Quarterly Notes Geological Survey of New South Wales

September 2011 No 137 A review of Cambrian and Ordovician stratigraphy in New South Wales

Abstract We present a comprehensive review of a significant interval spanning 100 million years in the geological history of New South Wales, listing all currently accepted groups, formations and constituent members of Cambrian and Ordovician age. These units are briefly described and placed in their tectonic context, with the most up-to-date biostratigraphic and isotopic age dating assembled to constrain correlations (depicted in 25 representative stratigraphic columns) across orogenic belts and terranes. Rock units previously assigned a Cambrian or Ordovician age, whose names are now obsolete, redundant or are known to be younger, are also discussed or listed in an appendix. The increasingly diverse literature on the Cambrian and Ordovician stratigraphy of the state is reflected in an extensive bibliography. This review is intended to benefit the mineral exploration industry, research workers both locally and overseas, and geological mapping generally by providing a ready reference to Cambrian and Ordovician rocks in NSW. It also indicates where current data are insufficient to resolve precise age determinations and correlations, thereby highlighting those areas that require further work before a complete synthesis of the early Palaeozoic geological history of NSW can be undertaken. Keywords: Cambrian, Ordovician, New South Wales, stratigraphy, biostratigraphy, Delamerian Orogen, Lachlan Orogen, New England Orogen, Narooma Terrane.

Introduction The Cambrian and Ordovician periods span an throughout the Ordovician (Glen 2005; Glen et al. 2009). interval of almost exactly 100 million years, from Cambrian rocks are therefore, in comparison with 542–443 Ma, during which the New South Wales Ordovician strata, relatively poorly represented areally portion of the Tasmanides expanded from restricted in NSW. They are best known from the Koonenberry accumulation on the Delamerian continental margin Belt in the far west of the state (Figure 1), the subject of a and a few distant seamounts during the Cambrian, to regional mapping program completed by the Geological an extensive complex of depositional settings including Survey of New South Wales (Greenfield et al. 2010). back-arc basin, volcanic island arc and offshore terranes As a result of numerous palaeontological studies in

AUTHORS I.G. Percival1, C.D. Quinn2 and R.A. Glen2 1 Geological Survey of New South Wales, W.B. Clarke Geoscience Centre, Londonderry, NSW 2753 2 Geological Survey of New South Wales, 516 High Street, Maitland, NSW 2320

© State of New South Wales through the Division of Resources and Energy, 2011 Papers in Quarterly Notes are subject to external review. External reviewer for this issue was Dr Barry Webby, Honorary Associate, Earth and Planetary Sciences, Macquarie University. His assistance is appreciated. Quarterly Notes is published to give wide circulation to results of studies in the Geological Survey of New South Wales. Papers are also welcome that arise from team studies with external researchers. Contact: [email protected] ISSN 0155-3410 Geological Survey of New South Wales Contents the past two decades, the stratigraphy of this region is much better known than was the case for the synthesis Abstract 1 of Shergold et al. (1985), which was largely reliant on

Introduction 1 unpublished thesis mapping by Warris (1967). The present review summarises the most recently available Delamerian Orogen 5 biostratigraphic data for the Koonenberry Belt to enable Koonenberry Belt 5 better-constrained correlation with other regions in Thomson Orogen 13 the Delamerian Orogen, such as those in the Flinders Ranges of South Australia. Elsewhere in NSW, very Lachlan Orogen — continental margin terranes 13 localised occurrences of fossiliferous ‘Middle’ Cambrian Albury–Bega Terrane 14 rocks (represented by limestone clasts) have been Hermidale Terrane 19 documented from Batemans Bay on the south coast, and in blocks along the Peel–Manning Fault system in the Oceanic crust and associated units 20 New England Orogen southeast of Tamworth. Cherts at Macquarie Arc 21 the base of the succession at Narooma on the south coast are of Late Cambrian age, and the Adaminaby Group in Narooma Terrane 26 this area also spans the Cambro-Ordovician boundary New England Orogen 27 (Glen et al. 2004). Though direct age control is lacking, Tamworth Belt 27 serpentinite in the Port Macquarie Block is inferred to Port Macquarie Block 28 be Cambrian. Ordovician rocks occupy approximately 20% Synthesis 28 of surface exposures in NSW (Figure 2), with a Acknowledgements 29 considerably greater subsurface extent. They host some References 29 of the most productive metalliferous deposits in the state. Largely due to their economic importance these Appendix 39 rocks have been the focus of recent and continuing mapping programs and associated research studies by the Geological Survey of New South Wales and other institutions. A large number of publications describing Cover photograph: View towards Dunhill Bluff from Fossil Hill, showing the thin-bedded Fossil Hill Limestone Ordovician rocks in NSW, many in specialist journals, and the lower part of the overlying massive Belubula have appeared since the Australasia-wide synthesis Limestone. Both units are of Late Ordovician age. of Webby et al. (1981). It is therefore timely to review (Photographer: S Meakin). the stratigraphic nomenclature established over the past three decades in order to provide a convenient synthesis from which to develop local and state-wide correlations. For that part of the Macquarie Arc in central NSW, the recent stratigraphic review of Percival Production co-ordination: Geneve Cox and Glen (2007) stands with some minor revisions. That review was largely built on the results of regional Geological editor: Simone Meakin mapping programs for the Bathurst, Dubbo and Forbes 1:250 000 sheet areas, combined with substantial Geospatial information: Cheryl Hormann research input from CODES (Centre of Excellence in Layout and charts: Carey Martin Ore Deposits, at the University of Tasmania). Extensive deep marine basins dominated by clastic sedimentary rocks of turbiditic origin, associated pelagic deposits and graptolitic shales, form the Albury–Bega Terrane and Hermidale Terrane in the centre and south of NSW (modified by Glen et al. 2009 after Glen 2005). Together with the chert-dominated oceanic terrane localised around Narooma on the far south coast (Glen et al. 2004), these deep marine sequences have only relatively recently become stratigraphically subdivisible The information contained in this publication is based on knowledge and understanding using conodont-based biostratigraphic zones. This at the time of writing (June 2011, revised October 2011). However, because of advances allows more precise correlations with the well-known in knowledge, users are reminded of the need to ensure that information upon which turbidite-dominated and graptolitic shale successions they rely is up to date and to check currency of the information with the appropriate of Victoria, the stratigraphy of which were recently officer of the Division of Resources and Energy, or the user’s independent adviser. synthesised by VandenBerg et al. (2000), Fergusson and

2 September 2011 Figure 1. Schematic map of the New South Wales portion of the southern Tasmanides showing distribution of Cambrian rocks in a) Delamerian Orogen and b) New England Orogen. Numbers refer to stratigraphic sequences discussed in text and depicted in Figure 5.

Quarterly Notes 3 Figure 2. Schematic map of the New South Wales portion of the southern Tasmanides showing distribution of Ordovician rocks in a) Delamerian Orogen and b) Lachlan Orogen, New England Orogen and Narooma Terrane. Numbers refer to stratigraphic sequences discussed in text and depicted in Figure 5.

4 September 2011 VandenBerg (2003), and Glen et al. (2009). Ordovician Restricted to a small area of exposure on the far south rocks of the New England Orogen are sparsely coast of the state, the Narooma Terrane (Glen et al. 2004) represented by shallow water lithologies including was accreted to the Albury–Bega Terrane during the limestone (some reworked into younger strata) along Late Ordovician. The stratigraphy of one or more poorly the Peel Fault, together with deep water sediments and known and as-yet unnamed oceanic floor terrane(s) pillow basalts of an accretionary complex in the Port associated with serpentinised belts in southern NSW is Macquarie region. Although areally restricted, they the focus of current work. provide critical tie points in correlations to rocks of the Lachlan Orogen. Delamerian Orogen Chronostratigraphic subdivisions of the Cambrian and Ordovician periods have been the subject of Further details of the stratigraphic units discussed in the ongoing revision in recent years. For the Ordovician we following section are provided in Greenfield et al. (2010). use a timescale based on that of Sadler et al. (2009), and Only the most significant fossil occurrences necessary for the Cambrian that of Shergold and Cooper (2004), to support biostratigraphic correlations are given in this modified internally with international subdivisions review; full listings are presented in Percival (2010). recommended by the respective stratigraphic subcommissions and ratified by the International Koonenberry Belt (Figure 5, columns 1–5) Commission on Stratigraphy (Ogg et al. 2008). The ICS timescale adopts a bipartite subdivision of the Mutawintji–Mount Wright area (Figure 5, column 1) Cambrian into Early and Late, but to facilitate Australia- Early and ‘Middle’ Cambrian rocks older than wide correlations of Cambrian rocks already in the ~500 Ma, of mostly shallow water lithologies in the literature, the currently accepted central and northern central Koonenberry Belt, are assigned to the Gnalta Australian trilobite zonation for ‘Middle’ and Late Group (originally named by Warris 1967; redefined Cambrian time (Figure 3) is also employed here (based by Percival, in Greenfield et al. 2010). The base of the on the recent review of Cambrian biostratigraphy in oldest formation, the Mount Wright Volcanics, is not Australia by Kruse et al. 2009), with the informal status exposed, but this unit (at least 1375 m thick) is presumed of ‘Middle’ Cambrian designated by use of diacritical to be as old as the Atdabanian (Early Cambrian, marks. We follow Laurie (2006, figure 3) in placing the Figure 3). The Coonigan Formation is the topmost Early–‘Middle’ Cambrian boundary in the latest Ordian, unit of the Gnalta Group, directly underlying the with the Mindyallan–Idamean boundary taken to be the Delamerian unconformity, and may be as young as late end of the ‘Middle’ Cambrian. Essentially the Australian Templetonian (‘Middle’ Cambrian). ‘Middle’ Cambrian equates to Series 3 of the ICS First recognised by Warris (1967), the Mount Wright Cambrian timescale. For biostratigraphic subdivisions Volcanics was redefined by Crawford et al. (1997) as of the Ordovician (Figure 4), we use the Australasian consisting primarily of calc-alkaline andesite and dacite graptolite-based zonal scheme of VandenBerg and with minor basaltic andesite, intruded by microdolerite Cooper (1992), together with a conodont biozonation to microdiorite dykes, overlying a lower section being developed for eastern Australia (Percival et al. in comprised of massive dark cherts interbedded with prep.). Statewide correlations of significant Cambrian altered basalts, siltstones, and prominent dolomitised and Ordovician strata are discussed in the text (with limestones. The limestones contain columnar currently accepted stratigraphic names shown in bold stromatolites of indeterminate age. Öpik (1976) recorded font), and these are depicted in Figure 5. (without description or illustration) fragments of Glen (2005) reviewed the stratigraphy and tectonic shelly microfossils including Tommotia, phosphatic evolution of the Tasmanides of eastern Australia, brachiopods, Chancelloria spicules and algal structures which in NSW includes the continental margin of the resembling Vermiculites, from isolated limestone Delamerian Orogen in the far west of the state (including lenses within volcanic rocks in the upper part of the largely sedimentary rocks of the Koonenberry Belt), formation. From the same lenses, Kruse (1982) described the poorly known Thomson Orogen in the northwest, 13 archaeocyathan species forming his assemblage the New England Orogen occupying the northeastern Fauna 1, to which Zhuravlev and Gravestock (1994) corner, and the intervening Lachlan Orogen that largely assigned an age equivalent to early Botoman. dominates the central and southern regions of NSW. Although all known contacts between the Mount New terminology has recently been introduced (Glen Wright Volcanics and the overlying Cymbric et al. 2009) for Ordovician terranes in the Lachlan Vale Formation (Warris 1967) are faulted, there is Orogen. Within NSW, these include the Albury–Bega unlikely to be a significant time gap between them Terrane (incorporating turbidite-dominated successions as Archaeocyathid Fauna 1 of Kruse (1982) is present and overlying Late Ordovician black shales west and in allochthonous limestone lenses in both the upper east of the Macquarie Arc), and the Hermidale Terrane Mount Wright Volcanics and the lower half of the (represented by the Girilambone Group in central NSW). Cymbric Vale Formation. Estimates of the thickness

Quarterly Notes 5 Australian ‘Middle’­–Late Cambrian Late Cambrian–Early Ordovician Ma stages trilobite zonation conodont zonation

Warendan Chosonodina herfurthi– 490 Cordylodus angulatus Cordylodus lindstromi ORD. C. prolindstromi–Hirsutodontus simplex Datsonian Cordylodus proavus 492 Mictosaukia perplexa Hispidodontus discretus Neoagnostus quasibilobus–Shergoldia nomas Hispidodontus appressus Payntonian Hispidodontus resimus

Stage 10 Sinosaukia impages Rhaptagnostus clarki maximus–Rhaptag. papilio Teridontus nakamurai Rhaptag. bifax–Neoagnostus denticulatus 494 Rhaptag. clarki prolatus–Caznaia sectatrix Iverian Rhaptag. clarki patulus–Caznaia squamosa Peichiashania tertia–Peichiashania quarta Stage 9 Peichiashania secunda–Prochuangia glabella 496 Wentsuia iota–Rhaptagnostus apsis Irvingella tropica FURONGIAN Stigmatoa diloma Idamean Erixanium sentum 498 Proceratopyge cryptica Paibian Glyptagnostus reticulatus

Glyptagnostus stolidotus 500 Mindyallan Acmarhachis quasivespa Erediaspis eretes 502 Damesella torosa–Ferenepea janitrix Guzhangian Boomerangian Lejopyge laevigata

Goniagnostus nathorsti 504 Undillan Doryagnostus deltoides Ptychagnostus punctuosus

Euagnostus opimus 506 Drumian Floran Acidusus atavus

‘SERIES 3’ Triplagnostus gibbus Pentagnostus shergoldi 508 Templetonian Pentagnostus praecurrens

Stage 5 Pentagnostus anabarensis Xystridura negrina association Ordian Redlichia forresti association 510 Toyonian

512

514 Stage 4

516 Botoman

518 ? ‘SERIES 2’

520 Siberian stages

522 Stage 3 Atdabanian 524

526 Stage 2 Tommotian 528 TERRENEUVIAN

Figure 3. Cambrian timescale and biostratigraphic zonation used in NSW, based on a review of Cambrian biostratigraphy in Australia by Kruse et al. (2009). Note that the informal status of ‘Middle’ Cambrian (that approximates Series 3 of the ICS Cambrian timescale) is designated by use of diacritical marks. Placing the Early–‘Middle’ Cambrian boundary in the latest Ordian, with the end of the ‘Middle’ Cambrian equivalent to the Mindyallan–Idamean boundary, follows Laurie (2006, figure 3).

6 September 2011

Australian Pacifi c Province Open-sea Ma stages graptolite zones conodont zones SILURIAN 444 HIRNANTIAN Bo5 Normalograptus? persculptus Bo4 Normalograptus? extraordinarus Bo3 Paraorthograptus pacifi cus 446 Bolindian Amorphognathus ordovicicus

Bo2 (pre-pacifi cus) 448 Bo1 Climacograptus? uncinatus Dicranograptus gravis Ea3–4 Dicellograptus kirki 450

Ea2 Diplacanthograptus lanceolatus Amorphognathus superbus KATIAN 452 Eastonian

454 UPPER Ea1 Diplacanthograptus spiniferus Baltoniodus alobatus subzone

456 Gi2 Orthograptus calcaratus Baltoniodus gerdae subzone

458 Gisbornian Baltoniodus variabilis subzone Gi1 Nemagraptus gracilis Amorphognathus traerensis

460 SANDBIAN

Pygodus anserinus

462 Da4 Archiclimacograptus riddellensis

Pygodus serra 464

Darriwilian Da3 Pseudoclimacograptus decoratus Eoplacognathus suecicus 466

468 DARRIWILIAN Eoplagnathus variabilis Da2 Undulograptus intersitus MIDDLE 470 Da1 Undulograptus astrodentatus Baltoniodus norrlandicus Ya2 Cardiograptus morsus Yapeenian 472 Ya1 Otricograptus upsilon Paroistodus originalis Isograptus victoriae maximodivergens Baltoniodus navis Ca3–4 Isograptus victoriae maximus Isograptus victoriae victoriae Baltoniodus triangularis DAPINGIAN Ca2 474 Castlemainian Ca1 Isograptus victoriae lunatus Oepikodus evae Isograptus primulus 476 Chewtonian Ch1–2 Didymograptus protobifi dus Be2–4 Pendeograptus fruticosus 3 & 4 branched 478

FLOIAN Bendigonian Be1 Pendeograptus fruticosus Prioniodus elegans 480

Tetragraptus approximatus 482 La3 Araneograptus murrayi La2b Paroistodus proteus

484 LOWER La2a Aorograptus victoriae

Lancefi eldian Paltodus deltifer 486 La1b Psigraptus jacksoni

488 La1a Anisograptus TREMADOCIAN Cordylodus angulatus Rhabdinopora fl abelliformis parabola 490

CAMBRIAN Figure 4. Ordovician timescale and biostratigraphic zonation used in NSW, based on the graptolite zonation of VandenBerg and Cooper (1992), together with the open sea conodont biozonation. Timescale from Sadler et al. (2009).

Quarterly Notes 7 of the Cymbric Vale Formation vary between 1500 m overlain by about 14 m of white micaceous shale of the (Warris 1967) and 1900 m (Kruse 1982). Predominant uppermost Coonigan Formation. From this shale a lithologies are tuffs and cherts, the latter generally diverse trilobite fauna is known (Öpik 1968, 1970, 1975, with a green hue. In the upper part of the formation, 1979, 1982; Shergold 1969; Laurie 1988), of essentially the two limestone lenses (one allochthonous, the other same earliest ‘Middle’ Cambrian age (though possibly biohermal) contain Archaeocyathid Fauna 2, which has extending into the late Templetonian) as that assigned to no species in common with the older assemblage (Kruse the First Discovery Limestone Member. Revision of the 1978, 1982). Many species in this younger fauna also Australian Cambrian biostratigraphic scheme (Shergold occur in the Syringocnema favus beds in the Arrowie 1996) has merged the concept of Öpik’s Ordian and and Stansbury basins of South Australia, of mid to late lower Templetonian stages, correlating the interval Botoman age (Zhuravlev & Gravestock 1994; Kruse & occupied by the First Discovery Limestone Member with Shi, in Brock et al. 2000). The uppermost beds (lithic the late Toyonian. and feldspathic sandstone, and associated impure iron- Late Cambrian to Middle Ordovician formations rich carbonate) of the Cymbric Vale Formation contain overlying the Delamerian unconformity in the central trilobites, brachiopods and monoplacophoran molluscs Koonenberry Belt are represented by the Mutawintji (Öpik 1976). Additional trilobites described by Jago et al. Group (redefined by Greenfield, Mills & Percival, (1997) and Paterson (2005) high in the upper Cymbric in Greenfield et al. 2010). Formerly known as the Vale Formation are of late Botoman aspect, confirming Mootwingee Group, the name was changed at the the age of Archaeocyathid Fauna 2. request of the indigenous custodians of the Mutawintji Isotopic dating using SHRIMP II U–Pb analyses Historic Site to better reflect its original pronunciation of zircons from a tuffaceous bed in the Cymbric Vale (Sharp 2004). Deposition commenced with basal Formation, which was interpreted by Paterson (2005) conglomerate (represented by the Nuchea Conglomerate to lie just above the lower archaeocyathid-bearing in the Mutawintji area), that is overlain successively limestone lenses of Kruse (1982), gave an age of by the Nootumbulla Sandstone, Bynguano Quartzite 510.5 ± 2.9 Ma (Black 2007). This is consistent with and Rowena Formation, displaying a rapid transition an age of 510.3 ± 3.2 Ma obtained from slightly higher from fluviatile to shallow marine environments with in this formation (Black 2005). These ages are slightly significant clastic influx derived from an extensive delta younger than the early Botoman age derived from (Webby 1978, figure 3; Webby 1983). A comparable correlations of Archaeocyathid Fauna 1 of Kruse (1982). succession is recognised in the Scropes Range, south of A disconformable relationship between the Cymbric the Barrier Highway (Figure 5, column 4), although a Vale Formation and the overlying Coonigan Formation different set of facies is present there. (Warris 1967) (uppermost unit of the Gnalta Group) The Nuchea Conglomerate (defined by Greenfield & was exposed in a trench excavated on the western limb Percival, in Greenfield et al. 2010) was first distinguished of the Gnalta Syncline (Roberts & Jell 1990, figure 2). in the Mutawintji area by Sharp (2004) where it attains a Evidence for the time break is provided by the presence maximum thickness of about 50 m. The conglomerate, of angular fragments of the Cymbric Vale Formation of fluvial origin, is clast-supported and consists of within basal limestone of the Coonigan Formation, in well-polished and highly rounded resistant blue–grey addition to the occurrence of the upper Ordian trilobite orthoquartzite and metaquartzite pebbles, cobbles and Redlichia petita Öpik, 1970 in overlying shales. Above boulders. The formation is also recognised to the south, these shales, the First Discovery Limestone Member in the Scropes Range between Wilcannia and Broken (first defined in Jell et al. 1985) is at least 115 m thick Hill (Pahl & Sikorska 2004). and forms much of the Coonigan Formation. Girvanella The overlying Nootumbulla Sandstone (redefined and algal oncolites occur in the lowermost beds of this by Percival, in Greenfield et al. 2010) comprises limestone, which are overlain by highly fossiliferous ~150–200 m of interbedded red shales, conglomerate limestone with a rich and diverse silicified fauna, lenses, and sandstones, initially feldspathic but comprising molluscs (Runnegar & Jell 1976), corals (Jell becoming more quartzose towards the top (Webby & Jell 1976), echinoderms (Jell et al. 1985), sphinctozoan 1978). In its type area on the east limb of the Gnalta sponges (Pickett & Jell 1983), brachiopods (Roberts & Syncline, the base of the Nootumbulla Sandstone Jell 1990), hyoliths, tommotiids and chancelloriid sponge is defined by the first appearance of interbedded spicules. Also present in this limestone is an abundant sandstone and shale above the Nuchea Conglomerate. trilobite fauna, of which only a few species have been The Nootumbulla Sandstone is interpreted to have been described by Jell (1975). The diverse assemblage of the deposited in a shallow marine environment, probably First Discovery Limestone Member is typical of the subject to influxes of deltaic sediment. Late Cambrian Peronaspis longinqua or Triplagnostus gibbus zones of fossils are common throughout; Shergold (1971) noted the Templetonian Stage (Roberts & Jell 1990). The upper saukiid and tsinaniid trilobites of Payntonian age within half of the First Discovery Limestone Member consists the lowermost beds. A thin limestone horizon in the of interbedded limestone, green siltstone and sandstone, middle part of the formation south of Mount Wright

8 September 2011 yields early Datsonian (Cordylodus proavus conodont marine environment. Zhen and Percival (2006) deduced Zone) conodonts (Zhen & Percival 2006). Uppermost an Early Ordovician age (Oepikodus evae conodont beds of the Nootumbulla Sandstone contain a prolific Zone) from a small but diverse conodont fauna from fauna dominated by trilobites of early Datsonian (latest a thin calcareous horizon in the lower to middle part Cambrian) age (Shergold 1971). These trilobites, which of the Rowena Formation. However, this conflicts with include Chuangiella and apatokephalids (Droser et al. an early Darriwilian age derived from the presence of 1994), remain undescribed. two fossils — the trilobite Prosopiscus tatei described Conformably overlying the Nootumbulla Sandstone from the Rowena Formation by Paterson (2006), and is the Bynguano Quartzite, consisting predominantly Arandaspis sp., identified by Young (2009) from a single of quartzite and cross-bedded sandstone about 330 m fish plate impression in the upper part of the Rowena thick. Droser et al. (1994) renamed the unit the Formation — that also occur in the Stairway Sandstone Bynguano Formation without justification, and on the in the Amadeus Basin. The discrepancy between basis of lithology and long-established priority, the the age based on conodonts, and that suggested by original name of Warris (1967) is retained. Diverse Prosopiscus tatei and Arandaspis, might be resolved if trace fossil assemblages indicative of a shallow marine the horizon in which the trilobite occurs lies within depositional environment are prolific throughout the upper (rather than the middle) part of the Rowena the formation (Webby 1983, Droser et al. 1994). Both Formation. Alternatively, there may be an unrecognised pre-depositional crawling traces (characterised by disconformity within the middle part of the unit, with abundant Rusophycus), and post-depositional tiered the lower part of the Middle Ordovician unrepresented. burrows have been recognised. Shelly faunas, including trilobites and helicotomid gastropods, are present Mount Arrowsmith (Figure 5, column 2) though few have been named or described. Shergold A Cambrian sequence correlated with the Gnalta Group (1971) mentioned the occurrence of richardsonellinid occurs on the western flank of Mount Arrowsmith, at and leiostegiid trilobites in the lower part of the the northern end of the Koonenberry Belt (Figure 1). Bynguano Quartzite, comparable with those in the The sequence was first studied by Warris (1967, 1969) uppermost Nootumbulla Sandstone, which suggests who established the stratigraphic terminology that a similar earliest Datsonian (latest Cambrian) age. remains in use, and by Wopfner (1967) who first Droser et al. (1994) recorded Microagnostus sp. and published a detailed map of the area. The stratigraphy saukiid trilobites from the basal 50 m of the formation. has recently been revised by Brock and Percival (2006). A younger trilobite assemblage in the upper part The oldest Cambrian unit, the Pincally Formation, is of the unit with asaphids, dikelokephalinids and at least 260 m thick, but as its base is not exposed the protopliomerids, indicative of an earliest Ordovician relationship with the underlying Neoproterozoic Kara (Warendan) age, implies that the Bynguano Quartzite Formation is undetermined. Poorly exposed grey–green spans the Cambro-Ordovician boundary. phyllitic siltstone and fissile shale comprise most of the The Bynguano Quartzite is conformably succeeded Pincally Formation, with a carbonate lens in the lower by the ~1700 m-thick Rowena Formation (Warris 1967) third and three prominent thin-bedded limestones in that consists of interbedded quartzose sandstones, the upper third of the unit. The diverse microfauna siltstones and shales with occasional calcareous beds in recovered from the limestones, which includes the middle. At the base of the formation is an unnamed chancelloriid sponge spicules, lingulate brachiopods, resistant quartzite up to 18 m thick. Another significant molluscs, hyolithids, hyolithelminthes and echinoderm quartzite, the Gundara Quartzite Member (defined sclerites (Brock & Percival 2006), indicates a shallow by Percival, in Greenfield et al. 2010) occurs in the marine setting. This assemblage is closely comparable upper part of the formation and includes a distinctive with that from the First Discovery Limestone Member conglomerate with angular clasts of vein quartz. Shelly of the Coonigan Formation, supporting an identical fauna, including trilobites (mostly undescribed) and latest Early Cambrian age (Toyonian, or Ordian–early lingulide brachiopods, are present in sandstones and Templetonian), based on the presence of Pelagiella siltstones in the middle part of the Rowena Formation. madianensis in the upper part of the Pincally Formation. The lingulide brachiopods were first documented by The Pincally Formation is conformably overlain Fletcher (1964) and have recently been redescribed by the Wydjah Formation, with the base of the by Percival and Engelbretsen (2007), who recognised latter unit marked by the appearance of a distinctive species of Hyperobolus, Lingulobolus, and the new genus cross-bedded, white quartz-rich sandstone (Brock Rowenaglossa. Webby (1983) documented the trace & Percival 2006). The Wydjah Formation is readily fossil Rusophycus from the lower part of the formation subdivisible into a lower and an upper upwards- above the basal conglomeratic quartzite. Skolithos is coarsening sand-dominated sequence (both culminating also recorded from these beds as well as higher in the in conglomeratic layers), separated by the Pimpira formation (Shergold et al. 1982). The trace fossils and Member that consists of four to five prominent lingulide brachiopods suggest a shallow water nearshore dolostone beds (and numerous thin and intermittent

Quarterly Notes 9 dolostones) separated by recessive phyllitic siltstones The overlying Tabita Formation is characterised by and shales. Total thickness of the Wydjah Formation interbedded limestone and dolomite. Estimates of the is 250 m, comprising 87 m for the lower unit, 74 m for thickness of the Tabita Formation vary from 82–130 m the Pimpira Member (including 8–9 m total thickness (Zhen, Percival & Webby 2003) to 190 m (Warris 1967). of dolostones), and 89 m for the upper unit (Brock & The strata are richly fossiliferous, yielding a varied Percival 2006). The upper and lower sandstone units macrofauna including nautiloids (Crick & Teichert are generally unfossiliferous. Several beds of granule 1983; Stait & Laurie 1985), brachiopods (Paterson & conglomerate, each up to 0.5 m thick and characterised Brock 2003), trilobites (Paterson 2004) and undescribed by detrital feldspar and volcanic debris, occur in the gastropods and bivalves. Conodonts from the Tabita middle Pimpira Member. A similar layer with angular Formation (Zhen et al. 2001, Zhen, Percival & Webby clasts both of volcanics and granite is found ~10 m 2003; Percival et al. 2003) are more diverse than in the below the top of the unit (K.J. Mills & R.A. Glen, field underlying Yandaminta Quartzite, but are of essentially observations 2006). The provenance of the volcaniclastic the same late Early Ordovician age. Both units were horizons is presently unresolved, although they may deposited on a shallow marine shelf. be related to similar beds present in the slightly older In the core of an overturned syncline on the west Cymbric Vale Formation of the Gnalta area to the south. flank of Mount Arrowsmith, the youngest shell coquina Dolostones of the Pimpira Member have yielded a of the Tabita Formation is conformably succeeded faunal assemblage comparable to that in the Pincally by the Pingbilly Formation, which is approximately Formation, though slightly less diverse. The chaotic 70 m thick. It comprises poorly outcropping micaceous brecciated appearance of the upper dolostone beds, mudstone that occasionally contains subangular which are also characterised by large algal oncolites, to rounded lithic clasts varying from 0.5–40 mm suggests very shallow water and a well agitated diameter. The age of the Pingbilly Formation is poorly depositional environment, possibly a lagoon affected by constrained, with only one fossil — the brachiopod periodic storms. Age is latest Early Cambrian (Ordian– Celsiorthis bulancis — having been described from it early Templetonian, or Toyonian), similar to the (Paterson & Brock 2003). As this species also occurs in underlying Pincally Formation, based on the presence of the underlying Tabita Formation, the two units are likely Pelagiella madianensis in the basal beds of the Pimpira to be of similar age. Member (Brock & Percival 2006). The absence of sandstones distinguishes the Koonenberry and adjacent areas (Figure 5, column 3) conformably overlying Wyarra Shale, defined by Brock In the Coturaundee Range, the Copper Mine Range and Percival (2006), from the Wydjah Formation. The Formation, redefined by Mills (in Greenfield et al. 2010), Wyarra Shale is estimated to be about 50 m thick and is is of probable Early or ‘Middle’ Cambrian age, based on dominated by strongly cleaved, unfossiliferous maroon, a trace fossil assemblage including Chondrites sp. and purple and khaki shales. It is either unconformably Planolites sp. documented by Webby (1984). Sponge overlain by, or is faulted against, the Ordovician Pimbilla spicules and possible paterinide brachiopods in this unit Tank Group immediately to the east. also imply a Cambrian age. The Teltawongee Group The Pimbilla Tank Group (defined by Percival, in (Mills, in Greenfield et al. 2010; previously Teltawongee Greenfield et al. 2010) includes in ascending order, beds of Mills 1992) consists of weakly metamorphosed the Yandaminta Quartzite, Tabita Formation, and graded bedded turbiditic sandstones, exposed in the Pingbilly Formation. These formations, first defined Wonnaminta and Kayrunnera areas east and west by Warris (1967), are confined to a syncline on the of Koonenberry Mountain (Figure 1). Constituent western flank of Mount Arrowsmith and represent post formations (defined by Mills, in Greenfield et al. 2010) Delamerian Orogeny rock units that correlate with the include the Wonnaminta Formation, the Nundora Mutawintji Group exposed at the northern end of the Formation to the west (which may be the oldest unit), Koonenberry Belt. the Bunker Creek Formation to the east, and the Depot TheYandaminta Quartzite is predominantly Glen Formation at the northwestern extremity of the quartzite, generally massive but locally cross-bedded, Koonenberry Belt. All these units are fault-bounded, and and grading to conglomerate at its northern limit of they may well be equivalent in part. The monotonous outcrop. Thickness of the formation varies along strike lithology and lack of marker units prevent an accurate from 200 m to 65 m (Warris 1967), possibly due to measurement of the thicknesses of individual faulting along the lower boundary with the Wyarra formations or the group as a whole. Biostratigraphic Shale. Grey–green shales containing carbonate nodules evidence for the age of these Teltawongee Group rocks are common in the middle to upper part of the unit but is lacking. The Depot Glen Formation contains a felsic are generally covered by quartzite scree. A conodont tuff member dated (U–Pb SHRIMP) at 504.5.1 ± 2.6 Ma fauna obtained from the carbonate nodules (Zhen et al. (Black 2006). On the Kayrunnera 1:100 000 geological 2003b) is of late Early Ordovician age (Oepikodus evae sheet, the Bunker Creek Formation has been intruded conodont Zone). by the Williams Peak Granite (defined by Gilmore,

10 September 2011 in Greenfield et al. 2010), which has a U–Pb SHRIMP Conglomerate; Hummock Formation; Morden zircon age of 515.1 ± 2.7 Ma (Black 2007), and so must Formation) lying directly above the Delamerian be pre-Ordian. unconformity pass upwards into deeper-water ThePonto Group of Mills (in Greenfield et al. sandstones and siltstones (Cupala Creek Formation; 2010), at least 5500 m thick, is mainly composed of Boshy and Watties Bore formations) containing Late variably metamorphosed, fine-grained marine clastic Cambrian to earliest Ordovician trilobites. Carbonate rocks (phyllites, schists, fine-grained sandstones beds and lenses are rare until higher in the succession and mudstones) of probable deep water origin. The (Funeral Creek and Kandie Tank limestones; Wheeney group is subdivided into eight formations (defined or Creek Formation). The Kayrunnera Group broadly redefined in Greenfield et al. 2010) that outcrop along correlates in age with the lower to middle part of much of the Koonenberry Belt on the western side of the shallow marine Mutawintji Group, and in part the Koonenberry Fault. From oldest to youngest, they represents a deeper water facies equivalent of the latter. are the Weinteriga Creek Formation (predominantly The oldest unit identified in the Kayrunnera Group, sandy phyllites in the Grasmere 1:100 000 sheet area), the Williams Creek Conglomerate (defined by Grasmere Formation (phyllites with feldspathic tuff Greenfield, in Greenfield et al. 2010) was previously horizons, quartz–magnetite rocks and mafic units), recognised as an unnamed basal conglomeratic facies Noonthorangee Formation (similar to the underlying of the Cupala Creek Formation by Powell et al. (1982). It Grasmere Formation but lacking its strong magnetic is a coarse polymictic conglomerate, up to 100 m thick, character), Koonenberry Formation (green phyllites with well-rounded clasts of sandstone, mafic volcanics with minor basaltic flows, tuffaceous and quartz– and chert, assumed by Powell et al. (1982) to be derived magnetite rocks, mostly confined to the Cobham Lake from the underlying Copper Mine Range Formation. 1:100 000 sheet area) and Yandenberry Formation The Cupala Creek Formation of Powell et al. (1982) (first defined by Mills, in Greenfield et al. 2010). The was redefined and subdivided by Greenfield (in Cannela Formation, thought to be correlative with Greenfield et al. 2010) into a lower quartzose sandstone- the Noonthorangee Formation, is confined to the to quartzite-dominated part named the Hummock Gorge Inlier on Mount Shannon and Mount Poole Formation, that is overlain conformably by the siltstone- stations at the northern extremity of the Koonenberry dominated Cupala Creek Formation. The Hummock Belt. The Baroorangee Creek Formation, which is Formation varies in thickness from about 530 m in mostly exposed on Cymbric Vale station, is more the Cupala Creek structural outlier, to over 1000 m in metamorphosed (attaining lower amphibolite grade the Nuntherungie area. Thickness of the Cupala Creek according to Mills, in Greenfield et al. 2010) than other Formation is also highly variable; the type section in the Ponto Group formations to the east, and relationships Cupala Creek area is only 390 m thick, whereas in the between rocks in these two areas are unclear. No Nuntherungie structural outlier the estimated thickness fossils have been found in rocks of the Ponto Group. is approximately 4000 m. The sole fossil identified in Three feldspathic tuff horizons in the Noonthorangee the Hummock Formation is the brachiopod Billingsella, Formation have been dated using SHRIMP zircon apparently the same species as occurs in the Cupala U–Pb analysis at 508.6 ± 3.2 Ma, 511.7 ± 3.5 Ma and Creek Formation (Powell et al. 1982). Trilobites and 512.0 ± 3.1 Ma (Black 2005), spanning the latest Early other fossils (monoplacophoran molluscs, brachiopods) Cambrian to earliest Late Cambrian interval. Extrusive from siltstones and sandstones, with minor fossiliferous rocks that are concentrated in the middle of the Ponto calcareous and dolomitic lenses, in the lower part of the Group, including E-MORB (enriched mid-ocean ridge redefined Cupala Creek Formation establish the age of basalts) tholeiitic pillow lavas, basaltic flows and basic these strata as Idamean (early Late Cambrian) (Jell, in tuffs, have been defined by Vickery and Greenfield (in Powell et al. 1982). Greenfield et al. 2010) as the Bittles Tank Volcanics. Southeast of Koonenberry Mountain, the Kayrunnera Also included in this unit are basaltic to doleritic sills Group was divided into three formations defined by which intrude the Ponto, Teltawongee and Grey Range Webby et al. (1988). The Morden Formation at the groups. One intrusive rock, dated using SHRIMP zircon base of the group consists of unfossiliferous medium- analysis at 496.3 ± 3.1 Ma (Black 2005), suggests that grained quartzite 1–6 m thick but regionally extensive the igneous activity responsible for the Bittles Tank over 16 km between Morden Creek and Kayrunnera Volcanics may have continued after the main pulses of homestead. This unit is conformably overlain by the Delamerian Orogeny; alternatively, the dated sills are the Boshy Formation, about 94 m thick in the type much younger than the volcanic unit to which they have section located approximately 18 km southeast of been assigned. Koonenberry Mountain (Webby et al. 1988). Dominant Rocks of the Kayrunnera Group (Greenfield, lithologies in this unit include interbedded fine-grained Mills & Percival, in Greenfield et al. 2010) occupy sandstones and siltstones, with minor calcarenites and several small basins east of the Koonenberry Fault. limestone lenses. Trilobites of latest ‘Middle’ Cambrian Basal conglomerates or quartzites (Williams Creek (Mindyallan) age were described by Wang et al. (1989)

Quarterly Notes 11 from two stratigraphic levels, the lower about one- Quartzite and Tabita Formation at Mount Arrowsmith, third up from the base of the formation, and the other i.e. of lower Reutterodus andinus and equivalent in the upper third of the unit. Although some minor Oepikodus evae Zone age, corresponding to the late differences in faunal composition are apparent between Bendigonian to early Castlemainian interval (Figure 4). the two levels, all species most likely belong to the late Bilpa–Comarto area, Scropes Range and Dolo Hills Mindyallan Glyptagnostus stolidotus Zone, possibly near its lower boundary with the underlying Acmarhachis (Figure 5, column 4) quasivespa Zone (Wang et al. 1989). The basal unit of the Mutawintji Group in the Scropes Range area, largely exposed south of the Barrier TheWatties Bore Formation conformably overlies Highway, is the Bilpa Conglomerate. Packham (1968a) the Boshy Formation, and consists of approximately and Webby (1983) first noted this unit, which was 2000 m of shales and siltstones, with some well-bedded subsequently informally named by Pahl and Sikorska and laminated impure shaly limestones and minor (2004) and formally described by Greenfield and limestone breccia lenses, interpreted to represent Percival (in Greenfield et al. 2010). It is a very poorly channel deposits by Webby et al. (1988). Trilobites, sorted, pebble to boulder polymictic conglomerate with described by Webby et al. (1988), are present at two levels rounded to angular clasts and a carbonate-rich cement. (separated by only about 100 m) close to the top of the At the base of the unit, clasts include mafic volcanic formation, one of latest Cambrian age with the more rock (very common), phyllite, psammite, vein quartz, diverse assemblage of 10 species, and the other of early gabbro, and felsic tuff, possibly derived from the locally Tremadoc (basal Ordovician) age characterised by a new underlying Teltawongee and Ponto groups. Higher species of Hysterolenus. This suggests correlation with in the sequence, quartz-veined rhyolite, plagioclase- the shallow-water facies equivalent Bynguano Quartzite phyric andesite, garnet-bearing felsic granitoid, gabbro, of the Mutawintji Group, which also spans the Cambro- psammite, limestone and metapelite pebbles and Ordovician boundary. sub-angular boulders up to 1 m across are present. On Morden Station, the Funeral Creek Limestone Although lacking fossils indicative of its depositional (defined by Greenfield & Percival, in Greenfield age, the conglomerate has yielded rare mudstone et al. 2010) — an isolated and apparently overturned pebbles containing the Early Cambrian protolenid allochthonous pod of fossiliferous limestone 20–30 m trilobite Bergeroniellus (identified by J.H. Shergold; thick — yielded conodonts of the Late Cambrian K.J. Mills, pers. comm. 1996). According to Palmer Eoconodontus and Cordylodus proavus zones (Zhen & and Rowell (1995), Bergeroniellus is closely related to Percival 2006). This limestone has a distinctive brecciated Hsuaspis, which was described from the upper Cymbric appearance, composed of subrounded to tabular clasts of Vale Formation by Jago et al. (1997) and subsequently carbonate up to 20 cm long, suggesting deposition in an synonymised with Estaingia by Paterson (2005). The agitated shallow water marine environment. similarity in appearance of these trilobite genera TheKandie Tank Limestone, first described by suggests that the fragmentary remains identified as Pogson and Scheibner (1971) with minor redefinition Bergeroniellus could well represent Estaingia, and that by Greenfield (in Greenfield et al. 2010), is another these mudstone pebbles may have been derived from isolated limestone pod up to 50 m thick, located exposed parts of the Cymbric Vale Formation, uplifted east of the northern end of the Coturaundee Range. and eroded during the Delamerian Orogeny. Undescribed species of Cordylodus in this limestone Conformably overlying the Bilpa Conglomerate appear to indicate an age also very close to the Cambro- in the Scropes Range is the Nuchea Conglomerate Ordovician boundary (B.D. Webby, pers. comm. 1995). (also known from the Mutawintji area: see Figure 5, Thus the Kandie Tank Limestone is slightly younger column 1), which is differentiated by its quartz pebble than the Funeral Creek Limestone, but appears to be monomict facies from the polymict Bilpa Conglomerate contemporaneous with unnamed limestone exposed (Pahl & Sikorska 2004). Thickness of the Nuchea near Anderson’s Tank on Devon Station in the Dolo Conglomerate in the Scropes Range is 50–109 m. Hills to the south (Zhen & Percival 2006). TheScropes Range Formation, redefined by Outcrop of the Wheeney Creek Formation (defined Greenfield and Percival (in Greenfield et al. 2010) with by Greenfield, in Greenfield et al. 2010), is mainly spelling corrected from earlier usage of ‘Scopes Range confined between the Koonenberry Fault on the Beds’, is the uppermost unit of the Mutawintji Group west, and the Big Wallaby Tank Fault to the east. The in the southern Koonenberry Belt. The formation, formation is up to 500 m thick and is characterised which consists of white to maroon cross-bedded by discontinuous lenses of polymictic conglomerate, quartz sandstone of fluviatile origin in the southwest, quartzite, interbedded psammite and slate, fossiliferous grading to shallow marine quartz sandstones to the limestone, intraclast limestone and dolomite. Conodonts northeast, is 1385–2012 m thick. Only trace fossils from limestone at Koonenberry Gap (Zhen et al. 2001, (Webby 1983) and lingulate brachiopods (Percival & 2003b) are identical to assemblages in the Yandaminta Engelbretsen 2007) have been documented from the

12 September 2011 Scropes Range Formation, which is believed to correlate extrusion coeval with the Easter Monday Formation with the Nootumbulla Sandstone, Bynguano Quartzite (Warratta Group) in the Late Cambrian. and Rowena Formation of the Bynguano Range and Mutawintji area. Thomson Orogen Warratta, Tibooburra and Mount Poole inliers Cambrian and Ordovician rocks are inferred to occupy (Figure 5, column 5) a large area of the very poorly exposed Thomson Orogen The Warratta Inlier west of Milparinka, and Tibooburra in northwestern New South Wales (Glen et al. 2010), Inlier in the immediate vicinity of Tibooburra, include but data on precise ages and correlations to units in the rocks interpreted to have been deposited following the adjacent Lachlan and Delamerian orogens are scarce. Delamerian Orogeny (although underlying basement Rocks of the Warratta and Tibooburra inliers and the is not exposed, and these inliers may possibly represent Yancannia Range, discussed above, may belong to the parts of the Thomson Orogen). These strata constitute Thomson Orogen. Unnamed quartz-rich turbiditic the newly defined Warratta Group (Greenfield, in rocks of probable Late Ordovician age (determined Greenfield et al. 2010), incorporating the Easter Monday from poorly preserved graptolites) were intersected Formation (Vickery, in Greenfield et al. 2010), Jeffreys in Louth DH L5 drillhole. This facies contrasts with Flat Formation (Greenfield, in Greenfield et al. 2010), contemporaneous black shales of the Warbisco Group and Yancannia Formation (Mills, in Greenfield et al. that are widespread in the Albury–Bega Terrane of 2010). These units are individually named because of the Lachlan Orogen (see below). Upper Ordovician their spatial separation (Jeffreys Flat Formation confined sediments are unknown in the Hermidale Terrane and to the Warratta Inlier; Easter Monday Formation from the Delamerian Orogen. represented only in the Tibooburra Inlier; Yancannia Formation restricted to the base of the Yancannia Range), but it is likely they were deposited contemporaneously Lachlan Orogen — continental (possibly in one connected depocentre) and therefore margin terranes probably represent facies equivalents. The lower part Coarse- to fine-grained sandstones and siltstones of of the Jeffreys Flat Formation, a pyritic siltstone– turbiditic origin, with associated pelagic sediments of mudstone deposited in deep water, is overlain by impure latest Cambrian to Middle Ordovician age, constitute limestone, diamictite (including boulders of felsic tuff a large part of the Lachlan Orogen. They include the possibly derived from the Depot Glen Formation of Castlemaine Supergroup in Victoria, the Adaminaby the Teltawongee Group), rippled sandstone beds and Group in southeastern New South Wales and eastern clean quartzite, that imply shallowing to a marine Victoria (including the equivalent Pinnak Sandstone shelfal depositional environment. Branching to sinuous of central and southeastern Victoria), the Abercrombie trace fossils from siltstone–sandstone interbeds of the Formation on the Goulburn 1: 250 000 geological lower Jeffreys Flat Formation in Gum Vale Gorge were map and adjacent areas, the Wagga Group in central inferred by Webby (1984) to be of possible Cambrian southern New South Wales and the Girilambone Group to Early Ordovician age. The Yancannia Formation in the central-northern part of the state. Although is mostly mudstone or siltstone of low metamorphic initially regarded as superficially similar throughout grade. The Easter Monday Formation is predominantly their stratigraphy (Coney 1992), these turbiditic and metasandstone, metamudstone and phyllite of probable associated sedimentary packages can now be subdivided turbiditic origin (interpreted from graded bedding and into five biostratigraphic zones of Early and late Bouma sequences) with rare diamictite. A laminated Middle Ordovician age using conodonts identified in felsic tuff from the Easter Monday Formation has a thin sections of cherts (Plate 1) that occur in horizons SHRIMP II U–Pb zircon age of 497.2 ± 2.6 Ma using the interbedded with the sandstone-dominated units Temora standard (Black 2006, 2007), comparable to the (Percival 2006a; Percival & Zhen 2007). Correlation of age of an intrusion in the Bittles Tank Volcanics of the this conodont-based biostratigraphy (following on from Koonenberry area. pioneering studies by Stewart 1988, Stewart & Fergusson The Evelyn Creek volcanics (informally named by 1988, and VandenBerg & Stewart 1992 in Victoria and Greenfield, in Greenfield et al. 2010) is an ungrouped unit southeastern NSW) with the detailed graptolite zonation comprising mafic igneous rocks of alkaline affinity that of the Castlemaine Group, has permitted recognition are restricted to flows, sills and dykes in the Tibooburra of different terranes of Ordovician age, as well as and Mount Poole inliers. These rocks imply protracted lithostratigraphic distinctions throughout the Lachlan intraplate magmatism in three stages throughout Orogen (Glen et al. 2009). Upper Ordovician rocks of the the ‘Middle’ to Late Cambrian in the Tibooburra– Lachlan Orogen lack cherts and (except for the Sunbury Milparinka area: an initial episode coeval with Group in Victoria) are typically rich in black shale that deposition of the Depot Glen Formation (Teltawongee contains graptolites; these rocks are included in the Group), followed by intrusion into this unit, and finally Bendoc Group throughout the Albury–Bega Terrane.

Quarterly Notes 13 Albury–Bega Terrane (Figure 5, columns 6–10) been complicated by imbrication of black shale, chert and turbiditic sandstone from various parts of the – As defined by Glen et al. (2009), the Albury Bega sequence (Glen & VandenBerg 1987; Glen et al. 1990). Terrane is an amalgamation of the Albury and The turbidite sequence is punctuated by 2–3 prominent Bega terranes (Glen 2005) now merged as a result of and regionally extensive chert-rich horizons of which additional biostratigraphic age dating. The stratigraphy the lowermost is more sporadic, consisting of thinly of the monotonous and extensive turbiditic sandstone bedded cherts, sometimes interlayered with turbiditic sequence (Adaminaby and Wagga groups) has been sandstones. The cherts contain conodont faunas ranging compiled from widespread observations of incomplete in age from Late Cambrian (indicated by paraconodonts sections. An understanding of the succession has including Furnishina) to Early Ordovician, dominated

Plate 1. A selection of biostratigraphically significant Ordovician conodonts that occur in cherts of the Lachlan Orogen in NSW. A. Oepikodus evae M element, Mummel Chert Member of Abercrombie Formation; locality AJJ 0015.02, Taralga 1:100 000 sheet. B. Oepikodus evae Sb element, Narrawa Formation; locality SJT 0270.01, Sussex 1:100 000 sheet. C. Oepikodus evae Sb element, Mummel Chert Member of Abercrombie Formation; locality AJJ 0015.02, Taralga 1:100 000 sheet. D. Oepikodus evae Sc element, Mummel Chert Member of Abercrombie Formation; locality AJJ 0015.02, Taralga 1:100 000 sheet. E. Oepikodus evae Sc element, Narrawa Formation; locality SJT 0270.01, Sussex 1:100 000 sheet. F. Oepikodus evae Sc element, Mummel Chert Member of Abercrombie Formation; locality AJJ 0015.02, Taralga 1:100 000 sheet. G. Paracordylodus gracilis S element, Narrawa Formation; locality SJT 0171.01, Sussex 1:100 000 sheet. H. Paracordylodus gracilis Sa? element, Mummel Chert Member of Abercrombie Formation; locality MMS 0104.01, Taralga 1:100 000 sheet. I. Pygodus serra Pa element, Nattery Chert Member of Abercrombie Formation; locality GLS 202, Goulburn 1:100 000 sheet. J. Periodon aculeatus Sa element, Nattery Chert Member of Abercrombie Formation; locality GLS 202, Goulburn 1:100 000 sheet. K. Periodon flabellum Pb element, Mummel Chert Member of Abercrombie Formation; locality MMS 0104.01, Taralga 1:100 000 sheet. L. Periodon flabellum Sc element, Mummel Chert Member of Abercrombie Formation; locality MMS 0104.01, Taralga 1:100 000 sheet. M. Periodon flabellum Sd element, Mummel Chert Member of Abercrombie Formation; locality ODT 0091.01, Taralga 1:100 000 sheet. N. Spinodus spinatus Sc? element, from unnamed chert (possibly Peach Tree Chert Member) in upper Abercrombie Formation; locality LJS 0179.01, Taralga 1:100 000 sheet. O. Paroistodus horridus Sb element, from unnamed chert in upper Abercrombie Formation; locality ODT 0543.01, Taralga 1:100 000 sheet. P. Periodon aculeatus conjoined (left to right) S, Pb? and possible M elements, Nattery Chert Member of Abercrombie Formation; locality LJS 331, Goulburn 1:100 000 sheet. Bar scales represent 0.1 mm. Chert sections are approximately 50 microns thick. (Photographer: D. Barnes)

14 September 2011 by Paracordylodus gracilis and Oepikodus evae. The sandstones of variable thickness. Sandstone/slate ratios Upper Cambrian cherts are correlatives in part of the and sandstone bed thicknesses vary and these have been Goldie Chert and Howqua Chert in Victoria, which used to locally discriminate lithofacies: Fenton et al. contain species of the conodont Cordylodus of latest (1982) inferred four lithofacies in the Mallacoota area of Cambrian (Datsonian) age (Stewart & Fergusson eastern Victoria, and Powell (1983) identified proximal 1988, Kakuwa & Webb 2010). However, in Lower and distal facies from outcrops on the NSW south coast. Ordovician rocks in Victoria, such cherts are generally Others working in the same region (e.g. Glen 1994) absent, being replaced by a dark grey to black siliceous discriminated thick-bedded (>1 m), medium-bedded shale or siltstone containing graptolites Tetragraptus (>20 cm) and thin bedded (<20 cm) sandstone facies. approximatus and Pendeograptus fruticosus (inter alia) Sandstone beds in thick-bedded facies are generally (VandenBerg & Stewart 1992). The upper horizon parallel-sided, contain Bouma divisions A and B, and comprises bedded chert up to 100 m thick that contains only rarely display sole markings. Sandstone beds in late Darriwilian (Pygodus serra Zone) conodonts. thin-bedded facies are dominated by divisions B and Graptolites are comparatively rare in turbidite C, with the latter containing cross-laminations, with sequences of Early and Middle Ordovician age in lesser convolute laminations and flame structures. The NSW. A fauna including the long-ranging Tetragraptus grain size of sandstone beds in the Adaminaby Group quadribrachiatus, found in highly cleaved slates of is mostly medium or finer, and conglomerates are andalusite grade in the Narrandera district by Keble and conspicuously absent. Mud-rich facies dominate in some Macpherson (1941), suggests a generalised Darriwilian areas (Glen & Wyborn 1997). age for these rocks. Jenkins (1982) also recognised mid- The prominent and widespread upper chert- – Darriwilian (Da2 3) graptolites in the Adaminaby dominated package is called the Numeralla Chert, first Group east of Braidwood. recognised in the Cooma region (Glen 1994; Glen & Above the younger chert horizon, turbidite Lewis 1994). The Numeralla Chert conformably overlies sedimentation decreases through a transitional, the lower, turbiditic parts of the Adaminaby Group with commonly laminated sequence of siltstone, black shale, a gradational lower contact and includes one or more and sandstone with thin cross-laminated quartzitic mappable chert-dominated units up to 100 m thick that silt layers (Glen & VandenBerg 1987; VandenBerg consist of beds of parallel-sided ribbon chert up to 50 cm et al. 1991; VandenBerg et al. 2000; Glen et al. 2009). thick, interbedded with cleaved slate and siltstone and Within this transitional package, the characteristically rare sandstone beds. Chert beds contain recrystallised micaceous, feldspathic and lithic, quartz-rich sandstones radiolarian tests as well as conodonts that were of the lower turbidite sequences become more mature. originally ascribed a Darriwilian–Gisbornian age (e.g. Subsequently, black shales of the Bendoc Group Glen 1994) but are now known to be of late Darriwilian (Warbisco Shale) dominate from the earliest Late (late Da3 to latest Da4) age (Percival 2006a; Percival & Ordovician. As the upper part of the sequence has been Zhen 2007). Although an older chert horizon has not most comprehensively described in eastern Victoria, been recognised in the Cooma–Monaro area, Oepikodus some discussion is included below with correlations evae and Paracordylodus gracilis have been reported in between that region and southern NSW. chert layers within undifferentiated Adaminaby Group Cooma–Monaro region and eastern Victoria on the NSW far south coast (Eden area) by Stewart and (Figure 5, column 6) Glen (1991). In eastern Victoria, both chert horizons In the Cooma–Bega–Mallacoota region, turbiditic were included in the Pinnak Sandstone (VandenBerg sandstones and cherts of Early–Middle Ordovician age et al. 1991) with some Pygodus serra-bearing cherts are attributed to the Adaminaby Group (first named (correlatives of the upper horizon) also reported in the by Fairbridge 1953, according to Glen 1994; current Sunlight Creek Formation (Willman et al. 1999, p. 103, definition dates from Glen et al. 1990). Undifferentiated after VandenBerg & Stewart 1992). turbiditic rocks of the Adaminaby Group in the Overlying the Numeralla Chert in the Cooma– Monaro region of southern NSW (Glen 1994) are Monaro region is a thin succession of interbedded equivalent to the Pinnak Sandstone of eastern Victoria sandstone, siltstone and slate forming the 300–400 m (VandenBerg & Stewart 1992; VandenBerg et al. 2000). thick Chakola Formation (Glen 1994). The top 50– No stratigraphic base to the turbidite package has been 100 m of that unit constitutes the Glen Fergus Member found due to the presence of internal imbrication and (Glen 1994; Glen & Lewis 1994), distinguished by very deformation (Glen 1995), although Late Cambrian thinly bedded mudstones and slates interbedded with conodonts are known from coastal outcrops in the thin sandstones containing broad, low-amplitude cross Batemans Bay area previously assigned to the Narooma laminations. The sandstones within this part of the Terrane (Glen et al. 2004) but now interpreted as part sequence are typically more mature than those below of the Albury–Bega Terrane (Kakuwa & Webb 2010). the Numeralla Chert horizon, with large quartzites Turbiditic sequences comprise green to grey–green lenses, although micaceous and feldspathic sandstones laminated slates and siltstones interbedded with are also conspicuous.

Quarterly Notes 15 In far south-eastern NSW and north-eastern Victoria, defined by Glen 1994) is reported to gradationally overlie rocks of the Adaminaby Group are conformably the Warbisco Shale and hence may be a correlative of the overlain by the Upper Ordovician Bendoc Group (Glen Akuna Mudstone (Glen 1994). However, the occurrence et al. 1990), which is defined primarily by conspicuous of monograptid graptolites of late Llandovery age in the and regionally extensive graptolitic black shales with Gungoandra Siltstone on the Michelago 1:100 000 map relatively minor development of sandstone. In some (Sherwin, in Richardson 1979) suggests that further areas, such as east Gippsland (eastern Victoria) and west investigation of this unit is necessary. of the Cooma Metamorphic Complex (southern NSW), the basal unit of the Bendoc Group is the Sunlight Canberra–Queanbeyan region (Figure 5, column 7) Creek Formation (formerly Sunlight Creek Member Around Canberra in the ACT and eastwards to of the Warbisco Shale; VandenBerg et al. 1991 after Queanbeyan in NSW, the Pittman Formation and Glen et al. 1990) of Gisbornian age that consists of well- the Acton Shale represent late Middle Ordovician and laminated black shales bearing Nemagraptus gracilis, Late Ordovician rocks (both units named and defined siltstones and thin beds of sandstone. More substantial by Öpik 1954, 1958). Öpik (1958) noted the presence of incursions of sandstone may also form part of this unit sandstone, shale and minor radiolarian chert beds (up and its relationship to the Chakola Formation (here left to 6 m in thickness) in the Pittman Formation. These ungrouped) requires further study. lithologies, together with the occurrence of graptolite The transition to Warbisco Shale (VandenBerg et al. faunas of two different ages listed by Öpik (1958) — 1991) by cessation of sandstone/quartzite/silt deposition, one of probable late Darriwilian age and the other (about 30 m below the Acton Shale) with Gisbornian took place within the Gisbornian as indicated by the affinities — suggest that the Pittman Formation likely presence of Climacograptus bicornis in the lower part of correlates with the uppermost part of the Adaminaby this formation (Percival & Sherwin 2005). Graptolitic Group. Additional evidence is provided by conodonts, black shales and siltstones of the Bendoc Group typically including Pygodus serra and Periodon aculeatus of latest occur as narrow, generally linear fault-bound belts Darriwilian age, that Nicoll (1980) documented from with a stratigraphic thickness generally less than 400 m shale underlying a thin chert bed within the Pittman (VandenBerg 1981; VandenBerg et al. 1991). Accurate Formation. Graptolites identified by Öpik (1958) measurements are rarely possible since some slices from the Acton Shale, of Gisbornian, Eastonian and have been internally imbricated or extended, illustrated possibly earliest Bolindian age (the latter represented locally by repetition or excision of graptolite zones by Pleurograptus linearis), support its correlation with (VandenBerg 1981; Glen & VandenBerg 1987). Typically, the Warbisco Shale of the Bendoc Group (Glen, Dawson older parts of the Warbisco Shale are more siliceous, & Colquhoun 2007). Although the Acton Shale has for locally becoming a black chert, whereas upper parts are many years been considered a member of the Pittman fissile parallel to bedding. Weathered black shales in the Formation (cf. Strusz & Henderson 1971; Abel 1991), our Michelago area south of Canberra (Richardson 1979), preferred correlation with the Warbisco Shale implies previously known informally as the ‘Foxlow beds’ but that any sandstone-dominated sequence overlying the now referred to the Warbisco Shale (Glen, Dawson & black shale is either a latest Ordovician New Country Colquhoun 2007), contain a diverse Late Ordovician Sandstone equivalent, or is Early Silurian. (Ea2–3) graptolite fauna (Williamson & Rickards 2006). Sporadically intercalated within the Warbisco Shale Above the Warbisco Shale, the base of of the turbiditic and its correlatives are very clean sandstones, the

New Country Sandstone (VandenBerg et al. 1998; most prominent of which is the Tidbinbilla Quartzite,

VandenBerg et al. 2004) is defined by the introduction a 300 m-thick lenticular unit that outcrops in the of medium- to fine-grained, pale to dark grey quartz Brindabella Ranges on the western side of the ACT. sandstone with common detrital muscovite, interbedded The unit was originally assigned by Owen and Wyborn with subordinate black mudstone. The distribution (1979) to the Silurian but later reassessed as Upper of the unit is sporadic and it is typically viewed as a Ordovician (VandenBerg & Stewart 1992). Although local transition to Yalmy Group or Cobbannah Group fossils are absent from the quartzitic sandstones, we sandstones into the Early Silurian. In east Gippsland concur with Owen and Wyborn’s original supposition (Victoria) the New Country Sandstone is laterally of a Silurian age, based on lithological similarity equivalent to, or overlain by, the Akuna Mudstone to sandstones of the Yalmy Group. The Tidbinbilla (VandenBerg et al. 1991) of latest Ordovician (late Quartzite was equated by Abel et al. (2008) with the Bolindian) age (VandenBerg et al. 1991), a unit that Lower Silurian Black Mountain Sandstone in the extends into far southern New South Wales just north Canberra region. of Delegate (White & Chappell 1989). Further north, in the Cooma 1:100 000 sheet area, a distinctive khaki Goulburn region (Figure 5, column 8) mudrock termed the Gungoandra Siltstone (modified Early–Middle Ordovician turbiditic rocks in the after Richardson 1975: Gungoandra Siltstone Member; Goulburn–Taralga area (between Sydney and Canberra) raised to formation status by Glen et al. 1990, and are referred to as the Abercrombie Formation

16 September 2011 (redefined by Thomas et al., in Thomas et al. in press, graptolites in the upper beds. Thus this unit is incorporating several units previously recognised on substantially similar to the Sunlight Creek Formation of the Taralga 1:100 000 sheet by Scheibner 1973). These VandenBerg et al. (1991). rocks are lithologically identical to the contemporaneous In the southern half of the Goulburn 1:250 000 undifferentiated Adaminaby Group in which they are mapsheet, the Warbisco Shale (see above) is overlain included. Framework grains in sandstone beds are by the Margules Group (Scott et al., in Thomas et al. dominated by plutonic quartz (up to 80%). Feldspar in press) with three constituent formations of possible and lithic fragments are more common low in the latest Ordovician or earliest Silurian age (although Abercrombie Formation beneath the oldest chert beds, palaeontological evidence is lacking). The Dignams characterising the Willigam Sandstone Member Siltstone (Thomas, in Thomas et al. in press), a silty (defined by Thomas & Scott, in Thomas et al. in press) and sandy unit 100–500 m thick that is distinguished as a quartzo-feldspathic sandstone. Stratigraphically by its olive–grey to brown colour, is confined to the higher sandstones are typically fine- to medium-grained Goulburn 1:100 000 mapsheet. Apparent conformable and moderately sorted, occasionally grading to poorly relations between the Warbisco Shale and the Dignams to bimodally sorted coarse- to very coarse-grained Siltstone suggest that the latter is likely equivalent to the sandstone with larger grains up to 3 mm. The main Akuna Mudstone. Possibly laterally equivalent in part, mineral components are rounded to sub-rounded grains and interpreted to conformably overlie the Dignams of quartz, up to 10% detrital feldspar and ~5% detrital Siltstone or the Warbisco Shale elsewhere on the Taralga white mica; metasedimentary lithic fragments are rare. 1:100 000 mapsheet, is the Poidevins Sandstone (Thomas Trace minerals include tourmaline, apatite and zircon. & Simpson, in Thomas et al. in press), consisting of The matrix to these framework grains varies from fine to very coarse-grained quartzose sandstone with – – 15 40%, composed of clay and silt mud sized quartz minor grey–green siltstone, at least 1200 m thick. Of grains. East of Mudgee, similar sandstone is fine- to very comparable thickness is the turbiditic Mundoonen – fine-grained, framework supported (matrix 2 23%) and Sandstone (modified by Sherwin, in Thomas et al. in – consists mainly of quartz (61 93%) displaying strong press, after Mundoonen Series of Sherrard 1939) that undulose extinction, polycrystalline metamorphic and forms characteristic red, brown and orange sandstone polygonal textures, all indicating a metamorphic source, exposures in the Mundoonen Range between Gunning together with albite feldspar (up to 4.6%) (Colquhoun and Yass. The Poidevins Sandstone (and possibly et al. 1999). the Mundoonen Sandstone) may correlate with the Biostratigraphic control is provided by conodonts Lower Silurian Cobbannah or Yalmy groups. Another including Oepikodus evae from the Mummel Chert interpretation (Sherwin & Strusz 2002), which we view Member (defined by Thomas & Scott, in Thomas et al. as less likely, regards the Mundoonen Sandstone as in press) indicative of a late Bendigonian to Chewtonian extending from the Bolindian into the Lower Silurian. age (Percival et al. 2003). A younger chert horizon in the region north of Goulburn, named the Peach Tree Oberon–Rockley region (Figure 5, column 9) Chert Member by Thomas, Pogson and Percival (in Considerable disparity exists in recent interpretations Thomas et al. in press) contains early to mid Darriwilian of the stratigraphy of Ordovician rocks found in conodonts (Percival & Zhen 2007). the Oberon–Rockley region. The oldest unit in this Also in the Goulburn area, thick late Middle area, indicated by presence of an Early Ordovician Ordovician (late Da3–latest Da4) cherts are represented (late Lancefieldian to early Bendigonian) conodont by the Nattery Chert Member of the Abercrombie assemblage dominated by Paracordylodus gracilis, is Formation (the member defined by Thomas & Pogson, the Budhang Chert (Murray & Stewart 2001). This in Thomas et al. in press). This member correlates formation, restricted in outcrop to a single large fault- with the Numeralla Chert in southern NSW. Stewart bounded block, was originally placed in the Macquarie and Fergusson (1995) reported cherts with the same Arc succession as a member of the Triangle Formation, conodont fauna (Pygodus serra) in what they referred to but subsequently was tentatively reassigned to the as Sunlight Creek Formation in the Bungonia area east Adaminaby Group by Percival and Glen (2007). The of Goulburn, though more recent mapping in the region Mozart Chert, also defined by Murray and Stewart (Thomas et al. in press) now recognises these outcrops as (2001) as a member of the Triangle Formation, is Nattery Chert Member. identical in appearance and age (based on the presence Fergusson and Fanning (2002) defined a 300 m-thick, of late Darriwilian conodonts) to the widespread distinctive thin-bedded turbidite sequence in the Numeralla Chert and equivalent facies such as the Shoalhaven Gorge area east of Goulburn as the Nattery Chert Member of the Abercrombie Formation Bumballa Formation. Those rocks consist of cross- on the Goulburn 1:250 000 sheet to the south of Oberon laminated sandstones — some of which have been (Thomas et al. in press), and therefore undoubtedly interpreted as contourites by Jones et al. (1993) — belongs to the Adaminaby Group. Another unit named interbedded with shales that contain late Gisbornian by Murray and Stewart (2001), the Gidyen Volcanic

Quarterly Notes 17 Member, has never been formally defined and appears et al. (1995) cannot be utilised to subdivide the Wagga to represent an admixture of allochthonous debris Group. As now defined by Hendrickx and Colquhoun indistinguishable from the Rockley Volcanics. The (in Colquhoun et al. 2005), the Wagga Group includes latter unit, together with the Triangle Formation, was units cropping out northwest of Condobolin that were previously assigned to the eastern belt of the Macquarie previously included in the Tallebung Group by Trigg Arc (Murray & Stewart 2001; Percival & Glen 2007). (1987) (see Appendix). The Triangle Formation consists of quartz siltstone with Isolated exposures of strata assigned to the Wagga conglomerate, debris flow and olistostromal horizons. Group in the western part of the Forbes 1:250 000 These rocks underlie the Rockley Volcanics, that has geological sheet were named the Clements Formation been assumed to consist entirely of volcaniclastic strata. by Duggan and Scott (in Lyons et al. 2000). Much of However, recent work (Quinn et al. in prep) has shown this formation is turbiditic, with alternating beds of that much of the Rockley Volcanics comprises quartz quartz-rich sandstone grading to siltstone and slate. The siltstones similar to those of the Triangle Formation. sandstones are described by Colquhoun, Hendrickx Conodonts of Gisbornian age were recovered from and Meakin (in Colquhoun et al. 2005) as very fine to cherty siliceous siltstones of the Triangle Formation medium grained, mature to supermature with minor in Triangle Creek (Fowler & Iwata 1995), but closer feldspar (up to 2%). Rare sedimentary and metamorphic inspection reveals that these cherty siltstones are clasts lithic fragments are present, and the matrix contains in younger matrix. less than 2% mica. Colquhoun et al. (2005) recorded The greatly contrasting ages of the Mozart and a 10–25 m-thick lens of clast-supported conglomerate Budhang cherts and their limited extent, the recognition grading to pebbly sandstone, in which clasts 2–15 mm of smaller chert blocks within a siliceous matrix in in diameter are composed of rounded to subrounded Triangle Creek, and the occurrence of Silurian fauna vein quartz, quartz sandstone, black chert, phyllite reported by Pickett (1973) in allochthonous? limestones and rare granite. The conglomerate lens appears to be mapped within the Triangle Formation (cf. Stuart- conformable with surrounding turbiditic sandstone in Smith & Wallace 1997) to the south, combine to suggest the upper part of the Clements Formation and therefore that a complete re-appraisal of the regional geology is likely represents a contemporaneous channel fill facies necessary. One hypothesis is that these Ordovician units (Colquhoun et al. 2005). Also present in the Clements – represent exotic blocks within a younger (Silurian Formation are outcrops of massive quartzite. Devonian) Triangle Formation. Alternatively, the chert Two discontinuous chert horizons provide age horizons may have been structurally imbricated with constraints. The Milby Chert Member, named by arc-related or later sediments and detached completely from the underlying and overlying turbidite strata. Colquhoun, Hendrickx and Meakin (in Colquhoun

These observations, together with a contrasting non- et al. 2005), contains the late Bendigonian to early magnetic and high-K geophysical signature, distinguish Castlemainian conodont Oepikodus evae. This chert this sequence from other parts of the Macquarie Arc occurs in the Tullibigeal area east of Lake Cargelligo

and imply that much of the sedimentary succession in (Percival et al. 2003) and also in the hanging wall of the Oberon–Rockley–Triangle Creek area is of Silurian the west-dipping Gilmore Fault Zone that bounds the or younger age incorporating allochthonous Ordovician Wagga Group to the east. Cherts of early Darriwilian elements. If the presence of autochthonous strata of age, comparable with those recognised in the Ordovician age cannot be confirmed, then the basis for Adaminaby Group, are not presently known from the – considering that part of the Rockley–Gulgong Volcanic Wagga Group. A Pygodus serra Periodon aculeatus Belt south of the Bathurst Batholith to be an easterly belt conodont assemblage (Percival & Zhen 2007) establishes of the Macquarie Arc must be seriously questioned. a latest Darriwilian age for the Doongala Chert Member (named by Colquhoun, Hendrickx & Meakin, Forbes–Condobolin–Cargelligo region in Colquhoun et al. 2005), which is estimated to be less (Figure 5, column 10) than 10 m thick in the Ungarie area. Both cherts are The Lower to Upper Ordovician Wagga Group, relatively poorly exposed and are impersistent laterally, consisting predominantly of quartz-rich turbiditic forming lenticular bodies which pass into sandstone, rocks with very minor cherts, is not well known due to mudstone and shale of the turbiditic succession. Vertical poor outcrop and lack of detailed mapping, except in stratigraphic relationships are similarly obscure. Late the Cargelligo region. Warren et al. (1995) introduced Darriwilian graptolites documented by Sherwin (1983) the term Wagga Group in the Cootamundra area. from isolated outcrops were previously assigned to Hendrickx and Colquhoun (in Colquhoun et al. 2005, the Tallebung Group at The Meadows Tank, 70 km p. 19) noted that sequence 1 of Warren et al. (1995) southwest of Cobar (Barnato 1:250 000 sheet) and most likely represents a fault-bounded slice of Bendoc Illewong near Mt Tallebung (northwest of Condobolin), Group (a contention supported by the presence of Late but now inferred (by Colquhoun, Hendrickx & Meakin, Ordovician graptolites in black shales), and thus it in Colquhoun et al. 2005, p. 31) to belong to the appears that the informal units recognised by Warren Clements Formation.

18 September 2011 In the eastern part of the Cargelligo 1:250 000 map The most recent revision of the Girilambone Group sheet, the most extensive unit of the Upper Ordovician (Trigg & Burton, in Burton et al. in press) incorporates Bendoc Group is the Currawalla Shale (formally three formations and two members recognised in the defined by Colquhoun & Hendrickx, in Colquhoun et al. Sussex–Byrock region northeast of Cobar. The Lower 2005), which occurs at or near the tops of thrust sheets Ordovician Narrama Formation (new name, defined and attains a thickness of ~100–200 m (not allowing by Burton et al. in press) consists of thick to thin bedded for internal thrust imbrication). These black shales quartz-rich turbiditic sandstone grading to siltstone, (equivalent to the Warbisco Shale) contain graptolites interbedded with thin chert horizons that contain the ranging in age from Gisbornian to early Bolindian index conodonts Paracordylodus gracilis (spanning the (Bo1) age (Colquhoun & Hendrickx, in Colquhoun late Lancefieldian to latest Chewtonian interval), and et al. 2005). The Currawalla Shale in part interfingers Oepikodus evae, which ranges from late Bendigonian with, and is overlain by, a regionally extensive ~800 m to early Castlemainian in age (Percival 2006b, 2007a). thick quartz-rich sandstone-dominated unit named the Enclosed within the turbidite sequence of the Narrama Willandra Sandstone by Hendrickx and Colquhoun (in Formation at Dijou Mountain and Bald Hills are Colquhoun et al. 2005). Compared with sandstone of the basaltic volcanics of oceanic intraplate affinity. These older Clements Formation, the Willandra Sandstone is include the 45 m-thick Kaiwilta Member (defined by less mature and had a more diverse provenance, derived Trigg, in Burton et al. in press), which typically has a from a predominantly metamorphic/granitic source basal basaltic/basic volcanic horizon overlain by lithic with possible volcanic input. According to Hendrickx quartz sandstone and minor siltstone. The top of the and Colquhoun (in Colquhoun et al. 2005), quartz-rich unit is marked by a 1–3 m thick, laterally extensive sandstone which makes up the bulk of this formation horizon of thinly bedded chert. The Kaiwilta Member is is white to pale grey in colour, poorly to moderately directly overlain by the Mount Dijou Volcanic Member sorted with subangular to rounded quartz and lithic (described in detail by Trigg & Burton, in Burton grains, the latter including chert, mudstone and very et al. in press, after Brunker 1968) which includes fine sandstone. In contrast, the characteristic black amygdaloidal pillow basaltic and trachytic lavas with sandstone that is distributed throughout the Willandra inter-pillow chert that contains Oepikodus evae. Felton Sandstone is composed almost entirely of poorly sorted (1981) also recorded the presence of mafic volcanics quartz grains of two main size groupings: 0.5 mm (altered vesicular basalt, in one place associated with diameter in the matrix, surrounding larger (1–2 mm) a small patch of limestone now converted to sheared grains. The black colour appears to be due to very fine marble) apparently interbedded within the Girilambone opaque material in the matrix. Another distinctive Group on the Canbelego 1:100 000 sheet area. facies (though relatively uncommon) in the Willandra TheBallast Formation was first termed the Ballast Sandstone is gritty lithic sandstone of granule to Series by Andrews (1913); subsequently it has been conglomeratic grainsize; constituent grains include clear variously called the Ballast Chert, Beds, Group and black quartz, inferred to be volcanic in nature, white Formation (the latter first used by Iwata et al. 1995). vein quartz, together with lithic components including Burton and Trigg (in Burton et al. in press) provide the schist, chert and mudstone. most detailed description of the Ballast Formation to Black shale beds within the Willandra Sandstone date. It consists of interbedded turbiditic sandstone- contain a diverse late Eastonian to early Bolindian dominated beds grading to siltstone and chert, as well as (Bo1–Bo2?) graptolite fauna, similar in age to that at thick persistent packages of ribbon chert tens of metres the top of the locally underlying Currawalla Shale. thick. Correlatives of the latter include the Whinfell Discontinuity of outcrop prevents placement of these Chert Member (Felton 1981) in the Canbelego area, and fossiliferous levels in accurate stratigraphic relationship Alandoon Chert on the Bobadah 1:100 000 map sheet to the sandstone forming much of the Willandra (Pogson 1991). Very small outcrops of basaltic and other Sandstone, and as the top of the unit is not exposed, the mafic rocks are present within the Ballast Formation. age of the upper beds is uncertain. Burton et al. (in press) also recognised a facies variant of the Ballast Formation, which they have defined as the Hermidale Terrane Lang Formation (although our preference is to include this unit as part of the Ballast Formation). Criteria Sussex–Byrock region (Figure 5, column 11) used to distinguish the two units include a greater TheGirilambone Group was initially identified by predominance of sandstone in the Lang Formation Andrews (1915) as the Girilambone Series, although and lesser proportion of chert compared with the this excluded the Ballast Beds (now a constituent Ballast Formation. Rare, very weathered volcanics are formation of the Girilambone Group). First usage known from two outcrops and a drillhole intersection of Girilambone Group in its current context was by in the Lang Formation. The formations were deposited Russell and Lewis (1965). For a historical overview of contemporaneously; cherts from both yield conodonts the nomenclatural history of the unit, see Pogson (1991). including Pygodus serra and Periodon aculeatus,

Quarterly Notes 19 indicative of a late Darriwilian (upper Da3 to top Da4) & R.A. Glen unpublished data cited in Lyons & Wallace age (Stewart & Glen 1986; Iwata et al. 1995; Percival & 1999). The postulated position of these chert bands in Zhen 2007). the upper Kirribilli Formation was taken by several authors (Raymond & Wallace, in Lyons et al. 2000; Condobolin–West Wyalong Lyons & Percival 2002; Meffre et al. 2007) to support The southernmost extent of Girilambone Group an Ordovician age for the Kirribilli Formation, but the rocks terminates against the Cowal Igneous Complex contiguity of these sediments with the cherts and their near West Wyalong. Just north of Condobolin, the provenance are suspect. Recent age-dating of zircon Murda Formation, defined by Scott (in Lyons et al. grains using LA-ICPMS (Quinn et al. unpubl.) indicates 2000), is characterised by magnetite-bearing massive a probable Silurian age for the Kirribilli Formation. red sandstone with minor white sandstone, siltstone and chert. Conodonts observed in the chert are long Oceanic crust and associated units ranging, and some appear to span the Late Ordovician In the eastern Lachlan Orogen just west of the Gilmore interval, though none provide a precise age (Percival, Fault Zone near Tumut, Ordovician mafic volcanics Palaeontological Appendix in Lyons et al. 2000). include the Nacka Nacka Metabasic Igneous Complex Other formations and subdivisions of the which has tholeiitic chemistry and contains hornblende Girilambone Group described from the exposed eastern with K–Ar dates of ~466 Ma (Basden 1990). Near West margin of the Lachlan Orogen west of Nyngan and Wyalong, mafic tholeiitic rocks are represented by the Tottenham include the Break O’Day Amphibolite (on Narragudgil Volcanics (defined by Duggan, in Lyons the Bobadah 1:100 000 map sheet: Pogson 1991), and et al. 2000). They are geochemically primitive, low 2K O, clastic rocks (phyllite, sandstone, quartzwacke and with a flat rare earth element pattern and have been quartz–mica schist) from drill core in the vicinity of the attributed to an ocean floor setting, either on a ridge or Tritton copper prospect, named the Tritton Formation back arc basin (Duggan & Lyons 1999; Duggan, in Lyons (Fogarty 1998) that unconformably overlies ‘basement et al. 2000). A minimum age is based on intrusion by the schist’ of unknown age. Constituents of the Tottenham Early Silurian (433.7 ± 2.3 Ma) Bland Diorite and a suite Subgroup on the Narromine 1:250 000 sheet including of dykes geochemically related to the diorite (L.P. Black the Mount Royal Formation, Bogan Schist and pers. comm., in Lyons et al. 2000, p38). Carolina Forest Formation were defined by Sherwin Initial descriptions of the Jindalee Group (Basden (1996) based on underground sections and drill core 1982, 1990; Warren et al. 1995) tentatively assigned a examined by Suppel (1977); these rocks are moderately Cambrian? to Early Ordovician age to a disparate set of strongly metamorphosed and lack fossils. loosely associated rocks in the Tumut and Cootamundra Parkes–Forbes–Junee area regions that entirely lacked fossils or isotopic age dating. Subsequent discovery of conodonts (Percival Poorly exposed quartz-rich turbiditic rocks between 1999b) spanning a late Darriwilian to Gisbornian – the Junee Narromine and Molong volcanic belts of range in the Hoskins Chert (Lyons, Duggan & Wallace the Macquarie Arc have been assigned to the Kirribilli in Lyons et al. 2000) provided some age control, as

Formation (Raymond & Wallace, in Lyons et al. 2000) did the documentation of similar late Middle to Late and its possible equivalents, the Bribbaree, Bronxhome Ordovician conodonts including Periodon aculeatus and Trigalong formations (Warren et al. 1995). and Pseudobelodina from chert blocks in the Jindalee Ordovician depositional ages have previously been Group north of Cootamundra (Lyons & Percival 2002). proposed for these units by lithological correlation with Rocks now assigned to the Jindalee Group occupy a either: (1) the Late Ordovician(?) to Early Silurian Cotton discontinuous belt that extends from the Tumut area Formation (Krynen et al. 1990; Warren et al. 1995) or (2) north to Narromine; they comprise a fragmented Early to Middle Ordovician quartz-rich turbiditic rocks ophiolitic sequence of now-serpentinized hartzburgites of the Lachlan Orogen, e.g. the Adaminaby, Wagga and and other ultramafic rocks, gabbros, pillow basalts Girilambone groups (Glen & Wyborn 1997; Meffre et al. and bedded and inter-pillow cherts, and jaspers within 2007). Fossils supporting an Ordovician age for these a younger sedimentary matrix (Quinn unpublished formations are lacking or unsubstantiated, except for late data). This group incorporates the Brangan Volcanics Darriwilian conodonts in the Flint Hill Chert Member (Lyons, Duggan & Wallace, in Lyons et al. 2000) and (of the Bribbaree Formation); however, these isolated Hoskins Chert (on the Forbes 1:250 000 Sheet, near chert units may represent a series of blocks redeposited Grenfell), the Valley View Metabasic Igneous Complex, into younger sediments (Quinn et al. in prep.). The Wermatong Metabasalt and Brungle Creek Metabasalt, Mugincoble Chert (Bowman et al. 1982 after Brunker and Bullawyarra Schist (all on the Tumut 1:100 000 1972; Krynen et al. 1990) that forms prominent ridges in sheet: Basden 1990), as well as some parts of the the area between Mugincoble rail siding and Parkes, also Wambidgee Serpentinite and Gundagai Serpentinite on contains late Darriwilian conodonts including Periodon the Tumut 1:100 000 and Cootamundra 1:250 000 sheets aculeatus and Pygodus serra (Percival 2007b; I. Stewart (Warren et al. 1995). All these units are now interpreted

20 September 2011 as blocks, redeposited together with Wenlock–Ludlow the Junee–Narromine Volcanic Belt and the western limestone and rare dacite clasts, and enclosed by matrix part of the Molong Volcanic Belt where Phases 1 and 2, that is no older than Ludlow–Pridoli in age (Quinn and Phases 2 and 4 are separated by hiatuses in arc et al. unpublished data). Unnamed volcanics east of magmatism. Phase 1 magmatism is characterised by Narromine consist of pillow basalts intermixed with medium to high K calc-alkaline geochemistry, with cherts containing late Darriwilian conodonts (Percival local shoshonites. Phase 1 rocks comprise andesitic and & Glen unpublished data) and are also included in this basaltic? lavas, and coarse-grained volcaniclastic rocks group, although the volcanics were too weathered for that grade up into finer, deepwater graptolitic siltstones meaningful analysis. of late Lancefieldian (La3) to mid Bendigonian (Be2) age (Glen, Crawford et al. 2007; Percival & Glen 2007). Macquarie Arc (Figure 5, columns 12–22) Monzonites with shoshonitic chemistry dated at 481 Ma The Macquarie Arc is a mineral-rich Ordovician mark the last stage of Phase 1 magmatism. intraoceanic island arc that was accreted to Gondwana A hiatus in magmatism of ~9 my, accompanied during the Benambran Orogeny in the earliest Silurian. by uplift and erosion of Phase 1 rocks (Percival & Ages and correlations of stratigraphic units and Glen 2007), predates Phase 2 magmatism, which is major volcanic packages across the Macquarie Arc represented in all three northern volcanic belts. Phase 2 have been presented recently in a detailed review by magmatism is expressed mainly by volcaniclastic Percival and Glen (2007) as part of a synthesis of the lithologies, ranging in age from the early Darriwilian geological evolution and metallogenesis of this region (Da2) to latest Gisbornian, and high/medium K calc- (Crawford, Glen et al. 2007), summarised below. Rocks alkaline lavas intruded by granodiorites and diorites of the Macquarie Arc occur in four belts that reflect (Crawford, Meffre et al. 2007). In both the western accretion followed by dismembering during extension and northern part of the central volcanic belt, Phase 2 in the Silurian–Devonian (Glen et al. 1998). The lavas and volcaniclastic sediments interfinger with late westernmost of these, the Junee–Narromine Volcanic Darriwilian to Gisbornian carbonate shelfal deposits Belt, approximates the core of the arc, containing at (Percival & Glen 2007). least 16 discrete igneous complexes distributed over In the western part of the reconstructed Macquarie a length >200 km. These complexes are buried under Arc, the latest Darriwilian to late Eastonian stages are younger strata and are recognised on the basis of characterised by a second hiatus in arc magmatism aeromagnetic anomalies. The best known examples marked by growth of an extensive shallow-water such as the Narromine, Cowal and Fairholme igneous carbonate platform 500 m thick over an interval of about complexes (described in detail by Crawford, Cooke and five million years (Percival & Glen 2007). This hiatus Fanning 2007) have been extensively drilled by mineral is broadly contemporaneous with Phase 3 magmatism, exploration companies. These complexes exhibit a represented by intrusive 451–447 Ma dacites. In similar history, with an initial Early Ordovician phase the eastern, mainly volcaniclastic, part of the arc, of basalt–andesitic lavas and volcaniclastics being allochthonous limestone bodies of comparable middle intruded (after a significant hiatus) during the later Eastonian age in deep water volcaniclastic sediments Middle Ordovician and Late Ordovician (see figure 2a provide a link to the in-situ platform to the west. Phase 3 in Percival & Glen 2007 for details of stratigraphy). In also coincides with a change in chemistry to high K the Narromine Igneous Complex, this intrusive phase shoshonitic Phase 4 magmatism. This last phase is comprises two petrographically and geochemically divisible into an extrusive interval from late Eastonian distinct suites, one dominated by monzodiorite (Ea4) to mid Bolindian (Bo3), and an intrusive with subsidiary monzonite and monzogabbro with episode in the Llandovery (Early Silurian). Products emplacement ages between 465–460 Ma, and the of both are shoshonitic, and contrast with the largely other characterised by younger dacitic dykes and medium to high K calc-alkaline geochemical signature a granodiorite stock, averaging 445 Ma (Crawford, characteristic of older parts of the arc. Cooke & Fanning 2007). A comparable history has During second generation regional mapping programs been described for the Cowal Igneous Complex in the conducted during the 1990s covering the Bathurst and southern part of the Junee–Narromine Volcanic Belt. Dubbo 1:250 000 map sheets, three groups of Ordovician Volcanic belts further east (Molong Volcanic Belt, and sedimentary rocks (including volcaniclastic, clastic and the northern part of the Rockley–Gulgong Volcanic carbonate strata) were defined for the Molong Volcanic Belt) and the less well known Kiandra Volcanic Belt to Belt. The concepts of these groups changed significantly the south, are largely dominated by volcaniclastic rocks as mapping proceeded, resulting in two of these groups that are inferred to represent parts of the arc apron. being incorporated into the third. As originally defined by The three main magmatic phases (plus an intrusive Pogson (in Pogson & Watkins 1998), the Cabonne Group Phase 3) that characterise the evolution of the arc corresponded generally to rocks of magmatic Phase 4 over 50 million years (Crawford, Glen et al. 2007; by including all Upper Ordovician strata overlying Crawford, Meffre et al. 2007) are best recognised in limestones of Eastonian age. However, with subsequent

Quarterly Notes 21 inclusion of those carbonate-dominated formations Gunningbland Formation (Sherwin & Percival, in (previously assigned to the now-obsolete Barrajin Group), Lyons et al. 2000, modified from Sherwin et al. 1987) together with mostly volcanic and volcaniclastic units of is of late Eastonian (Ea3–4) age, indicated by as yet- Darriwilian to Gisbornian age formerly constituting the undescribed graptolites. This formation also contains Kenilworth Group (also now obsolete — see Appendix), a diverse fauna including brachiopods (Percival 1978, the Cabonne Group as currently defined (in Thomas et al. 1979a, 1979b), trilobites (Edgecombe & Webby 2006, in press) is equivalent to all volcanic and sedimentary 2007) and nautiloids (Percival 2009) in fine sandstones units that comprise magmatic Phases 2 and 4, and thus and siltstones, with corals and stromatoporoids (Webby correlates with the Northparkes Group of the Junee– & Morris 1976; McLean & Webby 1976) in limestone Narromine Volcanic Belt. lenses. The Gunningbland Formation is presumed to Parkes–Gunningbland–Trundle area, central Junee– be overlain by the uppermost beds of the Goonumbla Volcanics, although the contact is covered by soil. Narromine Volcanic Belt (Figure 5, column 12) The palaeontological framework is complemented by TheNelungaloo Volcanics (Sherwin 1973; Sherwin, a detailed volcanic facies analysis of the Goonumbla in Lyons et al. 2000) is the oldest formation in this Volcanics and overlying Wombin Volcanics (Simpson region. Due to poor exposure, the nature of the contact et al. 2005). The youngest Ordovician strata in this with the overlying Yarrimbah Formation (Sherwin, region are siltstones (with minor chert beds) containing in Lyons et al. 2000, modified from Sherwin et al. latest Ordovician (late Bolindian) graptolites listed 1987) is unclear, but appears to be marked by a coarse by Sherwin (1970). Although Sherwin assigned these conglomeratic facies at its base, suggestive of a brief rocks to the ‘lower’ Cotton Formation that is elsewhere erosional interval. Siliceous siltstones that form the of Early Silurian age, thereby implying depositional majority of the Yarrimbah Formation contain graptolites continuity across the Ordovician–Silurian boundary with an age range from late Lancefieldian (La3) to mid that is unproven from any other succession in NSW, Bendigonian (Be2) (Sherwin 1979, 1990). This formation more likely these siltstones are facies equivalents of the is unconformably overlain by volcaniclastic rocks and near-contemporaneous Jingerangle Formation exposed andesitic lavas of the Goonumbla Volcanics (Sherwin to the southwest between Grenfell and West Wyalong.

1973; Krynen et al. 1990) the concept of which has been Ordovician volcanic rocks lying east of the Parkes

modified several times, by Percival (in Lyons et al. 2000), Thrust, that were recognised and defined by Sherwin

Simpson et al. (2005) and Percival and Glen (2007). The et al. (1987) and Krynen et al. (1990), include the Northparkes Group (originally Northparkes Volcanic Parkes Volcanics (in a high-strain zone near Parkes)

Group of Percival, in Lyons et al. 2000) was established and Daroobalgie Volcanics (north of Forbes). The to include the Goonumbla Volcanics and correlative Parkes Volcanics were described by Crawford, Meffre – volcanic and sedimentary units. In the Trundle Bogan et al. (2007) as moderately plagioclase-phyric basaltic Gate area, this group includes poorly exposed andesitic andesites and andesites with subordinate augite to trachyandesitic lavas, tuffs, volcaniclastic breccias and phenocrysts, that are compositionally distinct from sparse fossiliferous limestones containing Eastonian both the Early Ordovician Nelungaloo Volcanics, and corals and conodonts (Pickett & Ingpen 1990), named the Middle to Late Ordovician Goonumbla Volcanics. the Raggatt Volcanics by Sherwin (1996), that correlate Crawford, Meffre et al. (2007) interpreted geochemical with the Goonumbla Volcanics. West of Parkes affinities of the Parkes Volcanics as closer to the Cargo in the Gunningbland district, several fossiliferous Volcanics and Walli Volcanics (Phase 2) of the Molong formations appear to be contemporaneous with the Volcanic Belt. In contrast, Crawford, Meffre et al. majority of the Goonumbla Volcanics, whereas to the (2007) found that the Daroobalgie Volcanics have a north and south of Parkes, comparable sedimentary shoshonitic signature comparable to the Goonumbla units are rare to absent (with one notable exception Volcanics, implying that this unit should not be merged of a fossiliferous arkose containing late Eastonian with the Parkes Volcanics as proposed by Sherwin and corals) and therefore continuity of Goonumbla Percival (in Lyons et al. 2000). Volcanics is assumed from the Darriwilian to early Bolindian. Conodont data from Zhen and Pickett Marsden–West Wyalong–Temora, southern Junee– (2008) show that the oldest limestone lens within Narromine Volcanic Belt (Figure 5, column 13) the basal Goonumbla Volcanics is early Darriwilian Ordovician stratigraphy of the southern part of the (Da2). The Billabong Creek Limestone (first named Junee–Narromine Volcanic Belt, where exposures by Sherwin 1970, although its Late Ordovician age are few, is comparatively poorly known. Percival was earlier recognised by Packham 1967; redefined by et al. (2006) documented a diverse conodont, coral Percival, in Lyons et al. 2000) is well-constrained by and stromatoporoid fauna of Eastonian age from conodonts and coral assemblages (Pickett & Percival unnamed limestone intersected in exploratory drilling 2001) ranging in age from late Darriwilian (Da4) to by Newcrest Mining Ltd in the Barmedman Creek early Eastonian (Ea2). The conformably overlying area, south of Marsden. The Jingerangle Formation,

22 September 2011 described by Warren et al. (1995) and Percival and limestones (Percival et al. 2001) is — apart from one Lyons (in Lyons et al. 2000), is exposed further southeast species of stromatoporoid in common — quite distinct towards Quandialla. It is predominantly a spiculitic from that in the overlying Reedy Creek Limestone (Ross facies of deep water origin containing sponges, a 1961; Adrian 1971), and its correlative, the Cliefden diverse nautiloid fauna and graptolites of probable early Caves Limestone Subgroup to the south. A graptolite Bolindian age (Percival et al. 2006). fauna from the middle of the overlying Cheesemans Warren et al. (1995) defined and assigned Creek Formation (Sherwin 1971) was revised by Ordovician ages to several volcanic and volcaniclastic VandenBerg (2003), who assigned a late Eastonian to rock packages in the southmost part of the Junee– early Bolindian age. Narromine Volcanic Belt on the Cootamundra Bowan Park, central western Molong Volcanic Belt

1:250 000 geological sheet, including the Gidginbung (Figure 5, column 15) Volcanics, Temora Volcanics, Junawarra Volcanics, Although Morgan, Scott and Krynen (in Pogson & and several units such as the Belimebung Volcanics, Watkins 1998) advocated that the term Cargo Andesite Boonabah Volcanics, Grogan Volcanics and be suppressed in favour of the Fairbridge Volcanics in Currumburrama Volcanics, that are only recognised the Cargo–Cudal–Bowan Park area, this suggestion has in the subsurface from borehole intersections. The been superseded by the studies of Simpson et al. (2007) Gidginbung Volcanics have high K calc-alkaline to and Crawford, Meffre et al. (2007), who have shown shoshonitic affinities (Glen, Spencer et al. 2007) and are that the Cargo Volcanics is distinct geochemically overlain by limestone containing an early Llandovery from the Fairbridge Volcanics. Hence the name Cargo conodont (Percival & Glen 2007, p. 149), so are most Volcanics (modified after Stevens 1950) is reinstated likely part of the Ordovician arc sequence. Although for the succession of lavas and volcaniclastics that are the Temora Volcanics are also shoshonitic, they are overlain unconformably by the Bowan Park Limestone associated with sparse fossils implying a Silurian Subgroup (modified after Stevens 1957) of the Cabonne age (Warren et al. 1995). The Junawarra Volcanics Group. The highly fossiliferous limestone contains are excluded by their tholeiitic geochemistry from conodont faunas, described by Zhen et al. (1999), that the Macquarie Arc (Wyborn 1996) and their age is range in age from the Taoqupognathus philipi conodont conjectural. Ordovician ages interpreted for the other Zone (early Eastonian, Ea1) in the lower Daylesford volcanic units mentioned here are speculative. Limestone (described and subdivided into multiple Bakers Swamp–Molong, northern Molong Volcanic Belt members by Semeniuk 1970, 1973) at the base of (Figure 5, column 14) the Bowan Park succession, through the T. blandus conodont Zone in the Quondong Limestone (Semeniuk In the Bakers Swamp area, the age of the conformable 1970, 1973), and into the T. tumidus Zone (late boundary between the volcaniclastic Mitchell Eastonian, Ea3–4) within the Downderry Limestone Formation (Morgan & Scott, in Meakin & Morgan Member of the Ballingoole Limestone (Semeniuk 1999) and the overlying Hensleigh Siltstone (Wolf 1970, 1973) at the top of the subgroup and also in et al. 1968) is provided by an upper Prioniodus elegans limestone clasts within the basal part of the overlying conodont fauna (mid to late Bendigonian age) obtained Malachis Hill Formation (Stevens 1957). Higher in from autochthonous limestones at the boundary, and the latter formation, about 300 m above siltstones from allochthonous limestones in the lower part of with an undescribed early Bolindian (Bo2?) graptolite the Hensleigh Siltstone (Zhen et al. 2004a). Graptolites fauna, limestone pods of probable allochthonous origin from the upper Hensleigh Siltstone are currently contain a diverse coral assemblage (Fauna IV of McLean under study (Kraft, Percival, Erdtmann & Sherwin, in & Webby 1976) believed to be of mid–late Bolindian prep.). A sparse conodont fauna from allochthonous (Bo3–4?) age (Percival & Glen 2007). limestones in the lower Fairbridge Volcanics (named by Adrian 1971; described in detail by Morgan, Scott & Belubula River valley, south of ‘Canomodine’, south- Percival, in Meakin & Morgan 1999) suggests an early western Molong Volcanic Belt (Figure 5, column 16) to mid-Darriwilian age (Percival et al. 1999). More The Cargo Volcanics in this area remained exhumed precise age control is provided by conodonts from the longer than at Bowan Park to the north, as carbonate Wahringa Limestone Member (Morgan, Percival & deposits, represented by the Canomodine Limestone Scott, in Meakin & Morgan 1999), which range in age (Stevens 1950) (including the synonymous Cargo Creek from late Darriwilian (Da4) to late Gisbornian (Gi2) Limestone) did not accumulate until Eastonian 2 time, (Zhen et al. 2004b). The upper beds of this unit therefore extending into the late Eastonian (Ea3). The age is based correlate with the Yuranigh Limestone Member on coral and stromatoporoid faunas (Webby 1969); (Scott & Pogson, in Pogson & Watkins 1998) near due to the sheared nature of the limestone, conodonts the top of the Fairbridge Volcanics in the vicinity of have not been obtained. The Canomodine Limestone Molong. The diverse fauna dominated by brachiopods, is overlain by the Rockdale Formation (Ryall 1966), stromatoporoids and sponges described from these a succession of siltstones of probable latest Eastonian

Quarterly Notes 23 to early Bolindian age (graptolites identified by Ryall Belubula River, the Ordovician stratigraphy contrasts would suggest a Gisbornian age, but the limited fauna markedly with that of the Cliefden Caves area to the requires revision) that is equivalent to the lower part southwest, owing to separation by a major thrust fault. of the Malachis Hill Formation. The youngest unit in The oldest unit recognised in the Cadiangullong Creek this area, assigned a latest Ordovician age (although valley is the Weemalla Formation (name formalised by palaeontological evidence is lacking), is the Millambri Wyborn, Krynen & Pogson, in Pogson & Watkins 1998, Formation (modified by Ryall 1966, from the usage of after unpublished thesis mapping by J. Taylor) which Stevens 1957 to include only the upper turbiditic sand- contains an undescribed Darriwilian (Da3) graptolite dominated part of his original Millambri Formation), fauna (Smith 1966), as well as calcareous mudstone composed of volcaniclastic sandstone and conglomerate beds yielding conodonts of Da2 age (Zhen & Percival containing clasts of andesitic volcanics. 2004b). Andesitic volcanics and volcaniclastic strata Cliefden Caves area, southeastern Molong Volcanic Belt conformably overlying the Weemalla Formation in the vicinity of Cadia are named the Forest Reefs Volcanics (Figure 5, column 17) (defined by Wyborn, in Pogson & Watkins 1998), for TheKenyu Formation (Stevens 1955), a volcanic and which the only internal age control is provided by Late volcaniclastic unit in the southern-most part of the Ordovician (Eastonian, Ea3) conodonts from thin Molong Volcanic Belt, has recently been determined to beds of altered limestone in its upper part (Packham

be as young as latest Gisbornian in age (Percival et al. et al. 1999). The Forest Reefs Volcanics beneath these 2008), based on conodonts from an allochthonous limestone interbeds is therefore contemporaneous with limestone block in its upper part. This age suggests a the Walli Volcanics and the Cliefden Caves Limestone minimal hiatus between the top of the correlative Walli Subgroup (Percival & Glen 2007), although there is no Volcanics (modified by Krynen & Pogson, in Pogson evidence of concurrent eruptive volcanism in the latter & Watkins 1998, after Stevens 1952) in the Cliefden above the middle of the Fossil Hill Limestone Member. Caves area and the disconformably overlying Cliefden To explain the absence of volcanic detritus in the Caves Limestone Subgroup (modified by Krynen Cliefden Caves Limestone Subgroup (and in correlative & Pogson, in Pogson & Watkins 1998, after Stevens formations such as the Regans Creek Limestone along 1952). Three formations (the lowermost with multiple strike to the north), Packham et al. (1999) put forward members) have been described by Webby and Packham (1982) from this limestone: the well-bedded Fossil the hypothesis that the Eastern Province of the Molong Hill Limestone at the base, overlain by the massive- Volcanic Belt (where Middle and Late Ordovician bedded Belubula Limestone, in turn overlain by the volcanism was concentrated) was not juxtaposed with Vandon Limestone. Conodonts obtained throughout the carbonate-dominated Western Province until the these limestones are of early Eastonian (Ea1–2) age latest Ordovician to earliest Silurian. (Zhen & Webby 1995), correlative with the Daylesford Forest Reefs–Junction Reefs–Blayney area Limestone to Quondong Limestone succession of (Figure 5, column 19) the Bowan Park Limestone Subgroup. Many papers Several different interpretations of stratigraphic have been published over the past forty years (mainly relationships in this area have been proposed in recent by Webby, Percival and colleagues) describing the diverse fossil assemblages of trilobites, brachiopods, years (see discussion in Zhen & Percival 2004b). The rugose and tabulate corals, stromatoporoids and following summary follows the views of Percival

sponges in the Cliefden Caves Limestone Subgroup and Glen (2007) and Crawford, Glen et al. (2007). and their depositional environments (see references TheCoombing Formation (modified by Wyborn, listed in Webby 1992). Siltstones and spiculites of the in Pogson & Watkins 1998, from the description of overlying Malongulli Formation (Stevens 1952) contain Wyborn 1992, to encompass only feldspathic mudstone diagnostic graptolite faunas close to its base (Ea3) and that is commonly silicified and grades to fine-grained top (Bo1) (Percival 1976), and its Late Ordovician age is volcaniclastic sandstone) is the oldest unit recognised. also is constrained by conodonts found in allochthonous Age constraints on the Coombing Formation are limited deep-water sponge-bearing limestones in its lower part and of poor quality. Crawford, Meffre et al. (2007) (Trotter & Webby 1995). Mid Bolindian (Bo3) graptolites derived a weighted mean age of 467 ± 4 Ma from a highly (Jenkins 1978) are present in several siltstone horizons distributed and discordant set of analyses (MSWD = 3.2, in the overlying volcaniclastic-dominated Angullong probability of fit = 0.000, n = 19) obtained by laser Formation (Krynen & Pogson, in Pogson & Watkins ablation ICP-MS U/Pb analyses of detrital zircons, to 1998, after Stevens 1952) but to date, no age-diagnostic imply an early Darriwilian volcanic source. Additionally, conodonts have been found in allochthonous limestones a few poorly preserved graptolites of probable late that are sporadically encountered in this unit. Darriwilian to Gisbornian age are known from the Junction Reefs area. In the vicinity of Forest Reefs, the Cadia–Panuara area (Figure 5, column 18) Coombing Formation is overlain by the Forest Reefs Between Panuara (southwest of Cadia mine) and the Volcanics (discussed above), with the first appearance of

24 September 2011 pyroxene-phyric lavas occurring just beneath the Mount River valley northwest of Euchareena (Zhen & Percival Pleasant Basalt Member. The latter was previously 2004a), but the age of the enclosing matrix is presently attributed to the Weemalla Formation by Wyborn (in unknown. Detailed mapping is necessary to adequately Pogson & Watkins 1998), but as noted by Percival and characterise this formation, which seems to constitute Glen (2007), based on stratigraphic revisions by Zhen and an amalgamation of facies and ages. Percival (2004b), the Weemalla Formation is not present in the Forest Reefs area east of the Wongalong Fault. Cumnock north to Ponto, west of the Catombal Range In the Blayney region further east, the Coombing Recent mapping and palaeontological discoveries in Formation is overlain by a thick succession the Ponto–Bournewood area west and southwest of predominately composed of basalt and basaltic andesite, Wellington (Percival & Quinn 2011) have resulted in that was subdivided by Crawford, Meffre et al. (2007) substantial revision of the stratigraphy of this region. on petrographic and geochemical grounds into the Rocks previously referred to the western outcrop lower and upper Blayney Volcanics, the Byng Volcanics, belt of the Oakdale Formation (Percival et al. 1999, and the Millthorpe Volcanics. Age control is restricted figures 1 & 4) have been reinterpreted as allochthonous to the occurrence of poorly preserved conodonts blocks of Late Ordovician age within probable Silurian from recrystallised limestone known as the Cowriga matrix in the Arthurville area. In the vicinity of the Limestone Member (of the upper Blayney Volcanics) former Gunners Dam mine along strike to the south, exposed at the Browns Creek mine; these conodonts strata informally named the ‘Gunnars Dam beds’ by were attributed a Late Ordovician age by B. Nicoll (pers. Percival and Glen (2007) are now regarded as blocks comm. to Wyborn & Krynen, in Pogson & Watkins of cherty spiculitic and graptolitic siltstone of Late 1998). The Blayney Volcanics (described by Wyborn, Ordovician age emplaced into the Lower Silurian in Pogson & Watkins 1998) has a clinopyroxene-phyric Kabadah Formation. Allochthonous Late Ordovician and olivine-phyric lower part, and a plagioclase-phyric limestone clasts, redeposited into the Upper Silurian upper part (Crawford, Meffre et al. 2007). The original Barnby Hills Shale, have previously been documented definition and distribution of the Byng Volcanics (Scott, from the Eurimbla area, northeast of Cumnock in Pogson & Watkins 1998), was modified by Crawford, (Zhen, Percival & Farrell 2003). Similarly, several large Meffre et al. (2007) to include only primitive basalts limestone lenses of Late Ordovician age mapped as associated with ultramafic cumulates, that are interpreted an unnamed member within the Sourges Shale in the on the basis of their shoshonitic affinities to be vicinity of Cumnock (Percival et al. 1999, figure 5) — the comagmatic with the upper Blayney Volcanics. Crawford, southernmost one of early Eastonian (Ea1) age and of Meffre et al. (2007) distinguished other volcaniclastic very shallow water aspect, whereas those to the north on rocks with evolved basaltic to basaltic andesite lavas, a markedly different trend are significantly younger (Ea3) previously also included in the Byng Volcanics, as the and contain a deeper water fauna — are now regarded Millthorpe Volcanics. This formation appears to lie as allochthonous blocks enclosed within sediments of above the level of the Cowriga Limestone Member in the known Llandovery age. This confirms that the Sourges upper Blayney Volcanics and therefore may represent Shale is a Silurian formation within the Cudal Group, as Phase 4 magmatism in this area, east of Orange. foreshadowed by Morgan (in Meakin & Morgan 1999). Thus, according to this new interpretation (Percival & Northeastern margin of Molong Volcanic Belt Quinn 2011), autochthonous strata of Ordovician age (Figure 5, column 20) are no longer recognised in the belt extending from In its original type area, between Neurea and Dripstone, Cumnock to Ponto, west of the Catombal Range. southeast of Wellington, the Oakdale Formation Sofala–Mudgee, northern Rockley–Gulgong (Strusz 1960) includes volcaniclastic conglomeratic facies deposited as mass flows, turbiditic sandstone, Volcanic Belt (Figure 5, column 21) and siltstone with Eastonian graptolites. All evidence Along the eastern margin of the Hill End Trough, in a points to the Oakdale Formation being deposited on belt extending southwards from Dunedoo to Rylstone, a slope setting along the (present-day) northeastern strata included in the Cabonne Group are the Coomber, margin of the Molong Volcanic Belt. Autochthonous Burranah and Tucklan formations. The Coomber deep-water carbonate rocks containing early Eastonian Formation (Pemberton et al. 1994; Colquhoun & conodonts at ‘Barham Winchester’, 10 km northeast of Meakin, in Meakin & Morgan 1999) lacks fossils, but Molong, are also assignable to the Oakdale Formation, is assigned a Late Ordovician age based on interpreted as are comparable limestones in the Bakers Swamp area conformable contacts with underlying Adaminaby (sample C1432 in Percival et al. 1999). Webby (1973, Group rocks that include chert bearing Pygodus serra 1974) described rare deep-water trilobites of Gisbornian of late Darriwilian age (Stewart & Fergusson 1995). age from the Neurea area. The oldest fauna from the Fergusson and Colquhoun (1996) described a variety Oakdale Formation are conodonts of late Darriwilian of facies from the Coomber Formation, including (Da3) age, in allochthonous limestones from the Bell massive lithic sandstone, thin-bedded sandstone and

Quarterly Notes 25 mudstone, siliceous or cherty mudstone, together with progressively more dominant up section. It is overlain scattered allochthonous limestone blocks, and sporadic by the Nine Mile Volcanics which is a finer grained basalt flows and shallow intrusions. The Burranah sequence with black shale that contains late Gisbornian Formation (described by Watkins, in Meakin & Morgan graptolites and volcaniclastic laminations (Sherrard 1999), and to a lesser extent, the Tucklan Formation 1954, after Öpik 1952). Rare blocks of limestone yielding (redefined by Colquhoun, Meakin & Henderson, in the Late Ordovician conodont Belodina and a solitary Meakin & Morgan 1999) consists of mass-flow deposits, rugose coral have been reported from isolated localities conglomerates, and minor allochthonous limestones in the Nine Mile Volcanics near Peppercorn Creek that provide the only fossil-based age constraints on (Owen & Wyborn 1979). Such limestones contrast with these units (Percival 1999a). An Ordovician age was the generally deep-water character of the Kiandra Group ascribed to these formations based in part on their high and are unlikely to be in-situ. The Gooandra Volcanics potassium response on ternary U–K–Th radioelement occurs within this upper part of the sequence and is imagery (typical of Ordovician rocks in the Macquarie of limited extent around Gooandra Homestead, with Arc), but indiscriminate application of this criterion much of the mapped area previously attributed to this has led to incorrect assumptions elsewhere, e.g. in formation comprising either volcaniclastic rocks (i.e. on the case of the Kabadah Formation. It is conceivable Long Plain), siliceous siltstone-dominated strata with that the Burranah and Tucklan rocks were originally volcaniclastic debris flows, gritstones and conglomerates deposited in the Late Ordovician, but were subsequently (in the Mt Selwyn to Three Mile Dam area) or siliceous reworked into Silurian deposits of the Hill End Trough. siltstones with interbedded quartz sandstones and Further south along the eastern margin of the Hill turbidite sequences (Geehi River, Mt Jagungal–Grey End Trough, allochthonous limestone blocks of late Mare areas) (Quinn et al., in prep.). The southern Eastonian age (comparable to those in the Burranah and extent of the Kiandra Volcanic Belt in north-east Tucklan formations) have also been recognised (Pickett Victoria (Allen 1988; Orth et al. 1995) is represented 1978; Percival 1999a) in a thick succession mapped as by the Blueys Creek Formation that includes the Sofala Volcanics, first described in detail by Packham Brumby Mafic Arenite Member and Banksia Chert (1968b) from the Turon River valley. Predominant Member; the latter is characterised by black chert lithologies in the Sofala Volcanics include volcaniclastic layers containing the conodonts Periodon aculeatus, conglomerates, sandstones and siltstones of possible deep P. cf. grandis and Belodina sp. (I.R. Stewart, in Allen water turbiditic origin, with pyroxene-rich andesites 1988) indicating a Gisbornian age. and basaltic andesites in the Sofala region that in some cases may represent eruptive centres (Packham 1968b; Watkins, in Pogson & Watkins 1998). Chert is present Narooma Terrane (Figure 5, column 23) throughout the formation, in places forming locally The areally restricted Narooma Terrane on the NSW extensive massive to thick-bedded bands particularly south coast consists of an apparently continuous prominent in the lower part. Although radiolaria and succession of Late Cambrian to Late Ordovician oceanic sponge spicules occur in the chert, no conodonts have sedimentary rocks deposited on the palaeo-Pacific yet been found. The age range of this formation is plate as it drifted towards the east Gondwana margin based on rare, poorly preserved graptolites that remain (Glen et al. 2004). In its type area around Narooma, unillustrated; one species of possible late Darriwilian to the Narooma Terrane comprises the Wagonga Group Gisbornian age was recorded by Packham (1968b, p. 115), (modified from Wagonga Series of Browne 1949, first and another fauna was assigned a mid Bolindian age by named and defined as Wagonga Group by Glen 1994), Fons VandenBerg (cited in Rickards et al. 1998). Ar–Ar consisting of the Narooma Chert and the overlying ages of 438.5 ± 0.8 Ma and 439.9 ± 0.8 Ma for monzonite argillaceous Bogolo Formation. In the revision of the and diorite that intrude the Sofala Volcanics (Perkins stratigraphic nomenclature by Glen et al. (2004), the et al. 1995) provide minimum earliest Silurian ages for Kianga Basalt (established by Glen 1994) was eliminated; deposition of this formation. it was previously interpreted to underlie the Narooma Chert. The lower part of the Narooma Chert (defined Kiandra Volcanic Belt (Figure 5, column 22) by Glen 1994) consists of ribbon chert containing As defined by Owen and Wyborn (1979), the Kiandra conodonts (illustrated in Glen et al. 2004) that range in Group comprised the Temperance Formation, age from Late Cambrian to Darriwilian–Gisbornian. Nine Mile Volcanics and Gooandra Volcanics. New Chert beds in the upper Narooma Chert are extensively mapping currently underway by Quinn (unpublished bioturbated with Planolites tubes (Kakuwa & Webb data) suggests that a significant reassessment of 2010) and alternate with shale and siltstone beds that this stratigraphy is warranted. The Temperance contain Eastonian graptolites. Where not deformed by Formation consists of a bedded chert sequence of late later faulting, the Narooma Chert passes gradationally Darriwilian age (indicated by presence of the conodont upwards into the Bogolo Formation (defined by Wilson Pygodus sp.) with thin mafic volcaniclastic layers become 1969, modified by Glen et al. 2004), which consists of

26 September 2011 argillite, conglomerate with blocks of basalt, chert and now known to be of ‘Middle’ Cambrian to early Late sandstone beds in an argillaceous matrix. Although Cambrian age based on the presence of paraconodonts undated by fossils, this formation is presumed to and absence of euconodonts (Stewart 1995). Hence be of Bolindian age on the basis of its stratigraphic the age of the Pipeclay Creek Formation effectively relationship to the underlying Narooma Chert and the constrains the age of deposition of the underlying presence of derived chert clasts of a wide size range. Murrawong Creek Formation to that of the limestone Outcrops of the terrane 100 km to the north, clasts found in conglomerates of unit 1. Lithologies in extending along the coast from Batemans Bay to the Pipeclay Creek Formation consist predominantly Burrewarra Point, have a less well defined stratigraphy, of siltstone and mudstone with subsidiary chert, tuff, containing blocks of ‘Middle’ and Late Cambrian sandstone and fine-grained conglomerate, more than limestone in basaltic breccia (Bischoff & Prendergast 900 m in total thickness (Bradley, in Pickett 1982; 1987; Prendergast 2007). One clast of a limestone Cawood 1983; Leitch & Cawood 1987). coquina from the southern side of Burrewarra Point Unconformably overlying the Cambrian sedimentary yielded a diverse microfauna characterised by abundant rocks is the Haedon Formation (Cawood 1983) that molluscs, indeterminate agnostid trilobite remains, includes sandstones and boulder conglomerates lingulate brachiopods, and rare conodonts including with clasts comprising limestone, mudstone, basalt Furnishina furnishi. A ‘Middle’ Cambrian (no older than and andesite. Autochthonous massive and bedded basal Undillan, i.e. late Drumian) age is postulated for limestones are intercalated with the conglomerates this limestone (Bischoff & Prendergast 1987). Overlying (Furey-Greig 2003a). Maximum thickness is estimated black shales assigned to the upper part of the Wagonga to be 100 m. The Middle Ordovician (Darriwilian) age Beds (now Group) by Jenkins et al. (1982) contain obtained for this formation from conodonts (including graptolite faunas at two levels, the older one of mid- Ansella jemtlandica, Oistodus lanceolatus, and Periodon Eastonian (Ea2–3) age and the younger fauna of early aculeatus) and the gastropod Macluritella sp. (Cawood Bolindian age. Most likely these black shales correlate 1976; Furey-Greig 2003a) may be further refined with the upper part of the Narooma Chert. to Da2–3 on the basis of fragmentary specimens of conodonts resembling Appalachignathus, Juanognathus? New England Orogen and possibly Periodon macrodentatus. Packham (1969, p. 231) reported the Early Ordovician (Bendigonian) graptolite Didymograptus cf. Tamworth Belt (Figure 5, column 24) D. minutus (currently under study by Kraft, Percival, The oldest rocks in the Tamworth Belt, of ‘Middle’ Erdtmann & Sherwin) from an isolated outcrop of Cambrian to early Late Cambrian age, are localised clastic sediments associated with the ‘Trelawney beds’. immediately west of the Peel Fault in the Copes Creek Limestones forming the latter unit are now regarded as area, southeast of Tamworth. The succession commences allochthonous blocks of Late Ordovician age emplaced with the Murrawong Creek Formation (Cawood 1983; in the Drik Drik Formation (with a depositional Leitch & Cawood 1987), being at least 450 m thick above age of Early Devonian: Emsian) (see Furey-Greig a faulted contact, and consisting largely of volcaniclastic 2000b pp. 133–134). Corals (Webby 1988) and conodonts sandstones interbedded with conglomeratic units. The (Furey-Greig 2000b) from these allochthonous blocks lowermost of these, designated unit 1, is 65 m thick and are of Eastonian age. The Drik Drik Formation is dominated by coarse-grained allochthonous limestone unconformably overlies the Haedon Formation, with blocks yielding a diverse shelly fauna of late ‘Middle’ the unconformity surface marked by the sudden Cambrian age (Undillan–Boomerangian, P. punctuosus appearance of red sandstone (Crook 1961; Cawood 1983; to L. laevigata trilobite zones). Fossils described from Furey-Greig 2003a) and basal conglomerates containing this level include a possible cnidarian (Engelbretsen limestone clasts yielding Ordovician conodonts. 1993), lingulate brachiopods (Engelbretsen 1996), molluscs (Brock 1998a) possible rhynchonelliformean Dunmore Terrane of Central Block brachiopods (Brock 1998b, 1999) and trilobites (Cawood The Wisemans Arm Formation of Leitch and Cawood 1976, Sloan & Laurie 2004). Unit 2 (20 m thick) in the (1980) sensu Furey-Greig (1999, 2003b), in the Manilla middle of the Murrawong Creek Formation, and unit 3 region north of Tamworth previously included what occupying the uppermost 80 m of the formation, are were interpreted as olistoliths of limestones and characterised by fine non-fossiliferous conglomerates. laminated fine-grained feldspathic sandstones. Brown Palaeontological evidence supporting essentially (2009) reinterpreted these blocks as fault-bounded, contemporaneous deposition of the allochthonous and assigned them to a unit he named the Glen Bell limestone blocks of unit 1 with the enclosing sediments Formation, incorporating the ‘Uralba Beds’ of Hall 1975 is provided by the conformably overlying Pipeclay (see Appendix for details). Possibly equivalent rocks Creek Formation, named by Crook (1961), who assigned in the Bingara 1:100 000 sheet to the north have been an Early Devonian age. Chert beds in the formation are referred to the Dinoga Formation (Aitchison et al. 1988;

Quarterly Notes 27 Barclay et al. 1999). These rocks occur immediately stratigraphy that have taken place in NSW over the east of the Peel Fault, in what is presumed to represent past three decades, although much more work needs the subduction complex in front of the magmatic arc to be done — particularly in areas such as the Kiandra (Leitch & Cawood 1980). Allochthonous limestone Volcanic Belt and the various serpentinite belts — blocks within the Glen Bell Formation contain macro- before relationships between terranes are adequately and microfaunas of two distinct ages: Late Ordovician defined. Placing all Cambrian and Ordovician rocks (Eastonian), and Early Silurian (late Llandovery to early known from NSW in the context of a unified timescale Wenlock). Depositional age of the Glen Bell Formation reveals some interesting patterns which provide a key to matrix must therefore be no older than Early Silurian, interpreting the tectonic evolution of the region over this so strictly speaking this is not an Ordovician unit time interval. Comparable facies in Middle and Upper (and therefore is not shown on Figure 5). However, it Ordovician turbidite successions that are widespread demonstrates that Late Ordovician limestones were in south-eastern Australia have in the past been given either once present in the Dunmore Terrane, or else they different names in NSW and Victoria. As these can now were deposited on the palaeo-Pacific plate and now lie be shown to be identical in age and appearance, and in the Dunmore Terrane due to accumulation in the exhibit reasonable continuity in the field, we argue that subduction complex. Evidence for the Late Ordovician they should be referred to the same unit. This process clast age is indicated by the presence of conodonts of is already underway with rocks of the Bendoc Group Eastonian, most likely Ea3, age (Furey-Greig 1999, being recognised throughout the Tasmanides of south- 2000a, 2003b; Pickett & Furey-Grieg 2000), and corals of eastern Australia. Adopting a common name (such as comparable or very slightly younger age (perhaps Ea3–4) Numeralla Chert) for the generally thick-bedded chert of (Hall 1975; Webby 1988). late Darriwilian age at or near the top of the Adaminaby Group would clarify much of the stratigraphy of the Port Macquarie Block (Figure 5, column 25) turbidite successions. However, distinguishing the ages ThePort Macquarie Serpentinite, defined by Och, of these Ordovician cherts is critical. At least five distinct Leitch and Caprarelli (2007), consists of massive and conodont-based zones, extending from late Tremadocian schistose serpentinite together with rodingite (highly to latest Darriwilian, can be recognised in cherts in altered mafic rocks, possibly originally dykes). The the Adaminaby Group and correlatives. If mapped serpentinite body is undated, although the ultramafic on lithology alone, these cherts could readily be mis- protolith is interpreted to be possibly as old as Early correlated, but when different units are discriminated Cambrian on the basis of correlation with comparable on the basis of conodont zones (though contrary to the serpentinised ultramafic rocks of the Woodsreef Australian Code of Stratigraphic Nomenclature), more Melange in the southern New England Orogen, dated accurate mapping results. at 530 Ma by Aitchison and Ireland (1995) using The new and revised correlations presented here are zircons from plagiogranite blocks. At Rocky Beach, of fundamental importance to biogeographic analyses the serpentinite encloses two small bodies of chlorite– that have widespread applicability in constraining actinolite schist containing blocks of high pressure tectonic reconstructions. For example, ‘Middle’ metamorphic rocks including blueschist and lawsonite Cambrian limestones are known in NSW from three eclogite. These exposures were named the Rocky Beach widely separated localities. The Murrawong Creek Metamorphic Melange (Och et al. 2003). They are Formation (New England Orogen) has rhynchonelliform undated, but are believed to be of similar age to the brachiopod faunas (Brock 1998a, b), for example, that surrounding serpentinite. share strong affinities at genus, but not species, level The serpentinite body is surrounded by the Watonga with the somewhat younger First Discovery Limestone Formation (Och, Leitch & Caprarelli 2007), that is well Member of the Coonigan Formation in the Delamerian exposed along the coastline immediately south of Port Orogen. Also micromolluscan faunas in these two Macquarie where it comprises mostly broken formation formations reveal three species in common, but these inferred to result from disruption of a once-stratified similarities appear to be outweighed by differences in sequence of basalt, chert, siliceous mudstone, siltstone, the remainder of the fossil assemblages. In comparing sandstone and conglomerate. Conodonts visible in thin faunal elements between different offshore terranes, sections of cherts establish a maximum age range for Engelbretsen (1993) identified two species of acrotretide these rocks extending from late Darriwilian to possibly brachiopods common to both the Murrawong Creek as young as the end of the Eastonian (Och, Percival & Formation faunas (Undillan–Boomerangian, P. Leitch 2007). punctuosus to L. laevigata trilobite zones) and those from ‘Middle’ Cambrian limestone clasts at Batemans Bay (basal Undillan or younger) associated with Synthesis the Narooma Terrane. Both these widely separated This review highlights the considerable advances occurrences can therefore be interpreted as essentially in understanding of Cambrian and Ordovician contemporaneous, representing faunas inhabiting

28 September 2011 shallow water environments of near-emergent Aitchison J.C., Blake M.C. jr, Flood P.G. & Murchey seamounts in the palaeo-Pacific Ocean that were B.L. 1988. New and revised stratigraphic units from the relatively remote from assemblages that were to develop southwestern New England Fold Belt. Quarterly Notes of slightly later on the Delamerian continental margin, the Geological Survey of New South Wales 72, 10–16. thereby explaining the subtle biogeographic signatures Aitchison J.C. & Ireland T.R. 1995. Age profile of distinguishing these faunas. ophiolitic rocks across the late Palaeozoic New England Finally, the dynamism of geological processes during Orogen, New South Wales: implications for tectonic the Early Palaeozoic evolution of the Lachlan and New models. Australian Journal of Earth Sciences 42, 11–23. England orogens is readily appreciable from this review, Allen R.L. 1988. Limestone Creek Graben. In: J.G. highlighting the numerous examples of Ordovician Douglas & J.A. Fergusson eds. Geology of Victoria (2nd rocks that have been entirely eroded from their original edition), p. 92. Geological Society of Australia, Victorian depositional settings, leaving only their records as Division, Melbourne. allochthonous blocks within younger strata. Recognition Andrews E.C. 1913. Advance report on the Mount of such occurrences of lost stratigraphy, which often Boppy goldfield. In: Annual Report of the Department of depends on palaeontological discrepancies between Mines, New South Wales, for the year 1912, pp. 177–178. clasts and matrix, has significantly increased over the past decade given the greater precision and widespread Andrews E.C. 1915. The Canbelego, Budgery and use of conodont age-determinations combined with Budgerygar Mines. Part II of the Cobar Copper and Gold- careful field observations. Field. Mineral Resources 18. Geological Survey of New South Wales. Acknowledgements Barclay A., Furey-Greig T. & Leitch E.C. 1999. A reappraisal of the Palaeozoic Dinoga Formation, Bingara, We are grateful to our colleagues in the Geological New South Wales. In: Flood P.G. ed. New England Survey of New South Wales engaged in regional Orogen, pp. 45–46. Earth Sciences, University of New mapping programs in the Lachlan, New England and England, Armidale NSW. Delamerian orogens during the past decade, who have reappraised or described many of the stratigraphic Basden H. 1982. Preliminary report on the geology of units reviewed in this paper, and acknowledge their the Tumut 1:100,000 sheet area. Quarterly Notes of the contributions — some of which are in press at the time Geological Survey of New South Wales 46, 1–18. of publication of this review. Gary Colquhoun supplied Basden H. 1990. Geology of the Tumut 1:100,000 Sheet data on distribution of Cambrian and Ordovician 8527. Geological Survey of New South Wales, Sydney. strata in the state as the basis for Figures 1 and 2. David Bischoff G.C.O. & Prendergast E.I. 1987. Newly Barnes assisted with photography of conodonts in chert discovered Middle and Late Cambrian fossils from the sections and compilation of Plate 1. Cartographic and Wagonga Beds of New South Wales, Australia. Neues editorial expertise was provided by Cheryl Hormann, Jahrbuch für Geologie und Paläontologie Abhandlungen Carey Martin, Geneve Cox and Simone Meakin. The 175, 39–64. Australian Stratigraphic Names database administered Black L.P. 2005. SHRIMP U–Pb zircon ages obtained by Geoscience Australia and accessible via their website, during 2004/05 for the NSW Geological Survey. Geological proved invaluable in searching for references to some Survey File GS2005/745. Geological Survey of New South obscure units. We particularly thank Barry Webby for Wales. his perceptive review of the original manuscript that has significantly improved the published version. Black L.P. 2006. SHRIMP U–Pb zircon ages obtained during 2005/06 for NSW Geological Survey projects. Geological Survey File GS2006/821. Geological Survey of References New South Wales Report.

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36 September 2011 Strusz D.L. & Henderson G.A.M. 1971. Canberra City Tectonophysics 214, 177–192. A.C.T. 1:50,000 geological map and explanatory notes. VandenBerg A.H.M., Willman C.E., Maher S., Bureau of Mineral Resources, Geology & Geophysics, Simons B.A., Cayley R.A., Taylor D.H., Morand Canberra. V.J., Moore D.H. & Radojkovic A. 2000. The Tasman Stuart-Smith P. & Wallace D. 1997. Oberon 1:100 000 Fold Belt in Victoria. Geology and mineralisation of geological map 8830. Australian Geological Survey Proterozoic to Carboniferous rocks. Geological Survey Organisation, Canberra and Geological Survey of New of Victoria, Special Publication. Department of Natural South Wales, Sydney. Resources and Environment, Melbourne. Suppel D.W. 1977. Copper deposits in the Girilambone VandenBerg A.H.M., Willman C.E., Morand V.J., Beds, Tottenham, New South Wales. Geological Survey McHaffie I.W., Simons B.A., Quinn C. & Westcott Report GS1977/300. Geological Survey of New South A.L. 2004. Buffalo 1:100 000 map area geological report. Wales. Geological Survey of Victoria Report, 124. Talent J.A. & Mawson R. 1999. North-eastern Molong Wang Q., Mills K.J., Webby B.D. & Shergold J.H. Arch and adjacent Hill End Trough (Eastern Australia): 1989. Upper Cambrian (Mindyallan) trilobites and Mid-Palaeozoic conodont data and implications. In: R. stratigraphy of the Kayrunnera Group, western New Feist, J.A. Talent & A. Daurer eds. North Gondwana: South Wales. BMR Journal of Australian Geology & Mid-Paleozoic Terranes, Stratigraphy and Biota. Geophysics 11, 107–118. Abhandlungen der Geologischen Bundesanstalt 54, 49–105. Warren A.Y.E., Gilligan L.B. & Raphael N.M. 1995. Cootamundra 1:250 000 Geological Sheet SI/55-11: Thomas O.D., Pogson D.J., Simpson C., Sherwin L., Explanatory Notes. Geological Survey of New South Scott M.M. & Johnston A. in press. Geology of the Wales, Sydney Goulburn, 1:250 000 sheet: Explanatory Notes. Geological Survey of New South Wales, Maitland. Warris B.J. 1967. The Palaeozoic stratigraphy and palaeontology of north-western New South Wales. Ph.D. Thomas O.D., Scott M.M., Warren A.Y.E. & Sherwin L. thesis (unpubl.), University of Sydney. 2001. Gunning 1:100 000 Geological Sheet 8728, provisional. Geological Survey of New South Wales, Orange. Warris B.J. 1969. The Mt Arrowsmith area. In: G.H. Packham ed. Palaeozoic sequences: Cambrian and Trigg S.J. 1987. Geology of the Kilparney 1:100,000 Sheet Ordovician beds. Journal of the Geological Society of 8132: Explanatory Notes. Geological Survey of New South – Wales, Sydney. Australia 16(1), 69 70. Trotter J.A. & Webby B.D. 1995. Upper Ordovician Webby B.D. 1969. Ordovician stromatoporoids from – conodonts from the Malongulli Formation, Cliefden New South Wales. Palaeontology 12, 637 662. Caves area, central New South Wales. AGSO Journal of Webby B.D. 1973. Remopleurides and other Upper Australian Geology & Geophysics 15, 475–499. Ordovician trilobites from New South Wales. VandenBerg A.H.M. 1981. A complete Ordovician Palaeontology 16, 445–475. graptolitic sequence at Mountain Creek near Deddick, Webby B.D. 1974. Upper Ordovician trilobites from eastern Victoria. Geological Survey of Victoria, Report central New South Wales. Palaeontology 17, 203–252. 1981/81. Webby B.D. 1978. History of the Ordovician continental VandenBerg A.H.M. 2003. Discussion of ‘Gisbornian platform shelf margin of Australia. Journal of the (Caradoc) graptolites from New South Wales, Australia: Geological Society of Australia 25, 41–63. systematics, biostratigraphy and evolution’ by B. Webby B.D. 1983. Lower Ordovician arthropod trace Rickards, L. Sherwin and P. Williamson. Geological fossils from western New South Wales. Proceedings of the Journal 38, 175–179. Linnean Society of New South Wales 107, 59–74. VandenBerg A.H.M. & Cooper R.A. 1992. The Webby B.D. 1984. Precambrian–Cambrian trace fossils Ordovician graptolite sequence of Australasia. from western New South Wales. Australian Journal of Alcheringa 16, 33–85. Earth Sciences 31, 427–437. VandenBerg A.H.M., Hendrickx M.A., Willman Webby B.D. 1988. The Ordovician genus Favistina Flower C.E., Magart A.P.M., Simons B.A. & Ryan S.M. and a related colonial coral from New South Wales, 1998. Benambra 1:100 000 map area geological report. Australia, pp. 139–152. New Mexico Bureau of Mines Geological Survey of Victoria Report 114. and Mineral Resources, Memoir 44. VandenBerg A.H.M., Nott R.J. & Glen R.A. 1991. Webby B.D. 1992. Ordovician island biotas: New South Bendoc 1:100,000 Map Geological Report. Geological Wales record and global implications. Journal and Survey of Victoria, Report 90. Proceedings of the Royal Society of New South Wales 125, VandenBerg A.H.M. & Stewart I.R. 1992. Ordovician 51–77. terranes of southeastern Lachlan Fold Belt: stratigraphy, Webby B.D. & Morris D.G. 1976. New Ordovician structure and palaeogeographic reconstruction. stromatoporoids from New South Wales. Journal and

Quarterly Notes 37 Proceedings of the Royal Society of New South Wales 109, Zhen Y.-y., Nicoll R.S., Percival I.G., Hamedi M.A. 125–135. & Stewart I. 2001. Rhipidognathid conodonts from – Webby B.D. & Packham G.H. 1982. Stratigraphy and Australia and Iran. Journal of Paleontology 75, 186 207. regional setting of the Cliefden Caves Limestone Group Zhen Y.-y. & Percival I.G. 2004a. Middle Ordovician (Late Ordovician), central-western New South Wales. (Darriwilian) conodonts from allochthonous limestones Journal of the Geological Society of Australia 29, 297–317. in the Oakdale Formation of central New South Wales. Webby B.D., VandenBerg A.H.M, Cooper R.A., Banks Alcheringa 28, 77–111. M.R., Burrett C.F., Henderson R.A., Clarkson P.D., Zhen Y.-y. & Percival I.G. 2004b. Darriwilian (Middle Hughes C.P., Laurie J., Stait B., Thomson M.R.A. & Ordovician) conodonts from the Weemalla Formation, Webers G.F. 1981. The Ordovician System in Australia, south of Orange, New South Wales. Memoirs of the New Zealand and Antarctica. Correlation Chart and Association of Australasian Palaeontologists 30, 153–178. Explanatory Notes. International Union of Geological Zhen Y.-y. & Percival I.G. 2006. Late Cambrian–Early Sciences, Publication No. 6. Ordovician conodont faunas from the Koonenberry Belt Webby B.D., Wang Q. & Mills K.J. 1988. Upper of western New South Wales. Memoirs of the Association Cambrian and basal Ordovician trilobites from western of Australasian Palaeontologists 32, 267–285. – New South Wales. Palaeontology 31, 905 938. Zhen Y.-y., Percival I.G. & Farrell J.R. 2003. Late White A.J.R. & Chappell B.W. 1989. Geology of the Ordovician allochthonous limestones in Late Silurian Numbla 1:100,000 Sheet 8624. Geological Survey of New Barnby Hills Shale, central western New South Wales. South Wales, Sydney. Proceedings of the Linnean Society of New South Wales Williamson P.L. & Rickards R.B. 2006. Eastonian 124, 29–51. (Upper Ordovician) graptolites from Michelago, near Zhen Y.-y., Percival I.G. & Webby B.D. 2003. Early Canberra. Proceedings of the Linnean Society of New Ordovician conodonts from far western New South South Wales 127, 133–156. Wales, Australia. Records of the Australian Museum 55, Willman C., Morand V.J., Haydon S.J. & Carney C. 169–220. 1999. Omeo map and geological report. Geological Survey Zhen Y.-y., Percival I.G. & Webby B.D. 2004a. Early of Victoria, Report 118. Ordovician (Bendigonian) conodonts from central Wilson C.J.L. 1969. The geology of the Narooma area, New South Wales, Australia. Courier Forschungsinstitut N.S.W. Journal and Proceedings of the Royal Society of Senckenberg 245, 39–73. New South Wales 101, 279–316. Zhen Y.-y., Percival I.G. & Webby B.D. 2004b. Wolf K.H., Flugel E. & Kemezys K.J. 1968. Ordovician Conodont faunas from the Mid to Late Ordovician calcareous algae from a bioherm, Blathery Creek boundary interval of the Wahringa Limestone Member Volcanics, New South Wales (Australia). Review of (Fairbridge Volcanics), central New South Wales. Palaeobotany and Palynology 6, 147–153. Proceedings of the Linnean Society of New South Wales 125, 141–164. Wopfner H. 1967 [imprint 1966]. Cambro-Ordovician sediments from the north-eastern margin of the Frome Zhen Y.-y. & Pickett J.W. 2008. Ordovician (Early Embayment (Mt. Arrowsmith, N.S.W.). Journal and Darriwilian) conodonts and sponges from west of Parkes, Proceedings of the Royal Society of New South Wales 100, central New South Wales. Proceedings of the Linnean 163–177. Society of New South Wales 129, 57–82. Wyborn D. 1992. Stratigraphy and geochemistry of Zhen Y.-Y. & Webby B.D. 1995. Upper Ordovician Ordovician volcanics from the Lachlan Fold Belt in conodonts from the Cliefden Caves Limestone central New South Wales. In: B.D. Webby & J.R. Laurie Group, central New South Wales, Australia. Courier eds. Global Perspectives on Ordovician Geology. pp. 495– Forschungsinstitut Senckenberg 182, 265–305. 497. Balkema, Rotterdam. Zhen Y.-Y., Webby B.D. & Barnes C.R. 1999. Upper Wyborn D. 1996. Geology, chemistry and gold/copper Ordovician conodonts from the Bowan Park succession, potential of the Temora belt and adjacent Gilmore central New South Wales, Australia. Geobios 32, 73–104. Fault System. In: Magmatic and hydrothermal evolution Zhuravlev A.Yu. & Gravestock D.I. 1994. of intrusive-related gold deposits in eastern Australia. Archaeocyaths from Yorke Peninsula, South Australia AMIRA project P425. and archaeocyathan Early Cambrian zonation. Young G.C. 2009. An Ordovician vertebrate from Alcheringa 18, 1–54. western New South Wales, with comments on Cambro- Ordovician vertebrate distribution patterns. Alcheringa 33, 79–89.

38 September 2011 Appendix Kenilworth Group (Pogson, in Pogson & Watkins 1998): now subsumed within the Cabonne Group Obsolete, redundant and rejected names (Pogson, in Pogson & Watkins 1998) as a result of for Cambrian and Ordovician units in NSW reassessment of stratigraphic relationships on the Dubbo 1:250 000 sheet (Meakin & Morgan 1999) and Goulburn Baroorangee Creek Subgroup (of Ponto Group): 1:250 000 sheet (Thomas et al. in press). briefly described by Buckley (2001) and in the legend to the 2nd edition Koonenberry 1:250 000 pre-Permian Kianga Basalt: now invalid, reinterpreted as blocks interpretation map (Stevens et al. 2002) – now of basalt within the Bogolo Formation overlying the

Baroorangee Creek Formation. Narooma Chert (Glen et al. 2004). Barrajin Group (Morgan, in Pogson & Watkins Malay Creek Formation: shown on provisional 1st

1998): now subsumed within the Cabonne Group edition of Gunning 1:100 000 geological map (Thomas

(Pogson, in Pogson & Watkins 1998) as a result of et al. 2001), this interbedded sandstone and black shale reassessment of stratigraphic relationships on the Dubbo unit occupies an identical stratigraphic position to the 1:250 000 sheet (Meakin & Morgan 1999) and Goulburn Sunlight Creek Formation, hence it is redundant. 1:250 000 sheet (Thomas et al. in press). Merrere Conglomerate Member: formalised by Beacons Hill Chert: distribution was shown on Scheibner and Basden (1998, p. 414) as a member of the provisional 1st editions of the Crookwell, Boorowa and Ballast Formation, this unit is now regarded as a basal Yass 1:100 000 geological maps, but this unit is now conglomerate of the Siluro-Devonian Cobar Supergroup regarded as an equivalent of the Nattery Chert Member of (Glen et al. 2010). the Abercrombie Formation, and is therefore redundant. Paddys Creek beds: part of Palgamurtie Subgroup Belah beds (of Ponto Group): part of Palgamurtie (obsolete) in the legend to the 2nd edition Koonenberry

Subgroup (obsolete) in the legend to the 2nd edition 1:250 000 pre-Permian interpretation map (Stevens et al. Koonenberry 1:250 000 pre-Permian interpretation map 2002); as discussed by Buckley (2001), probably a thrust (Stevens et al. 2002). repeat of what is now called the Grasmere Formation, hence obsolete. Bendee beds (of Ponto Group): part of Palgamurtie Subgroup (obsolete) in the legend to the 2nd edition Palgamurtie Subgroup (of Ponto Group): only Koonenberry 1:250 000 pre-Permian interpretation previously briefly described in map legends to map – now assigned to Grasmere Formation preliminary versions of the Koonenberry pre-Permian

(Greenfield et al. 2010). interpretation map (Stevens et al. 2002); now obsolete. Blue Rock Well Basalt, Blue Rock Well Phyllite, Blue Tallebung Group: Colquhoun, Hendrickx and

Rock Well Sandstone, Blue Rock Formation (of Ponto Meakin (in Colquhoun et al. 2005, p. 30) recommended Group): all previously part of Noonthorangee Subgroup suppression of the name Tallebung Group as the concept (obsolete) in legend to Koonenberry Pre-Permian of that unit (Trigg 1987) appeared to include strata of Interpretation Map (Stevens et al. 2002) – now included both Early to Middle Ordovician age (Wagga Group in Noonthorangee Formation (Greenfield et al. 2010). equivalents) and Late Ordovician age, indicated by the presence of probable Eastonian graptolites. Budgery Sandstone Member (of Girilambone Group): a heavily altered quartzite, mentioned in ‘Trelawney Beds’ (Philip 1966; Webby 1988): the legend of the Cobar 1:250 000 metallogenic map comprises clasts, predominantly limestone of Late (Gilligan et al. 1994), but never defined. Obsolete. Ordovician (Eastonian age), in the Early Devonian Drik Drik Formation of Crook (1961). Gum Creek Basalt (of Ponto Group): part of Noonthorangee Subgroup (obsolete) in the legend to ‘Uralba Beds’ (Hall 1975, Webby 1988, Furey- the 2nd edition Koonenberry 1:250 000 pre-Permian Greig 2000a): clasts, predominantly limestone of Late interpretation map (Stevens et al. 2002) – now included Ordovician and Early Silurian age, incorporated into in Noonthorangee Formation (Greenfield et al. 2010). Wisemans Arm Formation sensu Furey-Greig (2003b), now part of Glen Bell Formation (Brown 2009). Humbug Sandstone (Duggan & Scott, in Lyons et al. 2000): this name for thick-bedded sandstone and Wonominta Beds (Warris 1967): includes rocks quartzite facies within the Wagga Group on the Forbes now variously assigned by Greenfield et al. (2010) to the 1:250 000 sheet has now been suppressed in favour of Grey Range Group (of Neoproterozoic age), and Ponto, an expanded definition of the Clements Formation Warratta and Kayrunnera groups, and is therefore not (Hendrickx & Colquhoun, in Colquhoun et al. 2005). equivalent to the Wonnaminta Formation.

Quarterly Notes 39 Figure 5. Correlation of selected Cambrian and Ordovician rock units within New South DELAMERIAN OROGEN LACHLAN OROGEN NEW Wales. As well as showing in-situ formations, we indicate (with broad arrows) the former NAROOMA TERRANE ENGLAND stratigraphic positions of allochthonous blocks, now redeposited into younger sediments, to Million KOONENBERRY BELT ALBURY–BEGA TERRANE HERMIDALE MACQUARIE ARC OROGEN illustrate a ‘ghost’ stratigraphy important to elucidating the geological evolution of the state. years LOWER TERRANE Units that are predominantly carbonate (limestone and dolostone) are shown in blue, and SILURIAN 442 Margules 442 chert in tan. Group Bo 5 ??? HIRN. Bo 4 Akuna Bogolo Abbreviations: 445 Bo 3 Mudstone Jingerangle ??? ??? ??? ??? ??? ??? ??? ??? 445 ??? ??? Jingerangle Millambri Millthorpe Formation Formation Formation Angullong ??? Willandra Cheesemans Malachis Hill Formation Volcanics UNDILL. = Undillan Bo 2 ??? Dignams Wombin Formation ??? Siltstone Sandstone ??? Creek Formation Rockdale ??? BOLINDIAN Volcanics Gooandra BOOM. = Boomerangian 448 Bo 1 Formation 448 Gunningbland ??? Formation Malongulli Burranah ?? ? Ea 3–4 Volcanics Glen “Trelaw. PAYNTON. = Payntonian Fm. BaL Formation clasts Bell Beds” Warbisco Narooma  Fm. clasts DATSON. = Datsonian Bowan Park QL Canomodine VL 451 Ea 2 Shale unnamed Limestone Cliefden Oakdale ? Chert 451

KATIAN ? Limestone Forest Reefs CHEWT. = Chewtonian Warbisco limestone at Reedy Creek Caves BeL Forest Reefs Upper Formation (upper) Daroobalgie Barmedman Subgroup Limestone Volcanics Nine Mile Shale Group DL Volcanics

Bendoc Limestone Blayney

Acton Group Group Volcanics Bendoc Subgroup Volcanics HIRN. = Hirnantian Ea 1 Bendoc Volcanics Sofala Group EASTONIAN FHL

Shale Bendoc 454 UPPER ? Volcanics 454 Fm. = Formation Currawalla ??? Yuranigh L. M. Coomber Kiandra Group Watonga Gi 2 Shale Formation Lst. = Limestone Sunlight Ck ? Formation Temperance Congl. = Conglomerate 457 Formation Parkes Kenyu 457 Bumballa Fm. Mt Pleasant Byng Formation Volcanics Wahringa Basalt Member Volcanics GFM = Glen Fergus Member Gi 1 Formation Limestone ? GFM ? ??? ??? ???

Cabonne Group Cabonne Blueys Creek Mbr = Member Chakola Member Group Cabonne

460 GISBORNIAN Lower Fm. (Vic) 460 SANDBIAN Formation Volc Mbr = Volcanic Member Limestone Billabong Creek Blayney Goonumbla Volcanics Da 4 Nattery Doongala Northparkes Group Numeralla Mozart Whinfell Volcanics Yuranigh L M = Yuranigh Limestone Member Chert Chert Chert Chert 463 Member Chert Member Member ??? ?? 463 ?? ? Pittman Adaminaby DL, QL, & Bal (in Bowan Park Limestone Subgroup) = Daylesford Limestone, Quondong Weemalla Coombing

Cargo Volcanics Cargo Clasts of Cargo Volcanics Cargo 

Formation Volcanics Walli Group Da3

Group Formation Formation Limestone, and Ballingoole Limestone, respectively Volcanics Fairbridge Da 3 Ballast limestone 466 Adaminaby Formation Coombing 466 FH, Bel, & VL (in Cliefden Caves Limestone Subgroup) = Fossil Hill Limestone, Belubula Peach Tree Formation Haedon Chert Formation

Limestone, and Vandon Limestone, respectively DARRIWILIAN

DARRIWILIAN ??? Member ? (Vic) = (Victoria); "Trelaw." = "Trelawney" 469 Da 2 ??? 469 ??? ??? ??? ??? ??? ??? ??? ???

MIDDLE Da 1 YAPEEN- Ya 2 Gundara Abercrombie Clements IAN Ya 1 Quartzite ? ? 472 Formation Formation Group Wagonga 472 Ca 3–4 Member Wagga Group Wagga GIAN CASTLE- Pingbilly Fm. DAPIN- DAPIN- O R DO V I C A N Ca 2

MAIN- Girilambone Group IAN Ca 1 Adaminaby Mummel Group Adaminaby Mt. Dijou 475 Milby Chert Volc Mbr 475 Tabita Fm. Wheeney Group Chert CHEWT. Ch 1–2 Member Member

Pimbilla Pimbilla Kaiwilta Mbr Be 2–4 Creek Fm. undifferentiated Tank Group Tank Hensleigh Narrama 478 Rowena Formation Siltstone 478 Yandaminta ChertNarooma (lower) “Trelawney FLOIAN Be 1 Formation Quartzite Willigam Yarrimbah arenite” NIAN Sandstone Formation Mitchell 481 BENDIGO- Member 481 La 3 Budhang Formation Chert Nelungaloo La 2b Scropes ??? ??? ??? Volcanics Range 484 La 2a 484 Mutawintji Group Mutawintji Formation LOWER La 1b ? 487 ? 487 La 1a LANCEFIELDIAN Kayrunnera Group TREMADOCIAN WAREN- Bynguano 490 DIAN Kandie Tank 490 Quartzite Lst. DATSON. ??? Stage 10 Nootumbulla ? PAYNTON. Funeral 493 Sandstone Creek Lst. 493 Nuchea Nuchea Congl. Conglomerate Watties Bore Bilpa Stage 9 Formation Conglomerate 496 ??? 496 IVERIAN Easter Monday 499 PAIBIAN Cupala Creek Fm. 499

IDA- Formation Jeffreys Pipeclay Creek FURONGIAN MEAN Flat Fm. Formation ?

Hummock Fm. Group Clasts at

Boshy Warratta MINDY- Yancannia 502 Stage 7 ALLAN Williams Creek Formation Burrewarra 502 Conglomerate Fm. Point ?? ? BOOM. Morden Fm. Murrawong ? Creek Fm. 505 DRUM- UNDILL. 505 IAN Weinteriga Ck Fm. ? FLORAN. Wyarra Shale Grasmere Fm. TEMPLE- Noonthorangee Fm. Stage 5 Wydjah Fm. Ponto Koonenberry Fm. 508 TONIAN Coonigan Yandenberry Fm. 508 Rocky Beach ‘SERIES 3’ Group ORDIAN Formation Pincally Fm. Cannela Fm. Metamorphic ? Baroorangee Ck Fm. Melange 511 511 ? Port Macquarie TOYONIAN Serpentinite Cymbric C A M B R I N Stage 4 Vale Wonnaminta Fm. Group 514 Formation Gnalta Teltawongee Nundora Fm. 514 Group Bunker Ck Fm. BOTO- Depot Glen Fm. MAN Copper 517 Mount Mine 517 ??? Wright Range Volcanics Fm. ? ? 520 ‘SERIES 2’ 520 Stage 3 Mt. Wright– Mt. Arrowsmith Kayrunnera–Koonenberry region Bilpa–Comarto, Warratta + Cooma−Mallacoota Canberra– Goulburn region Oberon–Rockley Cargelligo Sussex–Byrock Junee–Narromine Marsden–West Nth Molong Bowan Park South of Cliefden Caves Cadia Forest Reefs– Blayney NE Molong Sofala–Dunedoo– Kiandra Volcanic Belt Narooma Tamworth–Nemingha Port Macquarie ATDAB- Mutawintji Scropes Range Tibooburra inliers region Queanbeyan Wyalong– Temora Volcanic Belt ‘Canomodine’ Junction Reefs Volcanic Belt Mudgee ANIAN 1 2 3 4 5 6 7 8 9 10 11 12 13 14 15 16 17 18 19 20 21 22 23 24 25 Quarterly notes Future papers: ‘Early Permian shell fossils of the Hunter Valley, New South Wales’ by N.S. Meakin, L. Sherwin, P.A. Flitcroft and I.G. Percival * * Index of Quarterly Notes from 101 to 136 * Available on DIGS: http://digsopen.minerals.nsw.gov.au. 101 1. Preliminary Palaeozoic bedrock interpretation of the Narromine and Nyngan 1:250 000 sheet areas 2. Palaeontology of drill hole DM Northern Parkes DDH 3 102 Stratigraphy, structure and mineralisation of the Mudgee 1:100 000 geological map sheet 103 Mineral deposits of the Glen Innes 1:100 000 map sheet area 104 1. Geology of the Cargelligo and Narrandera map sheet areas: removing the cover using Discovery 2000 geophysics 2. Geology and sand resources of the Stockton Bight–Port Stephens area 105 A re-appraisal of the Darling Basin Devonion sequence 106 A comparative study: Calc-silicate ellipsoids from Broken Hill and diagenetic carbonate concretions from the Sydney Basin 107 1. Controls on opal localisation in the White Cliffs area 2. The age of the Nandilyan and Narragal limestones, Molong high, Central Western New South Wales 108 1. Late Ordovician biostratigraphy of the northern Rockley–Gulgong volcanic belt 2. Ordovician stratigraphy of the northern Molong volcanic belt: new facts and figures 109 DIGS — Digital Imaging of Geological System, an interactive database for the mineral industry 110 Age constraints on strata enclosing the Cadia and Junction Reefs ore deposits of central New South Wales, and tectonic implications 111 Peel Discovery 2000 Geophysics — providing keys to exploration in the western New England region of New South Wales 112 An internet information delivery vehicle for the resources industry — DIGS on the Net 113 Volcanic Textures in the Palaeoproterozoic Hores Gneiss, Broken Hill, Australia 114 Peel South Exploration NSW geophysics — interpretation of new data for exploration and geological investigations in the western New England area of New South Wales 115 New geochronology from the Coolah–Mendooran area: evidence for Middle Jurassic erosion in the southern Surat Basin 116 Mineral deposits and models, Cootamundra 1:250 000 map sheet area 117 1. Definition of the Brawlin Formation, Cootamundra area, New South Wales 2. Sulphur and lead isotope studies for the Cargelligo 1:250 000 map sheet area 118 Murray–Riverina region: an interpretation of bedrock Palaeozoic geology based on geophysical data 119 The Willyama Supergroup in the Nardoo and Mount Woowoolahra Inliers 120 40Ar/39Ar geochronology of the Tara intrusion-related base metal deposit: implications for metallogenesis in the central Lachlan Orogen 121 Inverell Exploration NSW geophysics — new data for exploration and geological investigations in the northern New England area of New South Wales 122 The Fox Tor Diorite, a newly recognised intrusion within the New England Batholith, northern New South Wales 123 Cainozoic igneous rocks in the Bingara to Inverell area, northeastern New South Wales 124 Evaluation of mineral resources of the continental shelf, New South Wales 125 A Middle Triassic age for felsic intrusions and associated mineralisation in the Doradilla prospect area, New South Wales 126 Geological units of the Port Macquarie–Tacking Point tract, north-eastern Port Macquarie Block, Mid North Coast region of New South Wales 127 Volcanic arc-type rocks beneath cover 35 km to the northeast of Bourke 128 Mineral Systems and Processes in New South Wales: a project to enhance understanding and assist exploration 129 Deep structure beneath the Murray Basin from teleseismic tomography 130 The Siluro-Devonian geological time scale: a critical review and interim revision 131 The newly defined Glen Bell Formation, and a reappraisal of the Wisemans Arm Formation, Halls Creek district, northern NSW 132 Mineral systems of the Murray Basin, New South Wales 133 Contrasting age and isotope characteristics of volcanic-hosted and skarn-type mineralisation near The Glen, Goulburn, in the Lachlan Orogen, New South Wales 134 A revised Triassic stratigraphy for the Lorne Basin, NSW 135 Phoenix: an Early Devonian granite-related tungsten deposit from the eastern Lachlan Orogen, New South Wales 136 Fossil microbes in opal from Lightning Ridge — implications for the formation of opal

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