney Serpentinite|Name first published by|Basden H., Adrian J., Clift D.S.L., Winchester R.E., 1978.|16-MAY-23
13504|Murder Dog Adamellite|Name source|The Murder Dog is an area name 439105 Tamworth 1:250 000.|16-MAY-23
13504|Murder Dog Adamellite|Type section locality|Area around 445103 Tamworth 1:250 000.|16-MAY-23
13504|Murder Dog Adamellite|Extent|Covers an area 3 miles x 2 miles centred at 445103 Tamworth 1:250 000.|16-MAY-23
13504|Murder Dog Adamellite|Lithology|Adamellite.|16-MAY-23
13504|Murder Dog Adamellite|Relationships and boundaries|Intrudes a lower Palaeozoic sequence.|16-MAY-23
13504|Murder Dog Adamellite|Age reasons|Lower Permian - belongs to the Hillgrove Plutonic Suite.|16-MAY-23
13504|Murder Dog Adamellite|Proposed publication|New England 1:500 000 Geological Sheet|16-MAY-23
13504|Murder Dog Adamellite|Defn approved by|Copied from xerox sent by NSW Stratigraphic Nomenclature Committee.|16-MAY-23
13504|Murder Dog Adamellite|Name first published by|Geological Survey of NSW, 1973.|16-MAY-23
13504|Murder Dog Adamellite|Reserved? Yes/No|D.J. Pogson|16-MAY-23
24410|Murga Intrusive Complex|Name source|Parish Murga, County Cunningham|16-MAY-23
24410|Murga Intrusive Complex|Unit history|Yates 1966 (unpub.) called this intrusive complex the Wanda Bye intrusion. Stroud 1973 unpubl. has included this intrusion in his Tout complex.|16-MAY-23
24410|Murga Intrusive Complex|Type section locality|GR 5468 9445, Narromine 1:250 000|16-MAY-23
24410|Murga Intrusive Complex|Extent|Outcrop area 2 km west of Fifield elongated northwest. Size: Covers an area approximately 4 km x 3 km.|16-MAY-23
24410|Murga Intrusive Complex|Lithology|Composition: Peripheral zone of coarse-grained hornblende pyroxenite grading to augite hornblendite, and a small central zone of sericitized and saussuritized meladiorite grading to quartz diorite.|16-MAY-23
24410|Murga Intrusive Complex|Relationships and boundaries|Intrudes the Cambro-Ordovician Girilambone Group.|16-MAY-23
24410|Murga Intrusive Complex|Age reasons|By correlation with other similar dated complexes (of Tout Complex), thought to be Early-Middle Devonian.|16-MAY-23
24410|Murga Intrusive Complex|Defn author|Bowman H.N., Richardson S.J., Dolanski J., 1982|16-MAY-23
24410|Murga Intrusive Complex|Proposed publication|A metallogenic study of the Narromine 1:250 000 sheet|16-MAY-23
24410|Murga Intrusive Complex|Defn Reference|86/25274 Defined P.328.|16-MAY-23
24410|Murga Intrusive Complex|Proposer|Bowman H., Richardson S., Dolanski J.|16-MAY-23
24410|Murga Intrusive Complex|Reserved? Yes/No|Yes|16-MAY-23
13924|Nash Hill Andesite|Name source|Nash Hill (GR 625907, Forbes 1:250 000).|16-MAY-23
13924|Nash Hill Andesite|Unit history|Previously named Goonumbla Volcanics (Forbes 1:250 000 Geological Sheet 1972). When the Goonumbla Volcanics were redefined by Sherwin (Rec. Geol Surv. NSW 15(1), 1973), a new name was required for this unit.|16-MAY-23
13924|Nash Hill Andesite|Type section locality|Middle of unit crops out on the flanks of Nash Hill. The top is to east while the bottom is to the west.|16-MAY-23
13924|Nash Hill Andesite|Extent|Crops out in north-south trending belt 20 km long by 5 km wide. 2 km northeast of Parkes.|16-MAY-23
13924|Nash Hill Andesite|Lithology|Andesitic lavas, tuffs and shales.|16-MAY-23
13924|Nash Hill Andesite|Relationships and boundaries|Overlies Late Ordovician undifferentiated sediments (relationship unknown); underlies (probably unconformably) undifferentiated Silurian sediments.|16-MAY-23
13924|Nash Hill Andesite|Age reasons|Assumed Late Ordovician by analogy with Coonumbla Andesite to west.|16-MAY-23
13924|Nash Hill Andesite|Defn author|Bowman h.n., 1977|16-MAY-23
13924|Nash Hill Andesite|Proposed publication|Forbes 1:250 000 Metallogenic Map|16-MAY-23
13924|Nash Hill Andesite|Name first published by|Bowman H.N., 1977|16-MAY-23
13957|Neds Beach Calcarenite|Name source|Neds Beach, north coast of Lord Howe Island located at 159o04.15'E longitude, 31o31.1'S latitude on map of Lord Howe Island. (Department of Lands, Sydney, 1966, 1:15840).|16-MAY-23
13957|Neds Beach Calcarenite|Unit history|Standard (1963) called this formation the Ned's Beach Calcarenite, the only change suggested is to alter the name in conformity with the map.|16-MAY-23
13957|Neds Beach Calcarenite|Type section locality|None designated, although typical outcrops occur in cliffs at eastern end of Neds Beach and in cliffs of Middle Beach to the west of Brodies Point.|16-MAY-23
13957|Neds Beach Calcarenite|Extent|Exposed over about 1 km2 in low lying country between northern flanks of Transit Hill and Neds Beach, and also locally around coast at North Bay and Kings Beach.|16-MAY-23
13957|Neds Beach Calcarenite|Thickness range|Maximum about 40 m.|16-MAY-23
13957|Neds Beach Calcarenite|Lithology|Calcarenite, often with well developed cross bedding and according to Standard (1963) consists mainly of fragments of coralline algae with less abundant coral, foraminifera and molluscs.|16-MAY-23
13957|Neds Beach Calcarenite|Relationships and boundaries|Overlies North Ridge Basalt and Rocky Point Breccia and locally overlies a talus deposit on southeast coast under Mount Gower.|16-MAY-23
13957|Neds Beach Calcarenite|Age reasons|Standard (1963) regards it as Pleistocene to Recent.|16-MAY-23
13957|Neds Beach Calcarenite|Proposed publication|Submitted to J. Geol. Soc. Australia|16-MAY-23
13957|Neds Beach Calcarenite|Comments|Notes: Interpreted as an aeolianite.|16-MAY-23
13957|Neds Beach Calcarenite|Defn approved by|See letter 1-JUL-1982 on NSW file from T. Russell.|16-MAY-23
31405|Oakfields Ignimbrite Tongue|Name source|Named after Oakfields Hill, 058268, Woolooma 1:63 360 Sheet.|16-MAY-23
31405|Oakfields Ignimbrite Tongue|Type section locality|Eastern side of Lake Glenbawn. Location of Type Section: The section incorporating the type locality of the Oakfields Tongue extends from 015307 to 051329 Woolooma 1:63 360 Sheet, near Curra Keith Creek. Type locality 033317.|16-MAY-23
31405|Oakfields Ignimbrite Tongue|Extent|Extends from Dangarfield north to Gundy, and east as far as Rouchel Brook Village.|16-MAY-23
31405|Oakfields Ignimbrite Tongue|Thickness range|a) At type section: 30 m.  b) Maximum known:  30 m.|16-MAY-23
31405|Oakfields Ignimbrite Tongue|Lithology|Consists of a lowermost red ignimbrite with white phenocrysts of andesine, separated by green and pink lithic sandstone from an upper massive purple to buff ignimbrite.|16-MAY-23
31405|Oakfields Ignimbrite Tongue|Relationships and boundaries|The Oakfields Ignimbrite Tongue is within the Isismurra Formation. It is laterally equivalent to the upper part of the Native Dog Ignimbrite Member, and is separated from the older Curra Keith Ignimbrite Member by a tongue of zeolitic lithic sandstone. Similar sandstones overlie the Oakfields Tongue.|16-MAY-23
31405|Oakfields Ignimbrite Tongue|Age reasons|Lower Carboniferous (Visean). Hornblende from the tongue has been dated at 308 +/- 6 and 309 +/- 6 million years. Marine lateral equivalents in the eastern part of the district contain the Orthotetes australis Zone.|16-MAY-23
31405|Oakfields Ignimbrite Tongue|Defn author|Roberts J., Oversby B.S., 1974|16-MAY-23
31405|Oakfields Ignimbrite Tongue|Proposed publication|BMR Bulletin|16-MAY-23
31405|Oakfields Ignimbrite Tongue|Defn approved by|Approved. Copied from xerox sent by NSW Stratigraphic Nomenclature Sub-Committee.|16-MAY-23
31405|Oakfields Ignimbrite Tongue|Name first published by|Roberts J., Oversby B., 1973|16-MAY-23
31405|Oakfields Ignimbrite Tongue|Proposer|Roberts J, Oversby B.S.|16-MAY-23
31405|Oakfields Ignimbrite Tongue|Reserved? Yes/No|J Roberts|16-MAY-23
14887|Parkes Andesite|Name source|Town of Parkes (GR 622902, Forbes 1:250 000).|16-MAY-23
14887|Parkes Andesite|Unit history|Previously named Goonumbla Volcanics (Forbes 1:250 000 geological Sheet 1972). When the Goonumbla Volcanics were redefifned by Sherwin (Rec. Geol. Surv NSW 15(1), 1973), a new name was required for this unit.|16-MAY-23
14887|Parkes Andesite|Type section locality|Small hill on road west of Parkes (GR 619903). The top is exposed to the east of this location while the bottom is exposed to the west.|16-MAY-23
14887|Parkes Andesite|Extent|Crops out in belt 1 km wide by 8 km long 3 km due west of Parkes.|16-MAY-23
14887|Parkes Andesite|Lithology|Andesitic lavas, and tuffs and shale.|16-MAY-23
14887|Parkes Andesite|Relationships and boundaries|Overlies Late Ordovician rocks (relationship unknown).|16-MAY-23
14887|Parkes Andesite|Age reasons|Assumed Late Ordovician by analogy with Goonumbla Andesite to north-east.|16-MAY-23
14887|Parkes Andesite|Defn author|Bowman H.N., 1977|16-MAY-23
14887|Parkes Andesite|Proposed publication|Forbes 1:250 000 Metallogenic Map|16-MAY-23
14887|Parkes Andesite|Name first published by|Bowman H.N., 1977|16-MAY-23
24462|Pomeroy Basalt|Name source|Pomeroy' property; GR 2920 6235, Goulburn 1:250 000 Sheet area (Sl 55-12).|16-MAY-23
24462|Pomeroy Basalt|Type section locality|This basalt is extremely poorly exposed and there appears to be in situ outcrop at one locality only, on the upper surface of the basalt at GR 3195 6038. This is designated as the type locality. A second locality, Quarry Hill (GR 3880 5193) is the K-Ar dating locality of Young & Bishop (1980) and while no in situ basalt crops out here, there is a clear relationship with underlying in situ silcrete.|16-MAY-23
24462|Pomeroy Basalt|Extent|Sinuous line (15 km long) of hilltop basalt on north bank of Wollondilly River, west of Goulburn.|16-MAY-23
24462|Pomeroy Basalt|Thickness range|Maximum of 40 m, generally about 30 m.|16-MAY-23
24462|Pomeroy Basalt|Lithology|Porphyritic to even-grained olivine basalt.|16-MAY-23
24462|Pomeroy Basalt|Relationships and boundaries|Either i) disconformably overlies undifferentiated Ordovician fine-grained metasediments or granitic rocks of the Wologorong Batholith, or ii) conformably overlies silicified quartrzose fluvial sediments (silcrete).|16-MAY-23
24462|Pomeroy Basalt|Age reasons|Late Oligocene on the basis of two K-Ar age determinations (Young & Bishop, 1980).|16-MAY-23
24462|Pomeroy Basalt|Proposed publication|Journal and Proceedings of the Royal Society of NSW|16-MAY-23
24462|Pomeroy Basalt|Proposer|Bishop P.|16-MAY-23
24462|Pomeroy Basalt|Resdate|SEP-OCT-1984|16-MAY-23
24462|Pomeroy Basalt|Reserved? Yes/No|Variation List 66|16-MAY-23
24466|Quigleys Hill Tuff|Name source|Quigleys Hill mine at GR 2235 8484(?) Bathurst 1:250 000 Metallogenic Sheet.|16-MAY-23
24466|Quigleys Hill Tuff|Type section locality|Best exposed to the southwest of Blayney along the highway.|16-MAY-23
24466|Quigleys Hill Tuff|Extent|The unit outcrops over a strike length of some 13 kms in a north-northwest direction through Blayney.|16-MAY-23
24466|Quigleys Hill Tuff|Thickness range|Maximum thickness 2500 m but probably a lot thinner than this.|16-MAY-23
24466|Quigleys Hill Tuff|Lithology|Andesitic tuff - mid-grey to greenish in colour - containing approximately equal proportions of porphyritic and fine-grained andesitic grains averaging 2 mm in size but up to 1 cm. Porphyritic fragments have mainly plagioclase with lesser pyroxene crystals. Low percentage groundmass overall.|16-MAY-23
24466|Quigleys Hill Tuff|Relationships and boundaries|The Quigleys Hill Tuff, along with the Cowriga Limestone (overlying) the Blayney Andesite (underlying) comprise the Angullong Group (previously Tuff). The Quigleys Hill Tuff is unconformably(?) overlain by the Wombiana Formation (nov.)|16-MAY-23
24466|Quigleys Hill Tuff|Age reasons|Late Ordovician. Subdivision of the Angullong Group which is thought to be of Late Ordovician age.|16-MAY-23
24466|Quigleys Hill Tuff|Proposed publication|Geological Survey of NSW|16-MAY-23
24466|Quigleys Hill Tuff|Proposer|Richardson S., Bowman H.|16-MAY-23
24466|Quigleys Hill Tuff|Reserved? Yes/No|Yes|16-MAY-23
38784|Ramparts Creek Sandstone Member|Name source|Ramparts Creek, a southeast flowing creek on Waterbag Station (south of Mootwingee National Park)|16-MAY-23
38784|Ramparts Creek Sandstone Member|Unit history|None|16-MAY-23
38784|Ramparts Creek Sandstone Member|Constituents|None|16-MAY-23
38784|Ramparts Creek Sandstone Member|Geomorphic expression|Forms the upper part of a narrow valley.|16-MAY-23
38784|Ramparts Creek Sandstone Member|Type section locality|In an east-flowing tributary of Ramparts Creek 1.5 km south of Rocky Tank South (Lat. 31o, 24', Long. 142o, 22.5').|16-MAY-23
38784|Ramparts Creek Sandstone Member|Extent|Forms a narrow belt between Ramparts Creek in the southeast and the southern boundary of the Mootwingee National Park in the North.|16-MAY-23
38784|Ramparts Creek Sandstone Member|Thickness range|50-60 m|16-MAY-23
38784|Ramparts Creek Sandstone Member|Lithology|Uniform thin bedded fine and medium grained laminated sandstone.|16-MAY-23
38784|Ramparts Creek Sandstone Member|Depositional environment|Coastal plain deposited, low-flow regime.|16-MAY-23
38784|Ramparts Creek Sandstone Member|Relationships and boundaries|Conformable with the Rocky Tank Conglomerate Member (below) and the Ravendale Formation (above).|16-MAY-23
38784|Ramparts Creek Sandstone Member|Age reasons|Mid-Late Givetian ? represents deposition during a global sea level rise during the Givetian Taghanic Transgression.|16-MAY-23
38784|Ramparts Creek Sandstone Member|Correlations|None known|16-MAY-23
16472|Rutledge Quartzite Member|Name source|Derived from Rutledge Trig. station (996m) at GR 167702 (Richardson 1979).|16-MAY-23
16472|Rutledge Quartzite Member|Unit history|Rutledge Quartzite (Oldershaw 1965).|16-MAY-23
16472|Rutledge Quartzite Member|Type section locality|Designated at Grose Meadow Hill (GR 204/722) and along Foxlow Creek valley where discontinuous outcrops of shale-clast conglomerate appear to grade laterally into grey quartzite in the faulted nose of a north plunging anticline (Canberra 1:100 000 sheet 8727). Quartzite rocks representative of this member also outcrop along Rutledge Ridge.|16-MAY-23
16472|Rutledge Quartzite Member|Extent|The unit crops out sporadically around the southern end of the Captains Flat Graben.|16-MAY-23
16472|Rutledge Quartzite Member|Thickness range|A maximum thickness of 100m is given by Oldershaw (1965).|16-MAY-23
16472|Rutledge Quartzite Member|Lithology|Narrow ridges and knolls of pale-grey quartzite with interbedded conglomerate, siltstone and shale.|16-MAY-23
16472|Rutledge Quartzite Member|Depositional environment|Shallow marine with clastic material derived from underlying Ordovician rocks.|16-MAY-23
16472|Rutledge Quartzite Member|Relationships and boundaries|A member of the Copper Creek Shale. Unconformable on Late Ordovician rocks. The Rutledge Quartzite Member is conformable with higher units on the Copper Creek Shale.|16-MAY-23
16472|Rutledge Quartzite Member|Age reasons|Unfossiliferous. A late Silurian age based on sparse fossil evidence in the overlying Copper Creek Shale.|16-MAY-23
16472|Rutledge Quartzite Member|Correlations|A unit of local derivation with possible correlation with conglomerate at the base of the De Drack Formation.|16-MAY-23
26132|Sandal Formation|Name source|Sandal Trig Station.|16-MAY-23
26132|Sandal Formation|Type section locality|Sandal Trig Station, 5 km south-west of Burcher. Isolated outcrop. 525853 (bottom) to 522853 (top) Forbes 1:250 000.|16-MAY-23
26132|Sandal Formation|Extent|Exposed along strike for about 20km from Blow Clear to west of Burcher.|16-MAY-23
26132|Sandal Formation|Thickness range|About 1500 m.|16-MAY-23
26132|Sandal Formation|Lithology|The formation consists predominantly of fine sandstones and siltstones and at the type section contains poorly preserved shelly fossils - brachiopods or bivalves. Further to the south, there are lenses of conglomerate, shale, siltstone, and aeromagnetics indicate also the presence of andesites. Also black cherts.|16-MAY-23
26132|Sandal Formation|Relationships and boundaries|Boundaries not exposed. Regional trend suggests unconformable relationship with underlying Burcher Greywacke.|16-MAY-23
26132|Sandal Formation|Age reasons|Probably Early Devonian, from regional considerations.|16-MAY-23
26132|Sandal Formation|Proposed publication|Bulletin Australian Society of Exploration Geophysicists (v.7 No. 1).|16-MAY-23
28174|Sara Beds|Name source|Sara River, which flows eastwards from the New England Plateau until it joins the Guy Fawkes River at GR 53432911 (Grafton 1:250 000) .|16-MAY-23
28174|Sara Beds|Type section locality|Good, although not continuous, exposures occur in the Guy Fawkes River in the vicinity of the junction with the Sara River from (GR 53582884 to GR 53542949).|16-MAY-23
28174|Sara Beds|Extent|The Sara Beds occupy an area of approximately 350 km2 to the north of the Dyamberin Beds. The boundary between the two units runs approximately NW-SE passing near the junction of the jAberfoyle River with the Guy Fawkes River.|16-MAY-23
28174|Sara Beds|Thickness range|Not determined but steep bedding planes indicate that a thick sequence is probably present.|16-MAY-23
28174|Sara Beds|Lithology|Orthoconglomerate horizons and associated siliceous mudstones, siltstones and volcanically-derived greywackes.  Rare basic and acid volcanics occur also.|16-MAY-23
28174|Sara Beds|Relationships and boundaries|The Sara Beds are bounded on the east by the Demon Fault and to the north and west by granitic rocks of the New England Batholith. They conformably overlie the Dyamberin Beds to the south. The Sara Beds are characterised by orthoconglomerates and only contain rare diamictites, and hence can be readily distinguished from the Dyamberin Beds.|16-MAY-23
28174|Sara Beds|Age reasons|Structural relations indicate that the Sara Beds conformably overlie the Dyamberin Beds and hence it is assumed that they are also of Permian age.|16-MAY-23
28174|Sara Beds|Defn author|Korsch R.J., 1978.|16-MAY-23
26325|Spicers Creek Adamellite|Name source|Spicers Creek on Parish Map: Parish of the Peaks, County of Buccleuch.|16-MAY-23
26325|Spicers Creek Adamellite|Type section locality|None given.|16-MAY-23
26325|Spicers Creek Adamellite|Extent|A granodiorite stock about 1 km across 7 km north of Rules Point and 1 km W of the Starvation Point Adamellite stock.|16-MAY-23
26325|Spicers Creek Adamellite|Lithology|Porphyritic biotite granodiorite with minor hornblende.|16-MAY-23
26325|Spicers Creek Adamellite|Relationships and boundaries|Intrudes Goobarragandra Beds.|16-MAY-23
26325|Spicers Creek Adamellite|Age reasons|Late Silurian as chemically related to the Young Granodiorite.|16-MAY-23
26325|Spicers Creek Adamellite|Proposed publication|Bureau of Mineral Resources Bulletin|16-MAY-23
26325|Spicers Creek Adamellite|Defn Reference|83/24087|16-MAY-23
26325|Spicers Creek Adamellite|First Reference|80/21171|16-MAY-23
26325|Spicers Creek Adamellite|Proposer|Owen M., Wyborn D.|16-MAY-23
26325|Spicers Creek Adamellite|Unit name|Spicers Creek adamellite|16-MAY-23
24500|Springponds Granodiorite|Name source|Springponds' property; GR 694414, Bungonia 1:25 000 Topographic Sheet (8828-II-N).|16-MAY-23
24500|Springponds Granodiorite|Unit history|Synonymous in part with the Bungonia Granite (Garretty, 1937).|16-MAY-23
24500|Springponds Granodiorite|Type section locality|1 km SE of 'Springponds' homestead on Blungonia Creek, GR 701407 - Bungonia 1:25 000 Topographic Sheet (8828-II-N).|16-MAY-23
24500|Springponds Granodiorite|Extent|The unit extends over 14 km2 as a 0.5-2 km wide belt in a NNE direction from Bungonia to the Marulan South road.|16-MAY-23
24500|Springponds Granodiorite|Lithology|Granodiorite.|16-MAY-23
24500|Springponds Granodiorite|Relationships and boundaries|A pluton of the Marulan Batholith (Naylor, 1939). It intrudes the Tangerang volcanics and is intruded by the Wylora Quartz Gabbro. It is overlain in part by Permian and Tertiary surficial deposits.|16-MAY-23
24500|Springponds Granodiorite|Age reasons|406 +/- 7 m.y., K-Ar age determination on a biotite separate (Carr, Jones & Wright, 1980).|16-MAY-23
24500|Springponds Granodiorite|Proposed publication|Proceedings of the Linnean Society of New South Wales|16-MAY-23
24500|Springponds Granodiorite|Proposer|Carr P.F., Jones B.G., Kantsler A.J., Moore P.S., Cook A.C.|16-MAY-23
24503|Starvation Point Adamellite|Name source|Starvation Point on parish map: Parish of the Peaks, County of Buccleuch.|16-MAY-23
24503|Starvation Point Adamellite|Type section locality|GR 391532, Tantangara 1:100 000 sheet area.|16-MAY-23
24503|Starvation Point Adamellite|Extent|An adamellite stock about 1 km across, 7 kms north of Rules Point and 1 km E of the Spicers Creek Granodiorite stock.|16-MAY-23
24503|Starvation Point Adamellite|Lithology|Hornblende-biotite adamellite.|16-MAY-23
24503|Starvation Point Adamellite|Relationships and boundaries|Intrudes the Goobarragandra Beds.|16-MAY-23
24503|Starvation Point Adamellite|Age reasons|Late Silurian?|16-MAY-23
24503|Starvation Point Adamellite|Proposed publication|Bureau of Mineral Resources Bulletin|16-MAY-23
24503|Starvation Point Adamellite|Defn Reference|83/24087|16-MAY-23
24503|Starvation Point Adamellite|Proposer|Owen M., Wyborn D.|16-MAY-23
24506|Stokefield Diorite|Name source|Stokefield' homestead GR 97057785 Blayney 1:50 000 (8730-I-IV).|16-MAY-23
24506|Stokefield Diorite|Type section locality|See above.|16-MAY-23
24506|Stokefield Diorite|Description at type locality|Hornblende diorite, in part foliated and strongly sheared. Typically a light grey-off white coarse-grained (2 mm) holocrystalline rock containing euhedral-subhedral crystals of andesine plagioclase (50-70%) and hornblende (5-15%) anhedral K feldspar (0-15%) and (in some cases) quartz (up to 8%) and pyroxene with accessory sphene, biotite, pyroxene and opaques.  Area: Covers approximately 5.5. km2.|16-MAY-23
24506|Stokefield Diorite|Extent|An intrusion with a diameter of 3 km in an area surrounding the township of Carcoar.|16-MAY-23
24506|Stokefield Diorite|Relationships and boundaries|The Stockfield Diorite is intruded by the Carcoar Granite (Rayner, 1960). The diorite intrudes the Malongulli Formation and the Abercrombie Beds. Small felsitic dykes thought to be related to the diorite intrude the adjacent volcanics and sediments. The diorite is strongly sheared along its western margin.|16-MAY-23
24506|Stokefield Diorite|Age reasons|(Late Silurian?)-Early Devonian age.|16-MAY-23
24506|Stokefield Diorite|Proposed publication|Geological Survey of NSW|16-MAY-23
24506|Stokefield Diorite|References|01/31635|16-MAY-23
24506|Stokefield Diorite|Proposer|Richardson S., Paterson I.B.L.|16-MAY-23
24506|Stokefield Diorite|Reserved? Yes/No|Yes|16-MAY-23
17701|Tallawudjah Leucoadamellite|Name source|Tallawudjah Creek, west of Glenneagh village. The creek cuts the intrusion at GR 60462738 (Dorrigo 1:250 000).|16-MAY-23
17701|Tallawudjah Leucoadamellite|Unit history|Previously undescribed.|16-MAY-23
17701|Tallawudjah Leucoadamellite|Type section locality|In the vicinity of Tallawudjah Creek where it cuts the intrusion at GR 60462738.|16-MAY-23
17701|Tallawudjah Leucoadamellite|Extent|The pluton crops out over some 0.7 km2, 5 km south-west of Glenreach.|16-MAY-23
17701|Tallawudjah Leucoadamellite|Lithology|Porphyritic leucoadamellite with phenocrysts of white feldspar set in a fine groundmass of feldspar, quartz and mafics.|16-MAY-23
17701|Tallawudjah Leucoadamellite|Relationships and boundaries|The intrusion has been emplaced into the Coramba Beds and its western boundary is covered by the Mesozoic Clarence-Moreton Basin sediments.|16-MAY-23
17701|Tallawudjah Leucoadamellite|Age reasons|Unknown, but intrudes the Coramba Beads of postulated Late Palaeozoic (possibly Carboniferous) age and is covered by the Late Triassic Mill Creek Siltstone.|16-MAY-23
17701|Tallawudjah Leucoadamellite|Defn author|Korsch R.J., 1978.|16-MAY-23
25523|Temperance Chert|Name source|Temperance Creek, a tributary of the Tumut River, in the Wagga Wagga 1:250 000 Sheet area.|16-MAY-23
25523|Temperance Chert|Type section locality|The type area is along Temperance Creek where, according to Fairbridge et al., "it occurs approximately along the line of latitude 35o59'S, between longitudes 148o27' and 148o28'E. It outcrops in this creek between 1/2 and 2 1/2 air miles (direct) above the junction with the Tumut River".  Type Section: A type section has been chosen within Fairbridge et al's type area. It extends westward along the southern bank of Temperance Creek, from a point 1100 m southwest of Skeleton Creek at longitude 148o28', latitude 35o59'19", to a point 400 m east of Frenchmans Creek at longitude 148o27'27", latitude 35o59'18". These coordinates were obtained from the Snowy Mountains Hydro-Electric Authority Topographic Sheets, Kiandra Series, 1960. The section is partly covered by soil, and thickness estimates in some cases depends upon observation of rock fragments rather than outcrop. The sequence, and estimated thickness of individual units is: Top of Section - Section ends at fault (inferred, soil-covered); 160 - Tuff, coarse tuff, tuffaceous chert, chert; 30 - Interbedded tuff and very fine-grained tuffaceous chert; 100 - Very coarse tuff and chert; 116 - Tuff and thin beds of chert; 40 - Tuff, fine and medium-grained; 1 - Slate; 15 - Thin beds of very fine-grained tuff; 48 - Tuff and interbeds of chert; 24 - Tuff; 8 - Thick-bedded banded chert, and interbeds of cherty silty greywacke; 80 - Tuff and interbeds of cherty tuff with a 2-metre layer of argillite and fine-grained argillaceous arenite or greywacke in the middle; 120 - Interbedded tuff and chert, with a 1-metre bed of tuffaceous slate in the lower half; 8 - Thick beds of chert, with thin interbeds or laminae of silty to argillitic chert and quartz argillite; Bottom of Section - Rests conformably on fine-grained arenite and siltstone at the top of the Boltons Beds.|16-MAY-23
25523|Temperance Chert|Extent|Forms a north-northwesterly trending belt a few kilometres wide in the Tallangatta 1:250 000 Sheet area, along the upper part of the Tumut River. The belt enters the southwestern corner of the Tantangara 1:100 000 Sheet area a short distance east of the village of Kiandra on the Snowy Mountains Highway; thence it continues with a width of 1 to 6 km along the eastern side of the upper Murrumbidgee River on the Long Plain, to longitude 148o40', latitude 35o33', near the northwestern side of Cooleman Mountains.|16-MAY-23
25523|Temperance Chert|Thickness range|No significant folding can be observed (although it cannot be ruled out). On that assumption, the type section exposes the lower 750 m of the formation. The type area is cut by several faults; by correlating between fault-blocks, a total estimated thickness of 200 m [?2000: see below] is obtained.|16-MAY-23
25523|Temperance Chert|Lithology|Interbedded tuff and chert with minor thin beds of clastic sediment (siltstone, very fine-grained quartz arenite or greywacke, and black shale and silty shale). Within the formation there are some distinctive individually mapped layers which have been an aid to correlation between outcrop areas, but are not formally named. These are a 100 m bed of agglomerate 1350 m above the units base, 250 m of chert above that agglomerate, and within the Tantangara Sheet area a bed of lava and another of tuff.|16-MAY-23
25523|Temperance Chert|Relationships and boundaries|Conformable above the Boltons Beds and below the Nine Mile Volcanics. The base of the formation is exposed in the type section. The top is exposed along Happy Jacks Road 650 m west of the junction of the Happy Jacks and Tumut Rivers. There, interbedded thin beds of tuff, chert and cherty fine-grained greywacke at the top of the Temperance Chert are overlain conformably by a 2-metre bed of black fissile shale at the base of the Nine Mile Volcanics.|16-MAY-23
25523|Temperance Chert|Age reasons|Late Ordovician, probably between Darriwillian and Gisbornian; deduced from stratigraphic relationships.|16-MAY-23
25523|Temperance Chert|Defn approved by|Copied from xerox from NSW Sub-Committee.|16-MAY-23
25523|Temperance Chert|Defn Reference|83/24087|16-MAY-23
25523|Temperance Chert|Status|1|16-MAY-23
18070|Thompsons Creek Granite|Name source|Bathurst 1:250 000 Village of Thompsons Creek 259806.|16-MAY-23
18070|Thompsons Creek Granite|Unit history|Called Burraga Granodiorite by Stanton R.L. (1955). Renamed because of synonomy with the better known Burraga Group.|16-MAY-23
18070|Thompsons Creek Granite|Type section locality|Location of type section: Burraga - Thompsons Creek road.|16-MAY-23
18070|Thompsons Creek Granite|Extent|East of this village.|16-MAY-23
18070|Thompsons Creek Granite|Thickness range|a) At Type Section: 6 sq miles in area;  b) Maximum known:|16-MAY-23
18070|Thompsons Creek Granite|Lithology|Massive granite - on basis of petrological description by L. Barrow.|16-MAY-23
18070|Thompsons Creek Granite|Relationships and boundaries|Intrudes Triangle Group.|16-MAY-23
18070|Thompsons Creek Granite|Age reasons|Late Carboniferous by analogy with The Bathurst Granite.|16-MAY-23
18070|Thompsons Creek Granite|Proposed publication|Rec. Geological Survey of NSW|16-MAY-23
18070|Thompsons Creek Granite|Defn approved by|Approved. Copied from xerox sent by NSW Stratigraphic Nomenclature Sub-Committee.|16-MAY-23
18070|Thompsons Creek Granite|Name first published by|Bowman N.H., 1975.|16-MAY-23
18070|Thompsons Creek Granite|Reserved? Yes/No|H. Bowman|16-MAY-23
24530|Toolamanang Volcanics|Name source|Parish of Toolamanang, County of Wellington|16-MAY-23
24530|Toolamanang Volcanics|Type section locality|1200 m of basal spherulitic rhyodacite, lutite and uppermost rhyodacitic lava and breccia, volcarenite from GR 764550 6364000 to GR 764200 6364800.|16-MAY-23
24530|Toolamanang Volcanics|Extent|The unit outcrops over 15 km2 to the east of Cudgegong Creek - however it apparently outcrops to the west and northwest - on the Mudgee 1:100 000 sheet.|16-MAY-23
24530|Toolamanang Volcanics|Lithology|Spherulitic rhyodacite, massive, highly fractured; lutite, well bedded, unfossiliferous, brown to grey; rhyodacitic lava, fine-grained, grey black, massive, well jointed; rhyodacitic breccia, very coarse-grained, massive, volcarenites, grey to black, massive, coarse-grained.|16-MAY-23
24530|Toolamanang Volcanics|Relationships and boundaries|Conformably overlies Willow Glen Formation - top of formation not seen.|16-MAY-23
24530|Toolamanang Volcanics|Age reasons|Lithological correlation with Silurian Bells Creek Volcanics (Packham, 1968).|16-MAY-23
24530|Toolamanang Volcanics|Proposed publication|Journal and Proceedings of the Royal Society of NSW|16-MAY-23
24530|Toolamanang Volcanics|Defn Reference|80/2103|16-MAY-23
24530|Toolamanang Volcanics|Proposer|Pemberton J.W.|16-MAY-23
24530|Toolamanang Volcanics|Reserved? Yes/No|Yes|16-MAY-23
24533|Towneys Creek Adamellite|Name source|After Towneys Creek which intersects the Jerangle-Captains Flat Road at GR 165295, Michelago 1:100 000 Geological Sheet.|16-MAY-23
24533|Towneys Creek Adamellite|Unit history|Although this phase was recognised as early as 1915 (Baker, 1915), Richards (1967) was the first to name the adamellite the Towneys Creek Adamellite.|16-MAY-23
24533|Towneys Creek Adamellite|Type section locality|At GR 187391 at the intersection of the Tinderry Road and the Jerangle-Captains Flat Road.|16-MAY-23
24533|Towneys Creek Adamellite|Description at type locality|Texturally inhomogeneous adamellite; fine to coarse-grained to porphyritic. The rock typically contains quartz, K-feldspar, plagioclase and biotite with accessory opaques, apatite and zircon. No xenoliths are present. Marginal aplitic phases are associated with the adamellite.  Size: 75 km2.|16-MAY-23
24533|Towneys Creek Adamellite|Extent|Extends from GR 140134 to GR 213444, Michelago 1:100 000 Geological Sheet and occupies the western third of the Jerangle Igneous Complex.|16-MAY-23
24533|Towneys Creek Adamellite|Relationships and boundaries|The Jerangle Igneous Complex has intruded Late Ordovician Foxlow Beds and the Towneys Creek Adamellite has characteristically developed a contact metamorphic aureole. Contact between the adamellite and the Anembo Granodiorite is minimal so that their exact time relationship is unknown.|16-MAY-23
24533|Towneys Creek Adamellite|Age reasons|K-Ar dating of the Jerangle Igneous Cojmplex has given an age of 393 m.y. (White, 1962), since revised to 396 mn.y. (J. Richards, pers comm).|16-MAY-23
24533|Towneys Creek Adamellite|Proposed publication|Geological Survey of NSW 1:100 000 Note Series|16-MAY-23
24533|Towneys Creek Adamellite|Unit name|Towneys Creek Adamellite (nov. aftr Richards 1967)|16-MAY-23
18579|Trewilga Beds|Name source|Trewilga GR 626945 Narromine 1:250 000 Sheet.|16-MAY-23
18579|Trewilga Beds|Type section locality|Alectown GR 625927, Narromine 1:250 000 in gullies and road cuttings.|16-MAY-23
18579|Trewilga Beds|Extent|The unit crops out over about 100 km2 area 15 km south of Peak Hill.|16-MAY-23
18579|Trewilga Beds|Lithology|Siltstone, sandstone, conglomerate, limestone, and regional metamorphic equivalents.|16-MAY-23
18579|Trewilga Beds|Relationships and boundaries|Unconformably overlies Late Ordovician volcanics and Early Silurian sediments, Upper boundary uncertain.|16-MAY-23
18579|Trewilga Beds|Age reasons|Late Silurian (?) by analogy with similar unnamed and variously named lithologies to the northeast near Yeowal. No fossils have been found in the unit.|16-MAY-23
18579|Trewilga Beds|Defn author|Bowman H.N., 1977|16-MAY-23
18579|Trewilga Beds|Proposed publication|Forbes 1:250 000 Metallogenic Map|16-MAY-23
18579|Trewilga Beds|Name first published by|Bowman H.N., Holley G., 1976|16-MAY-23
18580|Trewilga Formation|Unit history|This unit has previously been defined under the title Trewilga Beds by Bowman 1977.|16-MAY-23
18580|Trewilga Formation|Defn approved by|See letter of 1/7/1982 on NSW file from T. Russell|16-MAY-23
26963|Tuross Head Granodiorite|Name source|Tuross Head - a prominent coastal feature; GR 424050 Narooma 1:100 000.|16-MAY-23
26963|Tuross Head Granodiorite|Type section locality|Exposures in the vicinity of the township of Tuross Head (GR 420060).|16-MAY-23
26963|Tuross Head Granodiorite|Extent|It is exposed over about 2 km2 on the peninsular separating Coila and Tuross Lakes in the northern portion of the Narooma 1:100 000 sheet.|16-MAY-23
26963|Tuross Head Granodiorite|Lithology|Hornblende biotite granodiorite. It possesses a distinct foliation formed by the parallel arrangement of the mineral constituents and alignment of abundant elongate xenoliths. This foliation is subvertical and trends at about 320o.|16-MAY-23
26963|Tuross Head Granodiorite|Relationships and boundaries|It is one of the intrusive bodies of the Moruya Igneous Complex (Moruya Plutonic Complex of Joplin, 1971) of Late Early-Middle Devonian age. It intrudes Late Ordovician sediments and several small unnamed tonalite bodies of the Moruya Igneous Complex.|16-MAY-23
26963|Tuross Head Granodiorite|Proposed publication|Chalker L.E. and Bembrick C.S. Narooma 1:100 000 Geological Sheet and Notes. Geol. Surv. NSW, Sydney.|16-MAY-23
26963|Tuross Head Granodiorite|Name first published by|Chalker L.E., Bembrick C.S., 1977|16-MAY-23
24558|Wangrah Adamellite|Name source|Wangrah trig. Station (1326 m) at GR 105259, Michelago 1:100 000 Geological Sheet.|16-MAY-23
24558|Wangrah Adamellite|Unit history|The adamellite was previously included under the name of Sapling Flat Granite (Joplin et al., 1953). Richards (1967) introduced the name Wangrah Adamellite.|16-MAY-23
24558|Wangrah Adamellite|Type section locality|The adamellite is well represented at GR 111255, where large pink tors outcrop in clusters.|16-MAY-23
24558|Wangrah Adamellite|Description at type locality|Biotite adamellite, containing quartz, K feldspar (microcline), plagioclase, biotite and rare muscovite. Textures vary from coarse to fine-grained to porphyritic. No xenoliths. Minor porphyritic phases within the adamellite have been included with it. These minor phases are characterised by the presence of hornblende.|16-MAY-23
24558|Wangrah Adamellite|Extent|The southern and central portions of the Sapling Flat Igneous Complex comprise the Wangrah Adamellite. The phse lies to the west of the Jerangle-Bredbo Road and to the west and southwest of Jerangle.  Size: 17 km2.|16-MAY-23
24558|Wangrah Adamellite|Relationships and boundaries|The Sapling Flat Igneous Complex, of which the Wangrah Adamellite is the major phase, intrudes Late Ordovician Foxlow Beds. The Narongo Fault forms the eastern boundary of the phase, placing the complex adjacent to the Kohinoor Volcanics of Late Silurian age.|16-MAY-23
24558|Wangrah Adamellite|Age reasons|Siluro-Devonian.|16-MAY-23
24558|Wangrah Adamellite|Proposed publication|Geological  Survey of NSW 1:100 000 Note Series|16-MAY-23
24558|Wangrah Adamellite|Unit name|Wangrah Adamellite (nov. after Richards 1967)|16-MAY-23
19453|Warderie Volcanics|Name source|Warderie property, GR 195960, Dubbo 1:250 000 sheet SI/55-4.|16-MAY-23
19453|Warderie Volcanics|Unit history|Included in the Oakdale Formation by various authors (Strusz 1958, 1960; Packham, 1969; etc).|16-MAY-23
19453|Warderie Volcanics|Type section locality|GR194958 to SI/55-4, shown on a text map (as "B6V8 to C3V4 in figure 1").|16-MAY-23
19453|Warderie Volcanics|Description at type locality|Rock types: Massive to autobrecciated flows and intrusives, conglomerates and breccias. A common rock type is poorly porphyritic andesite. Highly porphyritic andesite, spilite and altered trachyte are also present.|16-MAY-23
19453|Warderie Volcanics|Extent|Sensu stricto, covers a small area (<10 mi2).|16-MAY-23
19453|Warderie Volcanics|Thickness range|200-400 m.|16-MAY-23
19453|Warderie Volcanics|Relationships and boundaries|Overlies the Wylinga Formation (nov.) of acid volcanics and limestones, contact unexposed. Overlain disconformably(?) by the Catombal Park Formation (nov.) of acid volcanics and limestone. Part of Dripstone Group.|16-MAY-23
19453|Warderie Volcanics|Age reasons|Middle to Late Silurian, determined from corals, graptolites, calcareous algae, etc. in underlying and overlying strata. Formerly believed to be Ordovician.|16-MAY-23
19453|Warderie Volcanics|Proposed publication|Records, Geological Survey of NSW|16-MAY-23
19453|Warderie Volcanics|Defn approved by|Basden N. (Photocopy sent to Register 18/7/75 shows def. Approved by NSW Sub-Committee 27/6/75 signed J.H. Bryan).|16-MAY-23
19453|Warderie Volcanics|Name first published by|Baker C.J., Schmidt B.L., Shenwiy L., 1975|16-MAY-23
27252|Warraderry Porphyry|Name source|Hamlet of Warraderry (near Grenfell) GR 625827, Forbes 1:250 000.|16-MAY-23
27252|Warraderry Porphyry|Type section locality|GR 628826, Forbes 1:250 000, on hillside.|16-MAY-23
27252|Warraderry Porphyry|Extent|Crops out in a narrow north-south belt 3 km east of Warraderry. The belt is several hundred metres wide and 1 km long.|16-MAY-23
27252|Warraderry Porphyry|Lithology|Quartz - feldspar porphyry.|16-MAY-23
27252|Warraderry Porphyry|Relationships and boundaries|Intrusive dyke (?) into Late Ordovician sediments.|16-MAY-23
27252|Warraderry Porphyry|Age reasons|Probably Early Devonian by analogy with the Lawsons Gully Porphyry.|16-MAY-23
27252|Warraderry Porphyry|Defn author|Bowman H.N., 1977|16-MAY-23
27252|Warraderry Porphyry|Proposed publication|Forbes 1:250 000 Metallogenic Map|16-MAY-23
27252|Warraderry Porphyry|Name first published by|Bowman H.N., 1977.|16-MAY-23
33760|Waverly Creek Formation|Name source|Waverly Creek flows southwards south of the Mootwing National Park MNP (1:100,000 Nuchea 7335).|16-MAY-23
33760|Waverly Creek Formation|Unit history|None|16-MAY-23
33760|Waverly Creek Formation|Constituents|Ramparts Creek Sandstone Member (top) Rocky Tank Conglomerate Member (base)|16-MAY-23
33760|Waverly Creek Formation|Geomorphic expression|Lower part forms a valley whereas the upper part is more erosion-resistant.|16-MAY-23
33760|Waverly Creek Formation|Type section locality|1.5 km south of Rocky Tank South in an east flowing creek (lat. 31? 24?; long. 142?  22.5?)|16-MAY-23
33760|Waverly Creek Formation|Extent|Forms a narrow belt between Ramparts Creek in the southeast and the southern boundary of the Mootwingee National Park in the North.|16-MAY-23
33760|Waverly Creek Formation|Thickness range|110m|16-MAY-23
33760|Waverly Creek Formation|Lithology|Bouldery at the lower part fining up to coarse sandstone. The upper part is a fine-grained sandstone.|16-MAY-23
33760|Waverly Creek Formation|Depositional environment|Lower part fluvial, upper part is lacustrine.|16-MAY-23
33760|Waverly Creek Formation|Relationships and boundaries|The lower part is unconformable on the Snake Cave Sandstone whereas the upper part (the Ramparts Creek Sandstone) is conformable with the Rocky Tank Conglomerate Member (below) and the Ravendale Formation (above).|16-MAY-23
19672|Weelah Formation|Name source|Parish of Weelah, County Gipps.|16-MAY-23
19672|Weelah Formation|Type section locality|Northward trending road 10 km north of Burcher onwards. Cherts, manganiferous shales, sandstones and shales are exposed along this road. 533878 (bottom) to 531869 (top) 1:250 000.|16-MAY-23
19672|Weelah Formation|Extent|The unit is exposed along 20 km strike length, Parish of Weelah, Yarnel, Ilgindrie, Bogandillon.|16-MAY-23
19672|Weelah Formation|Thickness range|About 10,000 m in the north, thins out completely in the south.|16-MAY-23
19672|Weelah Formation|Lithology|The Weelah Formation is a thick clastic unit, consisting predominantly of shales and fine sandstones but containing also members of conglomerate, chert, and manganiferous shale. Although sandstones are the most characteristic outcrop expression of the Weelah Formation, there are also thick sequences of poorly outcropping micaceous shales. The stratigraphic sequence of the formation is as follows: a) Poorly outcropping shaly and sandy units overlying and grading up from the Manna Conglomerate; b) Bogandillon Chert member, about 500 m thick, and apparently a lenticular but persistent horizon, consisting of resistant dark grey massive chert; c) Manganiferous shale horizon. The thickness of this unit is difficult to estimate. However, very persistently, the shales overling the Bogandillon Chert are in many places stained with manganese veins and joint fillings.  d) Darby Conglomerate member. This unit forms the prominent Darby's Range in the north of the area. It is about 2000 m thick and consists of a massive sheared conglomerate of well rounded quartzite and quartz-sericite-schist pebbles and boulders. It is very similar to the Manna Conglomerate; e) Overlying the Darby Conglomerate member is a succession of fine argillaceous sandstones;  f) towards the top of these sandstones there is a horizon characterised by containing small and large dark grey massive chert lenses.|16-MAY-23
19672|Weelah Formation|Relationships and boundaries|The formation thins out or merges with the Manna Conglomerate to the south of the Burcher area, but in the north it thickens to about 10,000 m. Because of poor outcrop the contact with the underlying Manna Conglomerate cannot be readily defined. The upper contact is exposed in the T-junction of roads 10 km north of Burcher where sandstones of the Weelah Formation are in contact with the rhyolite tuff porphyry of the Cowal Member of the Ina Volcanics. The contact with the overlying Cowal Member of the Ina Volcanics is exposed at the T-junction mentioned previously. Because the sandstones overlying the Cowal Member rhyolite tuff porphyry are similar lithologically to those of the Weelah Formation, the change from the Weelah Formation to the Ina Volcanics is not a change in the sedimentary environment. The boundary is useful stratigraphically because the rhyolite tuff porphyry is a good marker horizon. As far as can be ascertained from the limited outcrop, the Weelah Formation appears to represent a deepening to the north of the Burcher sedimentary basin. It both overlies the Manna Conglomerate and is a lateral facies change of the Manna Conglomerate.|16-MAY-23
19672|Weelah Formation|Age reasons|Probably Silurian, from regional evidence. Encrinurus sp. Found just above Bogandillon Chert Member.|16-MAY-23
19672|Weelah Formation|Proposed publication|Bulletin Australian Society of Exploration Geophysicists (v.7 No. 1)|16-MAY-23
19672|Weelah Formation|Apprdate|12-OCT-1978|16-MAY-23
19672|Weelah Formation|Defn Reference|79/20208|16-MAY-23
19752|Werrie Formation|Name source|Werrie Basin (Carey, 1934).|16-MAY-23
19752|Werrie Formation|Unit history|Werrie Basalts (Hanlon, in Hill 1954) renamed Werrie Formation because the unit consists of Sandstones, conglomerates and basic lava flows - hence the lithologic term Basalts invalid. Member = Allombie Ash Fall Tuff (new name).  Host Formation = Werrie Formation.|16-MAY-23
19752|Werrie Formation|Type section locality|Werrie Basin, near Werrie Creek, NSW.  Location of Type Section: Located as above. Representative Section = Loder's Mountain Section along creek 835862 to 837867 then on easterly bearing to 834866 (Quirindi A-1:31 680 topographic sheets).|16-MAY-23
19752|Werrie Formation|Extent|Forms core of Temi Syncline and flanks of Back Creek Anticline.|16-MAY-23
19752|Werrie Formation|Thickness range|a) At type section: approximately 5000 ft; b) Maximum known: approximately 5000 ft; c) Representative Section: 1800 ft.|16-MAY-23
19752|Werrie Formation|Lithology|Basic lava flows and interbedded orthoconglomerates and lithic sandstones.|16-MAY-23
19752|Werrie Formation|Fossils|Allandale type fauna.|16-MAY-23
19752|Werrie Formation|Relationships and boundaries|The Werrie Formation conformably overlies the Temi Foramtion in most cases but occasionally is unconformable on the Willawarra Dacite, The Willow Tree Formation (Hanlon in Hill, 1954) disconformably overlies the Werrie Formation (Runnegar, 1970).|16-MAY-23
19752|Werrie Formation|Age reasons|Probable Allandale age (Runnegar, pers comm.), i.e. Early Permian.|16-MAY-23
19752|Werrie Formation|Proposed publication|Jour. & Proc. Royal Soc. NSW|16-MAY-23
19752|Werrie Formation|Defn approved by|Approved. Copies from xeros sent by NSW Stratigraphic Nomenclature Sub-Committee.|16-MAY-23
19752|Werrie Formation|Proposer|Lowe S.P.|16-MAY-23
31409|Willawarra Dacite|Name source|Willawarra Homestead 765807 (Quirindi A-D 1:31 680 topographic sheets)|16-MAY-23
31409|Willawarra Dacite|Unit history|Currabubula Formation in part.|16-MAY-23
31409|Willawarra Dacite|Type section locality|Back Creek Anticline, Willow Tree NSW.  Location of Type Section: Along Chilcotts Creek 812816 to 815822.|16-MAY-23
31409|Willawarra Dacite|Extent|Back Creek Anticline|16-MAY-23
31409|Willawarra Dacite|Thickness range|a) At type section:  800 ft;  b) Maximim known:  800 ft.|16-MAY-23
31409|Willawarra Dacite|Lithology|Dacitic Lava Flow|16-MAY-23
31409|Willawarra Dacite|Relationships and boundaries|The Willawarra Dacite conformably overlies the Kankool Formation. Where the Kankool Formation is not present the Willawarra Dacite conformably overlies the Chilcotts Mudstone. A low angle unconformity is developed at the top of the Willawarra Dacite and sometimes the formation has been completely eroded out. Hence the Willawarra Dacite is unconformably overlain by the Kerona, Temi or Werrie Formations.|16-MAY-23
31409|Willawarra Dacite|Age reasons|Late Carboniferous due to stratigraphic position.|16-MAY-23
31409|Willawarra Dacite|Proposed publication|Journal & Proceedings of the Roya Soc. NSW|16-MAY-23
31409|Willawarra Dacite|Category|2|16-MAY-23
31409|Willawarra Dacite|Defn approved by|From xerox copy sent by NSW Stratigraphic Nomenclature Sub-Committee|16-MAY-23
31409|Willawarra Dacite|Reserved? Yes/No|S.P. Lowe|16-MAY-23
26217|Williamsdale Volcanics|Name source|Village of Williamsdale; GR 933613, Michelago 1:100 000 sheet area.|16-MAY-23
26217|Williamsdale Volcanics|Unit history|Sharp (1949) introduced the name Keewong-Micaligo Porphyry Complex and subdivided the mass into the Keewong Porphyry, the Micaligo Porphyry and minor acid porphyries.|16-MAY-23
26217|Williamsdale Volcanics|Type section locality|Typical specimens of rhyodacitic crystal tuffs are found to the north of the Williamsdale-Burra road.|16-MAY-23
26217|Williamsdale Volcanics|Extent|Southern extremity at GR 953456 (Michelago 1:100 000) near Michelago village. The formation extends northwards for some 30 km with its northern boundary near the Queanbeyan-Royalla road.|16-MAY-23
26217|Williamsdale Volcanics|Thickness range|Possibly up to 4330 m thick.|16-MAY-23
26217|Williamsdale Volcanics|Lithology|Massive, rhyodacitic crystal lithic tuffs with a mild primary foliation are dominant, with rocks showing some variation in the crystal to lithic ratio. Rock fragments up to 130 mm long vary in composition between aplites, rhyolites and pumice to rhyodacites. Minor rhyolitic lavas or shallow intrusives are also present.|16-MAY-23
26217|Williamsdale Volcanics|Relationships and boundaries|Intertonguing relationship with the Colinton Volcanics. Along its eastern margin it is in partial faulted contact with the Late Ordovician Foxlow Beds.|16-MAY-23
26217|Williamsdale Volcanics|Age reasons|A Late Silurian age is postulated for the formation because of its stratigraphic relationship with a recognised Late Silurian formation i.e. the Colinton Volcanics.|16-MAY-23
26217|Williamsdale Volcanics|Proposed publication|Geological Survey of NSW 1:100 000 Note Series|16-MAY-23
26217|Williamsdale Volcanics|References|01/31638|16-MAY-23
26217|Williamsdale Volcanics|Unit name|Williamsdale Volcanics (nov.)|16-MAY-23
20182|Wiltagoona Sandstone Member|Name source|Wiltagoona Creek, GR 333166, Louth 1:250 000.|16-MAY-23
20182|Wiltagoona Sandstone Member|Unit history|Rayner (1969) included these beds in the Mulga Downs Group. Brunker (1969) included them in the Amphitheatre Beds.|16-MAY-23
20182|Wiltagoona Sandstone Member|Type section locality|A section has been measured by Durney (1975) from GR 360157 (the base) to 349157, Cobar 1:250 000. Good exposures of the member occur on ridges and gullies in this vicinity.|16-MAY-23
20182|Wiltagoona Sandstone Member|Extent|The unit is exposed over at least 150 km2 in the NW corner of the Cobar 1:250 000 Sheet (SH 55-14), NE corner of the Barnato 1:250 000 Sheet (SH 55-13) and SW corner of the Louth 1:250 000 Sheet (SH 55-9).|16-MAY-23
20182|Wiltagoona Sandstone Member|Thickness range|Durney (1975) measured about 1650 m of the member in the type section.|16-MAY-23
20182|Wiltagoona Sandstone Member|Lithology|Sandstone, fine to medium grained, quartzose; siltstone; minor claystone; thick bedded; some cross beds; extensively bioturbated.|16-MAY-23
20182|Wiltagoona Sandstone Member|Relationships and boundaries|Occurs in the upper part of the Amphitheatre Formation; overlain by laminated and bioturbated siltstones (Durney, 1975); underlain by thinly bedded, laminated sandstones, siltstones; and claystones commonly showing ripples, convolute bedding.|16-MAY-23
20182|Wiltagoona Sandstone Member|Age reasons|Part of Amphitheatre Formation which has been dated as Early Devonian (Sherwin, 1974).|16-MAY-23
20182|Wiltagoona Sandstone Member|Proposed publication|Quarterly Notes of the Geological Survey of New South Wales.|16-MAY-23
20182|Wiltagoona Sandstone Member|Name first published by|Baker C.J., Schmidt B.L., Sherwin L., 1975|16-MAY-23
37324|Woodsreef Ophiolitic Melange|Name source|The name is derived from Woodsreef Township (Cobbadah 1:100 000 topographic map sheet 9037 GR 832358) where the unit is well exposed.|16-MAY-23
37324|Woodsreef Ophiolitic Melange|Unit history|Woods Reef serpentine, Osborne 1950 (undefined); Woodsreef serpentine Proud and Osborne 1952 (undefined); Woodsreef Serpentinite, Glen and Heugh 1973 (undefined). All names were used informally to refer to part of the Great Serpentine Belt of Benson (1913) and revision to Woodsreef Ophiolitic Melange is proposed.  Synonomy: Great Serpentine Belt (Benson 1913), Peel Serpentinite (Crook 1961).|16-MAY-23
37324|Woodsreef Ophiolitic Melange|Type section locality|Stratotype: A type area is nominated as the Upper Bingara area from the township (Cobbadah 1:1000 000 topographic map sheet 9037 GR 728725) northwestwards along the road which follows Barrack Creek.|16-MAY-23
37324|Woodsreef Ophiolitic Melange|Extent|Discontinuous lenses and bodies up to 5 km wide which crop out immediately east of, and in some places a considerable distance to the east of the Peel Fault System for over 400 km.|16-MAY-23
37324|Woodsreef Ophiolitic Melange|Thickness range|Indeterminate.|16-MAY-23
37324|Woodsreef Ophiolitic Melange|Lithology|Serpentinite matrix ophiolitic melange containing blocks and slabs of unmetamorphosed gabbro, dolerite, plagiogranite, basalt, and sedimentary rocks.|16-MAY-23
37324|Woodsreef Ophiolitic Melange|Relationships and boundaries|Faulted contacts; structurally overlies Woolomin Group and is in turn structurally overlain by Dinoga Formation.|16-MAY-23
37324|Woodsreef Ophiolitic Melange|Age reasons|Indeterminate; metamorphosed by Late Carboniferous Bundarra Suite granitoids.|16-MAY-23
37324|Woodsreef Ophiolitic Melange|Proposed publication|Quarterly Notes Geological Survey NSW.|16-MAY-23
37324|Woodsreef Ophiolitic Melange|Comments|Metamorphism: Blocks range from unmetamorphosed to blueschist and eclogite.|16-MAY-23
20544|Wookookaroo Beds|Name source|"Wookookaroo Ck" Broken Hill 1:250 000 Sheet SH 54-14 GR 44330995.|16-MAY-23
20544|Wookookaroo Beds|Type section locality|Bottom GR 4586 1078 to top GR 4631 1114. Approximately 3400 m of metamorphosed interbedded shales, sandstones and quartzites. Three prominent chiastolite/andalusite schist horizons are present in the top 400 m. The section is along the old coach road from Poolamacca H.S. to Bijerkerno H.S. and the limits of the section are defined by Texas Bore (bottom) and the Old Lady Don Hotel (top).|16-MAY-23
20544|Wookookaroo Beds|Extent|The unit is exposed in the Euriowie Block, west and southwest of Bijerkerno H.S. and covers an area of at least 95 km2. The same unit (or more precisely its presumed stratigraphic equivalent) is also developed around Brewery Well in the Broken Hill Block proper.|16-MAY-23
20544|Wookookaroo Beds|Lithology|Well bedded psammopelites with interbedded pelites and quartzites. Graded bedding common within psammopelites. Beds range in thickness from 10 cm to 100 cm rarely massive. Metamorphic grade decreases generally down the section. Grain size is of ten coarse destroying the primary sedimentary mesofabric.|16-MAY-23
20544|Wookookaroo Beds|Relationships and boundaries|The unit is conformably overlain by the Bijerkerno Beds, Rose (1970), and overlies a complex series of gneisses and amphibolites with uncertain relationships. Discordance of gneisses at the contact suggests either an unconformity or the presence of a nappe structure. The top of the Wookookaroo Beds is defined by a 2-3 m thick laminated calc-silicate horizon which is a very prominent marker.|16-MAY-23
20544|Wookookaroo Beds|Age reasons|The Wookookaroo Beds belong to the Willyama Complex which is est. about 1800 m.y., Shaw (1968). The Rb/Sr age on the first metamorphic event is approximately 1650-1700 m.y., Pidgeon (1967), Shaw (1968). The age therefore is probably late Early Proterozoic to Middle Proterozoic.|16-MAY-23
20544|Wookookaroo Beds|Proposed publication|Journal of the Geological Society of Australia (v.25, pt 1, 2).|16-MAY-23
20544|Wookookaroo Beds|Name first published by|Tuckwell K.D., 1978|16-MAY-23
33405|Yarrimbah Chert|Name source|Yarrimbah station, 12 km NW of Parkes. Parkes 1:50 000 GR 999 399, Forbes 1:250 000 GR 612 910.|16-MAY-23
33405|Yarrimbah Chert|Extent|Scattered float, except where exposed in shallow gravel pits, on low hills between Nelugaloo and Goonumbla, forming a marker band within the Forbes Anticline. |16-MAY-23
33405|Yarrimbah Chert|Thickness range|About 85 m exposed in type locality.|16-MAY-23
33405|Yarrimbah Chert|Lithology|Dominant lithology is chert, dark grey when fresh, with occasional pyritic nodules. At Yarrimbah there is a thin bed of conglomerate below the chert, which contains pebbles of volcanic rock. At the type area the formation overlies trachytic porphyritic volcanics, but the upper boundary is obscured. Elsewhere, the Yarrimbah Chert is overlain by an almost aphyric black amygdaloidal lava (Nelungaloo Volcanics). Thick conglomerate beds are present at Wilga, a few kilometres west of Yarrimbah, and there are thin bands of volcanic derived sandstone.|16-MAY-23
33405|Yarrimbah Chert|Age reasons|Early Ordovician, possibly La3 based upon graptolite fauna with Tetragraptus (Eotetragraptus) approximatus.|16-MAY-23
33405|Yarrimbah Chert|Proposed publication|Alcheringa|16-MAY-23
33405|Yarrimbah Chert|Category|2|16-MAY-23
33405|Yarrimbah Chert|First Reference|87/25805|16-MAY-23
33405|Yarrimbah Chert|Reserved? Yes/No|Yes|16-MAY-23
