Revisions to Geological Maps in the Southern Part of the Dial Range/Fossey Mountain Trough, Northern Tasmania, with Emphasis on Cambrian Geology

Home , Blackberry Hill, Greywacke, Mount Read (Tasmania), Sticht Range

Tasmanian Geological Survey Record 2008/01

Revisions to geological maps in the southern part of the Dial Range/Fossey Mountain Trough, northern Tasmania, with emphasis on Cambrian geology

by M. J. Vicary

DepartTasmanianment o fGeological Infrast Surveyructu Recreord, E n2008/01ergy and Resources 1 Mineral Resources Tasmania Mineral Resources Tasmania PO Box 56 Rosny Park Tasmania 7018 Phone: (03) 6233 8377 l Fax: (03) 6233 8338 Email: [email protected] l Internet: www.mrt.tas.gov.au Contents

Introduction ……………………………………………………………………………… 4 Montana/Deloraine map sheets …………………………………………………………… 5 Gog map sheet …………………………………………………………………………… 6 Sheffield map sheet ………………………………………………………………………… 7 Wilmot map sheet ………………………………………………………………………… 9 Cethana map sheet ………………………………………………………………………… 10 Conclusions and implications for mineralisation ……………………………………………… 12 References ………………………………………………………………………………… 15

Figures

1. Index map of 1:25 000 scale map sheets, northern Tasmania………………………………… 4 2. Middle and Late Cambrian biostratigraphic correlation chart ……………………………… 8 3. Provisional stratigraphic correlation chart for correlates of the Mt Read Volcanics in northern Tasmania …………………………………………………………………… 9 4. Cambrian stratigraphy and mineralisation in the Castra–Gog area ………………………… 13 5. Simplified geology of the Cethana–Gog area ……………………………………………… 14

While every care has been taken in the preparation of this report, no warranty is given as to the correctness of the information and no liability is accepted for any statement or opinion or for any error or omission. No reader should act or fail to act on the basis of any material contained herein. Readers should consult professional advisers. As a result the Crown in Right of the State of Tasmania and its employees, contractors and agents expressly disclaim all and any liability (including all liability from or attributable to any negligent or wrongful act or omission) to any persons whatsoever in respect of anything done or omitted to be done by any such person in reliance whether in whole or in part upon any of the material in this report.

Tasmanian Geological Survey Record 2008/01 3 Introduction constrain the interpretation. The extensive thin section collection at Mineral Resources Tasmania proved This report documents revisions to six 1:25 000 scale invaluable when detailed descriptions were not digital geological maps in the Deloraine to Cethana documented in the original source. area. The project forms part of the four-year Tasmanian Government funded TasExplore Project, Several new provisional stratigraphic units have been which aims at advancing mineral exploration in introduced. These units are informally defined and northern Tasmania by producing a refined 3D model have been indicated by the use of lower case in the for the region based on the integration of new lithostratigraphic descriptor (e.g. Groove Creek geological mapping and additional geophysical formation, Riana subgroup). Existing stratigraphic studies. The review of existing data in the Deloraine to nomenclature as defined in the Geoscience Australia Cethana area was made as part of a regional mapping Stratigraphic Units Database (e.g. Gog Range program aimed at the re-examination of the Lower Greywacke, Tyndall Group) is capitalised. Although Palaeozoic stratigraphy and structure in the Dial the term Western Volcano-Sedimentary Sequence has Range–Fossey Mountains region in late 2006 to June not been formally defined in the Geoscience Australia 2007 (fig. 1) and includes new work by C. Calver, Stratigraphic Units Database, it is used in this report as J. Everard, D. Green, M. McClenaghan, D. Seymour it is a current and commonly used stratigraphic term in and this author. The results of the regional mapping western Tasmania (Corbett, 2002). The term Sprent program and this review will be integrated in a conglomerate is used to describe parts of the Gog planned project aimed at the revision of the 3D geological model of Tasmania in 2009–2010. Revised Range Greywacke that are mainly derived from Late digital geological maps will be available in late 2008. Neoproterozoic–Early Cambrian protoliths. The 1:25 000 rock code mnemonics documented Many of the geological observations presented in this throughout the text, are those used in the legends on report have not been confirmed by the author and the revised maps. information from a wide variety of sources (unpublished field mapping, thin sections, published The conclusions of this report remain at best mapping, company reports, University theses, and preliminary, pending additional mapping and published and unpublished papers) was used to geochemical evaluation.

5 460 000 mN

PORT STOWPORT ULVERSTONE DEVONPORT SORELL 5 440 000 mN

RIANA KINDRED LATROBE HARFORD

WEST LOYETEA CASTRA RAILTON FRANKFORD 5 420 000 mN

LOONGANA WILMOT SHEFFIELD PARKHAM

LEA CETHANA GOG DELORAINE 5 400 000 mN

PENCIL PINE LIENA MOLE CREEK MONTANA

5 380 000 mN E E E E m m m m

0 0 0 0 0 0 0 0 0 0 0 0

0 0 0 0 2 4 0 6 4 4 4 4 Figure 1 Index map of 1:25 000 scale map sheets in northern Tasmania showing maps revised in this study in green. Other maps updated during TasExplore Project are shown in yellow.

Tasmanian Geological Survey Record 2008/01 4 Montana/Deloraine map sheets no obvious pyroxene crystals. It is similar to other (Vicary, 2008a; Vicary 2008b) felsic crystal-rich volcaniclastic sandstone units interbedded within the Gog Range Greywacke Descriptions of the Cambrian sequence in the (Ódsvgv), and may not be the lateral continuation of Deloraine–Montana area are given in Pike (1973), the basal Tyndall marker horizon as suggested by Pike. Barton et al. (1969), Wells (1957), Herrmann (1991) and Andesitic lavas/intrusive rocks occur within the Gog Woodward et al. (1993), and these references form the Range Greywacke at Kentish Hill. These are basis for the following discussion. lithogeochemical equivalents of the Beulah andesite The Cambrian sequence consists of interbedded (Herrmann, 1991), although on the map they are micaceous greywacke, siltstone, shale, siliceous designated Óda rather than Ódta as their stratigraphic conglomerate and volcaniclastic sedimentary rocks correlation is uncertain. Mapping by Herrmann (1991) with minor felsic–intermediate lava/intrusive units. suggests that the andesitic unit at Kentish Hill occurs in the core of a syncline. It is tentatively suggested that The bulk of the Cambrian sequence represents the the andesite may be at the same stratigraphic level as along-strike continuation of similar units that outcrop the Tyndall correlates near Pumicestone Ridge, in the Gog–Sheffield area and is correlated with the although additional detailed mapping and Gog Range Greywacke of the Western geochemistry is needed to confirm this. Volcano-Sedimentary Sequence. Internal subdivision within the Gog Range Greywacke is based on the An epidote-altered tholeiitic basalt occurs at the relative abundance of coarse siliceous (Proterozoic faulted contact between the andesite sequence and the derived) conglomerate facies and on the relative Gog Range Greywacke. This is considered to represent abundance of the felsic volcanic component (quartz- a structurally emplaced slice of Neoproterozoic–Early feldspar crystals and glass shards/pumice fragments). Cambrian basement, and is tentatively correlated with Geological maps of the Gog Range Greywacke in the the Motton metabasalt (Crawford, in Herrmann, 1991). Deloraine–Montana area by Barton et al. (1969) and Tholeiitic basalts also occur in a similar structural Herrmann (1991) show marked differences in the position in the Gog Range area (Herrmann, 1991; internal subdivision, and many of the mapped units McClenaghan et al., 2001). are probably gradational. Original field maps for the The Wurawina Supergroup unconformably overlies Quamby one inch to one mile (1:63,360 scale) map Proterozoic basement and the Cambrian sequence in show that much of the mapped distribution of the Flinty Rock–Native Hop Hill area, although the conglomerate facies (Ódsvgc) consists of interbedded contact relationships are highly modified by later greywacke, lithic greywacke and siltstone with faulting. The structural interpretation of Woodward et discontinuous lenses of siliceous conglomerate. This al. (1993) has been added to the map. This includes sequence is gradational to the siltstone-dominated thrust faulting at the contact between the Wurawina facies (Ódsvg) and has an exaggerated distribution on Supergroup and the Proterozoic units on Native Hop the current map sheets. Units within Ódsvg that are Hill and between the Wurawina Supergroup and rich in felsic volcanic detritus have been designated Cambrian rocks near Flinty Rock. The thrust on Native Ódsvgv. Hop Hill may continue west and cut Long Ridge at a low angle to the apparent strike. This accounts for the A distinctive crystal-rich volcaniclastic sandstone (the apparent thickening of the Wurawina Supergroup ‘marker horizon’ of Pike, 1973) crops out to the south of correlates on the eastern end of Long Ridge. Pumicestone Ridge. Two samples collected by Marshall (66/40 and 68/169) are feldspar-quartz- The Wurawina Supergroup correlates in the Flinty pyroxene phyric volcaniclastic sandstones which are Rock–Native Hop Hill area were described by Wells petrologically similar to pyroxene phyric (1957) who established the following sequence: volcaniclastic units which define the base of the Tyndall Group in the Gog–Sheffield–Cethana area. Gordon Limestone ~ 300 m The volcaniclastic sandstone is overlain by a Caroline Creek Sandstone ~ 300 m mixed-provenance volcaniclastic conglomerate Owen Conglomerate ~ 90 m sequence with interbedded extrusive/intrusive The interpretation of Wells (1957) has been added to rhyolite/dacite bodies. A chemical analysis the map although his stratigraphic correlations have (Herrmann, 1991) suggests that these bodies can be been modified. The unit correlated by Wells with the correlated with the high Zr Minnow Keratophyre in Caroline Creek Sandstone contains Tritoechia careyi, a the Gog–Sheffield area. Both the crystal-rich sandstone fossil that is currently placed in the upper part of the and the overlying conglomerate sequence have been Owen Group in the Florentine Valley Mudstone tentatively correlated with the Tyndall Group on the (Laurie, 1996). This unit has been correlated with the maps. Owen Group (ÓOsu on the map) following the Pike (1973) reported that the ‘marker horizon’ can be stratigraphy determined by recent mapping in the traced westward to about one kilometre south of Railton–Sheffield area by C. Calver (Calver et al., 2008). Beefeater Hill. Sample 69/102, from this location, is a In the Native Hop Hill area, ÓOsu overlies a basal quartz-feldspar phyric volcaniclastic sandstone with conglomerate that is correlated with the Roland

Tasmanian Geological Survey Record 2008/01 5 Conglomerate (ÓOcr). No definitive Moina Sandstone can be traced from the hinge of the Gog syncline to the lithologies have been recorded in the Deloraine– Firetower prospect and Upper Minnow River areas Montana area although because of the limited (Callaghan, 2002). An important result of this study is mapping, it is possible that the upper parts of ÓOsu that the mineralisation at the Firetower prospect is unit may include some Moina Sandstone correlates. hosted in the upper parts of the Gog Range Greywacke Subdivision of Owen Group and Gordon Group close to the contact with the overlying Tyndall Group. correlates in the Needles Ridge–Long Ridge area Quartz-feldspar phyric pumiceous volcaniclastic units remains unresolved. also occur in the Western Volcano-Sedimentary Sequence, although these contain no detrital pyroxene The presence of a basal conglomerate horizon (ÓOcr) crystals or andesitic detritus. in the Native Hop Hill area implies that although the contact with the underlying Proterozoic rocks has been Both the Tyndall Group and the underlying Western modified by later thrusting (Woodward et al., 1993), Volcano-Sedimentary Sequence are intruded by the the amount of movement associated with this fault Minnow Keratophyre and in places, such as on the need not be great. Similarly the greywacke and eastern side of Kenzies Hill, the Tyndall Group conglomerate-rich facies of the Gog Range Greywacke correlates are stoped out by the intrusion. The Minnow contain a high proportion of quartz-muscovite schist Keratophyre has been recoded as Óqfpz to distinguish and micaceous quartzite clasts, also implying local it from other quartz-feldspar porphyry bodies in the derivation from Proterozoic rocks. Mount Read Volcanics. It has a highly variable Three discontinuous outcrops of possible Caroline phenocryst assemblage of quartz-feldspar ± pyroxene Creek (Moina Sandstone) correlates have been ± hornblende ± biotite and is characterised by high mapped in the Stockers Plain area near 470 000 mE, zirconium contents (typically 300–600 ppm). Similar 5 393 700 mN (Wells, 1957; Barton et al., 1969). These high Zr rhyolite/dacite units occur in the Sock Creek have been shown on the current maps as area (Barwick, 1991) and at Jukes Proprietary (Doyle, 1990). Undifferentiated Cambrian–Ordovician (ÓO), although a potential correlation with either the Eldon Several felsic porphyry bodies that intrude the Group or a sandstone facies of the Gordon Limestone Western Volcano-Sedimentary Sequence to the south (e.g. Mole Creek Formation) is also likely. An of the Firetower prospect and near Minnow Falls have alternative explanation for these occurrences is that been recoded Óqfbp on the basis of their high biotite they may be Tertiary silcrete deposits (S. Forsyth, pers. content (Callaghan, 2002). Three quartz-feldspar comm., 2007). bodies in the Lower Beulah area have been removed The Permian geology at Quamby Brook (near from the map. 476 000 mE, 5 397 000 mN) has been updated following A major revision to the map is the reinterpretation of Moore (1971). the contact between the Beulah andesite and the Gog Gog map sheet Range Greywacke to the south of the Lower Beulah (McClenaghan et al., 2008) Barite prospect. South of the Lower Beulah Barite prospect, correlates of the Gog Range Greywacke dip Descriptions of the Cambrian sequence in the Gog area and face south and seem to overlie the Beulah andesite. are given in Herrmann (1991) and McClenaghan et al. Mapping and core logging by previous workers has (2001). Although no explanatory report on the latter suggested that this contact is conformable and work has been published, an extensive collection of possibly interfingering (Rand and Noonan, 1989; thin sections and original field maps and notes is Corbett and McClenaghan, 2003), although Porter available at Mineral Resources Tasmania. The (1973) favoured a faulted contact. A review of data Cambrian sequence in the Gog area is also discussed in from the adjacent Sheffield map suggests that the Corbett and McClenaghan (2003) and Callaghan western contact between the Gog Range Greywacke (2002). and the Beulah andesite is conformable, with the Beulah andesite overlying the Gog Range Greywacke. A review of thin sections collected during field A thin unit of rhyolitic–andesitic volcaniclastic mapping in the Gog area (McClenaghan et al., 2001) sandstone (with minor pyroxene phyric andesitic has shown that several discontinuous outcrops of volcaniclastic sandstone) occurs at the contact and is feldspar-pyroxene phyric andesitic volcaniclastic petrologically equivalent to similar units developed in sandstone are interbedded with a regionally extensive the basal Tyndall Group in the Cethana, Roland and unit of quartz-feldspar phyric pumiceous Gog areas. This suggests that the Beulah andesite is the volcaniclastic sandstone that outcrops in the core of the stratigraphic equivalent of the Dasher andesite and is Gog syncline. The andesitic units are petrologically age-equivalent to the Tyndall Group. similar to other andesitic volcaniclastic sandstones at the base of the Tyndall Group in the Sheffield–Roland Diamond-drill hole DD84BB4 (Dickson, 1992), drilled area, and suggest that this sequence can be correlated through the contact between the Gog Range with the Tyndall Group in contrast to a previous Greywacke and the Beulah andesite near the Lower interpretation which placed these units in the Western Beulah Barite prospect, was reviewed as part of an Volcano-Sedimentary Sequence. This package of rocks additional study (Vicary and Seymour, in prep.), and

Tasmanian Geological Survey Record 2008/01 6 is summarised below. In general the hole was collared Sheffield map sheet in a south-dipping and facing sequence of fine (Calver et al., 2008) greywacke and siltstone correlated with the Gog Range Greywacke. Between 51 and 64 m, the core was The lowest stratigraphic unit exposed in the Sheffield strongly broken and a fault zone was interpreted at area is the Gog Range Greywacke (McClenaghan, approximately 57.3 m. Below the fault, there is a 2004). There has been little internal subdivision of this pronounced change in lithology with abundant unit to date and no Sprent conglomerate has been andesitic to dacitic? lavas and re-sedimented identified. A conglomerate horizon (Ódsvgc) in the hyaloclastite breccias with interbedded thinly bedded Beulah Heights area is predominantly derived from black siltstone. Rand (1990) reported that quartz Proterozoic rocks (mainly quartzite and micaceous phyric rhyolitic volcaniclastic sandstone may also schist) and contains a component of chert. occur within this sequence. The black siltstones have been previously correlated with the Gog Range The Gog Range Greywacke is overlain by the Tyndall Greywacke sequence, however they are now Group in the Paradise area. The lowest units of the considered to be part of a package of volcaniclastic Tyndall Group are internally complex and have been sedimentary rocks and lavas which occurs at a high designated Ódtsc, Ódtvs, Ódtca and Ódtsa. This stratigraphic level within the Beulah andesite. A subdivision reflects either a change in provenance or re-interpretation of the drill hole and local surficial grain size, although the units are commonly mapping (Rand, 1990) suggests that the faulted contact gradational and interbedded. Ódtsc is a siliceous between the Beulah andesite and the Gog Range conglomerate-rich facies mainly derived from a Greywacke dips at a steep angle to the south-south Proterozoic source. Ódtvs is principally a west. The stratigraphic correlation of the Beulah volcaniclastic sandstone facies derived from andesitic andesite (see Sheffield section) with the Tyndall Group and rhyolitic sources, and is possibly a lateral suggests that there is significant reverse movement on equivalent of Ódtp on the Gog sheet. Volcaniclastic the fault. facies principally derived from andesitic sources have Andesitic to dioritic rocks are common within the Gog been designated Ódtca or Ódtsa depending on the Range Greywacke south of the fault contact and field dominant grain size of the unit (i.e. conglomerate or evidence suggests they are largely intrusive. A large sandstone respectively). dioritic intrusion has been mapped in Garden of Eden Late Middle Cambrian fossils have been reported from Creek at 452 100 mE, 5 407 750 mN. Andesitic intrusive the Paradise area (Jago, 1989; Laurie et al., 1995) and rocks have also been identified in the Lower Beulah have been correlated with the Tyndall Group (Corbett, Barite adit (Rand, 1990). 2002; Corbett and McClenaghan, 2003). A review of The Western Volcano-Sedimentary Sequence in the data from the Paradise area (Rand, 1989; Gog Range area is a highly variable sequence of McClenaghan, unpublished data) suggests that the interbedded greywacke, siltstone, siliceous fossils occur in a discontinuous micaceous siltstone conglomerate and quartz-feldspar phyric pumiceous horizon that is underlain by a poorly defined unit of volcaniclastic sandstone and siltstone, with minor quartz-feldspar phyric pumiceous volcaniclastic mixed provenance volcaniclastic sandstones and sandstone. A poorly-defined sequence of interbedded dacitic to rhyolitic lavas. feldspar-quartz ± hornblende ± pyroxene phyric crystal-rich volcaniclastic sandstone and feldspar ± Five point occurrences of chert and basalt-rich biotite phyric lava overlies the fossiliferous siltstone lithicwackes (Ódsvgs) have been added to the map in horizon. In contrast to the above stratigraphic the Mersey River area. These are compositionally and correlation, which places the entire sequence into the texturally similar to lithologies from the Sprent Tyndall Group, it is tentatively suggested that the conglomerate that outcrops extensively towards the fossiliferous siltstone and underlying rhyolitic upper parts of the Western Volcano-Sedimentary pumiceous volcaniclastic sandstone occur in the upper Sequence in the Dial Range area. In contrast to the parts of the Gog Range Greywacke. The overlying greywacke and interbedded pebbly sandstone facies, andesitic volcaniclastic sandstone and lavas are which are derived from Proterozoic Tyennan correlates of the Tyndall Group. protoliths, these occurrences are sourced from dominantly Neoproterozoic–Early Cambrian Fossils from the Radfords Creek Group in the lithologies. Sugarloaf Gorge area (Kindred map) are similar in age to the Paradise fossils (Jago, 1989; Laurie et al., 1995). Other changes include minor revision to the Cambrian Previous workers (Corbett, 2002; Corbett and geology in the Beaumonts Road area and to the McClenaghan, 2003) have correlated the Radfords Wurawina Supergroup correlates in the Punchs Terror Creek Group with the Tyndall Group, however on the area based on a review of original mapping and thin basis of the above observation and field relationships it sections collected by D. C. Green. is suggested that the Radfords Creek Group is likely to The Wurawina Supergroup correlates near Dynans represent the upper stratigraphic part of the Gog Bridge have been recoded following mapping on the Range Greywacke (fig. 2, 3). It is apparent from the adjacent Sheffield map by C. R. Calver in 2007. fossil evidence that deposition of the Gog Range

Tasmanian Geological Survey Record 2008/01 7 WESTERN NORTHERN TASMANIA TASMANIA ) ) 1 ) d 3 p 5 a 1 W

k u ) , ( ( o

a o r 1 2 r e e e ( ( R e

i g g g P t k d d r r b T

n n a a o o s i u i k o o e o S L c G G

n r l R R P t a f f i k l

t r e a a c e e a a a M n v T l l

i s o o o

n i l l w t e u u e l r r e R l e d s h a

d d a a a t v d e i a n e n n t t m r g g u V a

a u a a a i a r o a u u t o s s I I C P S S R N S Q S C C S. diloma N A

I E. sentum

E IDAMEAN R

T P. cryptica B A L M G. reticulatus A G. stolidotus C MINDYALLAN C. quasivespa I I I

a E. eretes t a

g D. torosa – A. janitrix i I I v

e H. arepo a l

BOOMERANGIAN .

L P. agra I P. cassis G. (G.) nathorsti N A I R

B UNDILLAN D. deltoides M A

C P. punctuosus

E L

D E. opimus D I

M LATE TEMPLETONIAN– A. atavus FLORIAN T. gibbus

ORDIAN–EARLY X. templetonensis – R. chinensis TEMPLETONIAN

LEGEND Tyndall Group

Tyndall Group (Comstock Andesite) e c - n o Gog Range Greywacke/Southwell Subgroup e n u a q c e l o Groove Creek formation S

V y

r n a r Que River Shale t e n t e s e m Isandula formation i W d e s Figure 2 Middle and Late Cambrian biostratigraphic correlation chart for northern and western Tasmania (modified from Laurie et al., 1995).

Greywacke in the Dial Range area continued during phyric andesitic volcaniclastic sedimentary rocks at the andesitic volcanism that defines the Tyndall Group the contact between the Gog Range Greywacke and the in the Sheffield–Gog area. Beulah andesite in the same area. The contact between the Gog Range Greywacke and Beulah andesite in the Geological mapping in the Paradise area (Rand, 1989) Beulah area requires additional mapping, as parts of shows marked divergence from the interpretation the Gog Range Greywacke may in fact be Tyndall presented on the Sheffield map (McClenaghan, 2004). Group. Given the stratigraphic importance of the Paradise fossils, additional mapping in the area is strongly The geology in the Beulah area has been updated with recommended. additional information from Vicary and Jackson (1993). This includes some modification to the western Thin sections of two samples (MR38 and MR40), margin of the Beulah andesite. A more detailed review collected from the Gog Range Greywacke near the of the geology and stratigraphic relationships in the western margin of the Beulah andesite in the Beulah area will be given in an additional report Beulah–Golden Gate area, show that the rocks are (Vicary and Seymour, in prep.). pyroxene phyric andesitic volcaniclastic sandstones The Lizard Hill porphyry is part of the Minnow which are petrologically identical to units associated Keratophyre and has been recoded Óqfpz. with the basal Tyndall Group in the Roland–Gog area. They have been indicated on the map as two minimum Polymict volcaniclastic conglomerate (Ódtc), mainly polygons of Ódtsa. Rand (1989) also reports pyroxene derived from Tyndall Group and older Cambrian Tasmanian Geological Survey Record 2008/01 8 Dove River–Bull Creek Beulah–Winterbrook Native Track Tier Castra–Dial Range St Valentines Peak area area area area area

t Riana subgroup? ? n l p u a u ? i t o a r l r Native Track St Valentines e t G F u b

Patrick Creek Riana l l a a

k Tier Peak a m L F Dykes? sequence d e

n sequence sequence a e y a r T t C t C e

i y ? ? r N l l ? i e p p n H n u u i

o i t o o

g Winterbrook h r r a a c

Z sequence a G G m

r l l g M i o l l Z F a a d d ? n n r a

i Lake l e y y u b T T Barrington J

m t

e volcanics M M d r r Gog Range e o e f Bull Creek b Dasher e

h Greywacke c

Gog Range l m n c

Formation andesite n e d n Greywacke (Radfords a e i y d M r i L Creek Group) u b q M

e m e

Back Peak S a t e

a c y

Beds Gog Range C r n L a e e

Greywacke t c u Sticht Range n n q e e

Beds e m u i S

q d y e e r S a

Alma S

t - c n o

i formation r e n y a m h i c l P d - o e

z Groove V t

S r -

Creek n a o r u e n formation t a Q s

c l e n r o W e V

t n s n a e r i a Isandula l r e E d t formation b s d i e m a M W C

Figure 3 Provisional stratigraphic correlation chart for correlates of Mt Read Volcanics in northern Tasmania. sequences, unconformably overlies the Western andesitic detritus (pyroxene crystals and andesite Volcano-Sedimentary Sequence in the Vinegar Hill– clasts). Blackberry Hill area. It is tentatively correlated with the Zig Zag Hill Formation. Poorly exposed quartz A relatively thick sequence of predominantly rhyolitic phyric volcaniclastic conglomerate with well rounded volcaniclastic sedimentary rocks underlies a sequence clasts up to 30 cm has been reported near 450 000 mE, of andesitic volcaniclastic sedimentary rocks to the 5 411 500 mN (Vicary and Jackson, 1993) and may be north of the Billet Creek Fault (near 432 000 mE, part of the same sequence. 5 415 000 mN). Previous work has correlated this sequence as part of the Tyndall Group, based on the Wilmot map sheet correlation of a siliceous conglomerate at the base of the sequence with a similar siliceous conglomerate at (McClenaghan, Green and Vicary, 2008a) the Tyndall Group contact in the Smiths Road area. As siliceous conglomerate horizons can occur at several Correlates of the Gog Range Greywacke crop out stratigraphic levels within the Western extensively in the Nowhere Else–Roland area Volcano-Sedimentary Sequence and in the overlying (McClenaghan and Green, 1997). The sequence is Tyndall Group, they have little use as regional largely undifferentiated and although no Sprent stratigraphic markers. conglomerate lithicwacke has been mapped, chert and basalt-rich lithicwacke occurs immediately to the In contrast to the previous interpretation, the rhyolitic north on the adjacent Castra map (Vicary and volcaniclastic sequence underlying the basal Tyndall McClenaghan, 2007). Siliceous conglomerate Group andesitic volcaniclastic sequence has been horizons, derived mainly from Proterozoic sources, correlated with the felsic volcaniclastic facies of the occur at several stratigraphic levels within the Gog Gog Range Greywacke (Ódsvgv). This sequence hosts Range Greywacke (Ódsvgc) and are also interbedded chalcopyrite-galena-sphalerite veining at the Lake within the overlying Tyndall Group sequence (Ódtsc). Barrington prospect. Detailed mapping at the Lake Although a siliceous conglomerate horizon is present Barrington prospect (MacDonald, 1993) has shown in places at the base of the Tyndall Group, its utility as a that the sequence is considerably more variable than stratigraphic marker horizon is poor and definition of indicated on the current map and consists of the Tyndall Group is based on the occurrence of interbedded quartz-feldspar phyric lavas and

Tasmanian Geological Survey Record 2008/01 9 hyaloclastic breccias, quartz-feldspar phyric Several bodies of rhyolite lava and breccia within the fine-grained to coarse-grained volcaniclastic sequence at Andersons Road have been recoded as sediments with minor black siltstone, feldspar phyric diorite/andesite (Ódaid) following a review of thin intrusive rocks and feldspar-quartz ± hornblende sections. The relationship between Ódaid and the phyric lavas. It is a possible correlate of the sequence tholeiitic Lake Barrington diorite (Ódid) (Poltock, which hosts the Cethana alteration zone and possibly 2002; Corbett and McClenaghan, 2003), which occurs the Bell Mount sequence. The significance of this within the Andersons Spur sequence near Wilmot, correlation is that it places the Cethana alteration zone remains unresolved. The Late Cambrian sequence in and the Lake Barrington prospect at the same the Native Track Tier area (Riana subgroup) has a stratigraphic level, although the mineralisation at the distinctly tholeiitic character (Berry et al., 1997). It is Lake Barrington prospect is probably Devonian. tentatively suggested that the Lake Barrington diorite may represent part of the Late Cambrian Riana The apparent asymmetric stratigraphic succession subgroup. within the Gog Range Greywacke across a north–south fault in the Promised Land area is suggestive that this A small body of quartz melasyenite (Ksm) fault may have been an active structure during outcropping in the Shackley Hill area is Cambrian volcanism and sedimentation. petrographically similar to the diorite/andesite rocks (Ódaid) from the Wilmot area and is probably Southwest of the Billet Creek Fault there is a thick Cambrian in age. sequence of Tyndall Group correlates which comprise a basal sequence of andesitic lavas and volcaniclastic The Cambrian sequence in the Bell Mount area has sediments (Dasher andesite) with an overlying been correlated with the felsic volcanic-rich portion of variable sequence of rhyolitic volcaniclastic the Gog Range Greywacke (Ódsvgv). This is discussed sedimentary rocks and rhyolitic to dacitic lavas (Lake in more detail in the following section. A Barrington volcanics). The rhyolitic volcaniclastic predominantly greywacke sequence to the north of a sequence is probably a lateral equivalent of the unit quartz-feldspar porphyry body in the Wilmot River Ódtss which possibly overlies the Dasher andesite on (near 424 000 mE, 5 411 000 mN) is probably part of the the northern slopes of Mt Roland. A review of thin Bell Mount sequence, and has been included within sections from the Roland area suggests that much of the Bell Mount sequence rather than Tyndall Group as the sequence designated Ódtsa is mostly coherent shown on previous maps (Pemberton and Vicary, andesite with subordinate volcaniclastic units. 1989).

A chemically distinct dacite lava (Ódtld) outcropping Cethana map sheet in the Lake Barrington area has high zirconium (McClenaghan, Green and Vicary, 2008b) contents and is probably an extrusive phase of the Minnow Keratophyre (Óqfpz) which crops out The Cambrian sequence on the Cethana map can be extensively in the Gog–Sheffield area. subdivided into two main associations that are The Cambrian sequence in the Nietta–Wilmot area is spatially separated by a zone of strong faulting poorly known (McClenaghan and Green, 1997). A (Machinery Creek Fault) in the Mt Claude area. review of original data collected by D. C. Green in 1996 The sequence immediately north of the Machinery has been undertaken and some generalised Creek Fault consists of quartz-feldspar phyric observations can be made. volcaniclastic sedimentary rocks and rhyolitic lava with interbedded siliceous sandstone, greywacke and Recent mapping on the adjacent Castra map sheet has sandstone and conglomerate with a mixed volcanic shown that the bulk of the sequence in this area can be and Proterozoic provenance (Hicks, 1989; correlated with the Gog Range Greywacke. A McClenaghan and Green, 1999). Rare granitic rocks structurally complex zone of rocks in the Andersons and possible quartz-feldspar-biotite lavas are also Road area (425 800 mE, 5 419 000 mN) contains recorded. This sequence has a strong NW-trending lithicwacke with interbedded greywacke, siltstone cleavage and hosts a zone of variable sericite-pyrite and rhyolitic volcaniclastic sedimentary rocks. The alteration (Cethana alteration zone). Limited dip lithicwacke (Ódsvgs) contains abundant chert, basalt readings suggest that the sequence dips to the N-NE. and dolomite clasts and suggests that parts of this No reliable facing is known although Murphy et al. sequence can be correlated with the Sprent (1999) suggested that the sequence faces north and conglomerate. The bulk of this sequence has been underlies a sequence of andesitic lavas (Dasher designated as undifferentiated Gog Range Greywacke andesite) and volcaniclastic sedimentary rocks in the (Ódsvg) on the map with minor intercalations of felsic Gowrie Park–Days Road area. The latter sequence is volcaniclastic sediments (Ódsvgv). Unpublished field correlated with the Tyndall Group. mapping by D. C. Green suggests that the Andersons Spur sequence overlies a predominantly greywacke Corbett and McClenaghan (2003) favoured correlation sequence (Ódsvgg) in a syncline. Potential correlates of the sequence which hosts the Cethana alteration of the Andersons Road sequence also occur along zone with the Eastern Quartz-Phyric Sequence. The Narrawa Road in the Wilmot area. Eastern Quartz-Phyric Sequence occurs to the south of

Tasmanian Geological Survey Record 2008/01 10 the Machinery Creek Fault and although generally In general terms, the sequence which hosts the poorly defined, the following stratigraphic succession Cethana Pyrite Zone is identical to the sequence has been established: underlying the Tyndall Group in the Lake Barrington, Sheffield and Gog areas and the favoured correlation is Youngest Bull Creek Formation: A sequence of with the felsic volcanic-rich parts of the Gog Range quartz-feldspar-biotite phyric lava and Greywacke of the Western Volcano-Sedimentary volcaniclastic sedimentary rocks which is Sequence. The relatively thick sequence of felsic lavas generally considered to represent an and volcaniclastic sedimentary rocks in the Cethana eruptive and locally reworked facies of the and Lake Barrington areas suggests that these intrusive Bonds Range Porphyry. occurrences are part of a proximal volcanic centre developed in the upper parts of the Gog Range Back Peak Beds: A sequence of rhyolitic Greywacke sequence near the southern margin of the volcaniclastic sedimentary rocks. Fossey Mountain–Dial Range Trough. The felsic Oldest Sticht Range Beds: A basal siliceous sequence is noticeably thinner and interbedded with conglomerate and sandstone sequence the Gog Range Greywacke in the Firetower and which is unconformable on Proterozoic Montana areas. The sequence in the Belstone Road basement. area on the Gog map contains abundant pumice and shard fragments and rare ignimbrites, suggesting that Thin sections of the sequence which hosts the Cethana this volcanism was partly explosive. Quartz-feldspar alteration zone and the Eastern Quartz-Phyric crystals and rhyolitic pumice are also common in the Sequence to the south of the Machinery Creek Fault overlying Tyndall Group, which may indicate that this were examined to find evidence to support the phase of volcanism probably continued during correlation of Corbett and McClenaghan (2003). Only Tyndall Group deposition. rare detrital biotite and minor biotite phyric lava was observed in the rocks from the Cethana alteration In the Bell Mount area, to the west of the Cethana zone, suggesting that direct correlation with the Bull alteration zone, the Cambrian sequence consists of Creek Formation is unlikely. The andesitic interbedded ashy-tuffaceous siltstone, greywacke and volcaniclastic sequence at the base of the Tyndall quartz-feldspar phyric volcaniclastic sedimentary Group in the Cethana–Paradise area contains clasts of rocks. Several large quartz-feldspar porphyry quartz-feldspar-biotite phyric porphyry and biotite intrusive bodies and interbedded feldspar phyric and hornblende detritus (G. Ebsworth, dacite and quartz-feldspar-hornblende phyric lavas M. McClenaghan, unpublished data). This suggests have been recognised (Pemberton and Vicary, 1989). that a correlation between the Bull Creek Formation The relationship between the Bell Mount sequence and and the Tyndall Group is quite likely. The Back Peak that of the Cethana alteration zone is poorly known. Beds are derived from rhyolitic sources and are rich in The description above suggests some similarities quartz and feldspar crystals, pumice fragments and although there is a noticeable increase in the glass shards. The rhyolitic provenance is similar to that abundance of ashy siltstone in the Bell Mount area and of the felsic volcanic-rich parts of the Gog Range feldspar phyric dacite lava has not been recorded from Greywacke. The Sticht Range Beds are similar in the Cethana alteration zone. Many of the uncertainties provenance and facies to the siliceous conglomerate are a consequence of a boundary between different MRT mapping programs in the vicinity of Cethana and sandstone (Ódsvgc and Ódsvgq) units of the Gog Bridge. To partly resolve some of the problems Range Greywacke in the Cethana and Gog areas. additional information from Murphy et al. (1999) and However as these units can occur at several Temby (1985) has been added to the map although the stratigraphic levels within the Gog Range Greywacke result is poorly constrained. and also in the overlying Tyndall Group (Ódtsc), direct correlation with the Sticht Range Beds may be The available evidence suggests that the Bell Mount unreliable. sequence may be a strike continuation of the Cethana alteration zone (Corbett and McClenaghan, 2003) and There is some evidence to support the idea of Corbett a correlate of the Gog Range Greywacke. The presence and McClenaghan (2003) that the Western of the feldspar phyric dacitic lavas and the increase in Volcano-Sedimentary Sequence and the Eastern ashy siltstones suggests that a correlation with the Quartz-Phyric Sequence are lateral equivalents, Alma formation, which outcrops in the Castra area, however this statement is very broad and poorly may also be possible. If this latter correlation can be constrained. The results of this review suggest that the proven, then the Bell Mount sequence may underlie felsic volcanic-rich parts of the Gog Range Greywacke the Cethana alteration zone. Additional mapping in have a similar provenance to the Back Peak Beds of the the Cethana Bridge and Bell Mount area is highly Eastern Quartz-Phyric Sequence and may be lateral recommended. equivalents, although this is hard to demonstrate due to the discontinuous nature of the outcrop to the south The Bull Creek Formation is general poorly described of the Machinery Creek Fault because of Late and the internal geology quite complex; this is partly Cambrian to Tertiary cover and Tabberabberan due to the previously mentioned boundary between deformation. two MRT mapping projects in the vicinity of Lake

Tasmanian Geological Survey Record 2008/01 11 Cethana and partly due to strong, texturally Volcano-sedimentary Sequence is a complex sequence destructive quartz-epidote-actinolite alteration of the of interbedded basement-derived sedimentary rocks Cambrian sequence adjacent to the Dolcoath Granite. with interbedded volcanic units. Sparse fossil A review of thin sections collected in the Bull Creek occurrences from the sequence range in age from late area has been made and a simplified geological Templetonian to Florian in the Isandula area to early interpretation is presented on the map, as many of the Boomerangian in the Paradise and Sugarloaf Gorge established geological boundaries and rock types areas. This suggests that deposition of the Western could not be verified. Volcano-sedimentary Sequence in northern Tasmania is largely contemporaneous with deposition of the Que A generalised stratigraphy of the Bull Creek River Shale and Southwell Subgroup in the Hellyer Formation of interbedded quartz-feldspar-biotite area of western Tasmania. phyric lava, autoclastic breccias and volcaniclastic sedimentary rocks overlain by an epiclastic sequence The overlying Tyndall Group is a bimodal sequence of of quartz-feldspar-biotite phyric volcaniclastic andesitic to rhyolitic volcanic rocks. Minor sandstone, lithic-rich sandstone and siltstone can be interbedded fossiliferous units range in age from established. This sequence is intruded by Boomerangian to early Mindyallan. A regionally quartz-feldspar-biotite phyric intrusive rocks extensive pyroxene-feldspar phyric crystal-rich correlated with the Bonds Range Porphyry (Óqfbp). volcaniclastic sandstone unit forms a distinct marker Thin sections from the sequence suggest that the horizon at the base of the Tyndall Group in the intrusive rocks, lavas and sediments are closely Deloraine–Cethana area, and is a possible correlate of related. A common feature of the formation is the high the Lynchford Member in western Tasmania. abundance of biotite and common occurrence of accessory apatite. The presence of glass shards and A zone of variable sericite-pyrite alteration (the abundant pumice fragments indicate local explosive Cethana Alteration Zone) underlies the basal activity. Lynchford Member in the Cethana–Gowrie Park area and is hosted in the upper felsic volcanic-rich parts of In general the Bull Creek Formation dips and faces to the Western Volcano-sedimentary Sequence. The the southwest and is dislocated by the Bismuth Creek overlying contact with the Tyndall Group has been Fault. The sequence to the southwest of the Bismuth considered to represent a favourable horizon for Creek Fault has been reinterpreted, following a review VHMS-style mineralisation (MacDonald, 1993; of available thin sections, as a structural repeat of the Stockwell, 1997; Denwer, 2000) with the underlying Bonds Range Porphyry with local interbedded Cethana Alteration Zone representing a large zone of sediment horizons. Towards the base of the sequence footwall style alteration. Lead isotope data from the the Bull Creek Formation is locally interbedded with Cethana Alteration Zone supports a Cambrian age for the underlying Back Peak Beds. A belt of Cambrian this mineralisation (Carr and Dean, 1989a). rocks to the south of the Bismuth Creek Fault consists of quartz-feldspar phyric volcaniclastic sandstones This review has shown that the basal Tyndall Group and siltstones and has been correlated with the Back volcaniclastic facies (the Lynchford member) is more Peak Beds. regionally extensive than previously mapped and can be traced to the Lake Barrington, Beulah and Gog areas Correlates of the Bull Creek Formation also occur in the (fig. 4, 5). Significantly, alteration at the Firetower, Iris River and Solomons Dome area. West Gog and Stonebridge prospects is located at or near the inferred favourable horizon. Vein style Conclusion and implications mineralisation (remobilised Cambrian alteration?) at for mineralisation the Lake Barrington prospect is hosted in a similar sequence to the Cethana Alteration Zone and may This report documents revisions to six 1:25 000 scale represent a zone of footwall style alteration. digital geological maps in the Deloraine to Cethana Several prospects (Days Road, Atkinsons, Mt Roland, area (fig. 1) with emphasis on the stratigraphy of the Staverton, Claude Road, Lower Beulah Barite) occur at Cambrian Mt Read Volcanics. It extends and refines higher stratigraphic levels than the favourable horizon the previous study of Corbett and McClenaghan at the base of the Tyndall Group. Lead isotope data (2003). suggest that some of these prospects (Lower Beulah The Cambrian Mt Read Volcanics in the Deloraine to Barite and Mt Roland) may be of Cambrian age, Cethana area can be divided into two main although there is also evidence of a later Devonian stratigraphic units; the Western Volcano-sedimentary overprint (Carr and Dean, 1989b; Crawford in Sequence and the Tyndall Group. The Western MacDonald, 1993).

Tasmanian Geological Survey Record 2008/01 12 r h t e a l c w u n o e e t o B e p

z r r i i s r e F o w o r o G h t t p L

c c O e n l e e G Z s b t p p

t c , a s s s a t r e b n o o u o r r W c P

f p p e ,

o v v i

u s r a u a u a r t t C B A F n S I s t c a t n o c

e v i D s u r L t d n I a E I o R F

e e F g d d E u i a r l H b C e S n o t S . a e r d a n n

a l o g n t o r o o t e R

v g G t a T n – t i M r S a r O r a t B M s

e a L I k C a

L W e h t

n i

n o i t 4 a

s i l e r a r u e d g a n e i i o n R F o

m Z

A y d n a o n N i D t a a A

r s y e n H t h l o T s p A

n a E a i r k n t C g a i A h t t a e r C t s

n a i r b m a D C ? ? E s a y R r s m l r s n r e A D o e P l s

N r d w I e a n h K a G

P /

f s c a o A n

M c o k t u R r s L o T e F r S P A C ? ? e s e n t e e t t e e e i i o l k k e n i c c c s t r c c o t n e n i n n e y a y a a o c c e n n e e i i i d h m h t t t i w w m u u o i i u u n c p i r

a i y y R d t s s q q q

d o c A o s e e e i

t a e e l f e e e m n t r r

s r n h a s d d s s e

s o k

f r o G G t a n n

r e c f a

l k c c e e i r l

i i g a a t o t t e e u o e

g c f e K a n s i r

r r l s s i

g g e o p e r a n r a e e u a a n n l C r w B l l p

a b / p d c L a a w a c c o r m i r e c i i U l p n l o n e R R B n e v n n t

a A o U L n a h o a a i s n g g e v i c s I o c c l k o o l l r M a o

a W o o G G

G v D L v v

r e b m e M d r o f h c n y L n o i t a m r o F ? r e b m e M

l l i H g a Z g i Z k c o t s m o C

p u o r G l l a d n y T e c n e u q e S y r a t n e m i d e s - o n a c l o V n r e t s e W

Tasmanian Geological Survey Record 2008/01 13 n o z i r o H

e l t b c a r e u p t l o s v u o r a a P F F m k

e t 5

E m 0 0 0 0 5 4 a B

h a l u e B

r e w o L r e t w s e o e c t n e W r

e i e u F q h e t t e

i f S n

o o

. y r r z a a a n e t t e r o n S g a e m

i g r m d i o b n d G e a e

n – s e e - t a o i c t o r n n n S o a i e a h d u c

t g l q e d o o 5 e e

C V G S

e t n e g n r i r s h r s e t e u e t

s t f s g a s W i

E m 0 0 0 0 4 4 F y U W E g o l o e g s

n d o e i s f i l n i p k t m i A S p p u u o o r d r r n G e G

a l l l b l l a o a m d p d R e

n u n t y M o y

r T M T

r G r e

t l o i e l f s g a h e n d c d u n n n o y y A Y L T a n a n h o t t e g n C n

i o t r t s r r a a e E v B

a t e p S k u a o d L r a

E m 0 0 0 0 3 4 e l n R t l

i i – e s n n H w y a

a r i a O d r

G D n b

n u n a m i o a a c i i R a r n C v

e o n o e v v a t d r o e h a t C D L O e C

t s e N m W

0 0 0

s 0 1 g 4

g i 5 H

Tasmanian Geological Survey Record 2008/01 14 References JAGO, J. B. 1989. Report on Cambrian fossils from near Paradise. Appendix 8 in: RAND, S. W.; NOONAN, D. J. 1989. BARTON, C. M.; BRAVO, A. P.; GULLINE, A. B.; LONGMAN, Exploration Licence 11/88, Gowrie Park, Tasmania. Progress M. J.; MARSHALL, B.; MATTHEWS, W. L.; MOORE, W. R.; report for the year ended July 1, 1989. Aberfoyle Resources NAQVI, I. H.; PIKE, G. P. 1969. Geological atlas 1 mile Limited [TCR 89-3004]. series. Sheet 46 (8219N). Quamby. Department of Mines, LAURIE, J. R. 1996. Correlation of Lower–Middle Ordovician Tasmania. clastics in Tasmania. Record Australian Geological Survey BARWICK, D. G. 1991. Geology and mineralisation of the Sock Organisation 1996/23. Creek and High Point areas, western Tasmania. B.Sc. (Hons) LAURIE, J. R.; JAGO, J. B.; BAO, J-S. 1995. Review of Tasmanian thesis, University of Tasmania. Cambrian biostratigraphy. Record Australian Geological Survey Organisation 1995/69. BERRY, R. F.; SELLEY, D.; WHITE, M. J.; MEFFRE, S. 1997. Lithogeochemistry, in: Structure and mineralisation of MCCLENAGHAN, M. P. 2004. Digital Geological Atlas 1:25 000 Western Tasmania. AMIRA Project P291A. Final Report. Scale Series. Sheet 4441. Sheffield. Mineral Resources 33-58. Centre for Ore Deposit and Exploration Studies, Tasmania. University of Tasmania : Hobart. MCCLENAGHAN, M. P.; GREEN, D. C. 1997. Digital Geological CALLAGHAN, T. 2002. Annual Report, Gog EL12/2001, Atlas 1:25 000 Scale Series. Sheet 4241. Wilmot. Mineral September 2001–August 2002. AurionGold Exploration Resources Tasmania. [TCR 02-4766]. MCCLENAGHAN, M. P.; GREEN, D. C. 1999. Digital Geological CALVER, C. R.; EVERARD, J. L.; MCCLENAGHAN, M. P.; Atlas 1:25 000 Scale Series. Sheet 4240. Cethana. Mineral VICARY, M. J. (compilers). 2008. Digital Geological Atlas Resources Tasmania. 1:25 000 Scale Series. Sheet 4441. Sheffield. Mineral MCCLENAGHAN, M. P.; GREEN, D. C.; VICARY, M. J. Resources Tasmania. (compilers). 2008a. Digital Geological Atlas 1:25 000 Scale Series. Sheet 4241. Wilmot. Mineral Resources Tasmania. CARR, G. R.; DEAN, J. A. 1989a. The metallogenic association of sulfide mineralization from the Gowrie Park Prospect, MCCLENAGHAN, M. P.; GREEN, D. C.; VICARY, M. J. northwestern Tasmania. Appendix 3 in: JONES, P. A. 1989. (compilers). 2008b. Digital Geological Atlas 1:25 000 Scale Exploration Licence No. 10/88 — Gowrie Park. Progress report Series. Sheet 4240. Cethana. Mineral Resources Tasmania. on exploration activity 22 August 1988 to 22 July 1989. Noranda Proprietary Limited [TCR 89-3009]. MCCLENAGHAN, M. P.; GREEN, D. C.; SEYMOUR, D. B.; BROWN, A. V. 2001. Digital Geological Atlas 1:25 000 Scale CARR, G. R.; DEAN, J. A. 1989b. Report to Aberfoyle Series. Sheet 4440. Gog. Mineral Resources Tasmania. Resources Limited on the Pb isotopic compositions and MACDONALD, G. 1993. Exploration Licence 10/88 Gowrie Park. metallogenic association of exploration samples from the Annual report on exploration activity August 1992 to July Cethana area of NW Tasmania. Appendix 5a in: RAND, S. 1993. Plutonic Operations Limited [TCR 93-3500]. W. 1990. Exploration Licence 11/88, Gowrie Park, Tasmania. Progress report for the year ended 1 July, 1990. Aberfoyle MCCLENAGHAN, M. P.; GREEN, D. C.; SEYMOUR, D. B.; Resources Limited [TCR 90-3153]. BROWN, A. V.; VICARY, M. J. (compilers). 2008. Digital Geological Atlas 1:25 000 Scale Series. Sheet 4440. Gog. CORBETT, K. D. 2002. Western Tasmanian Regional Minerals Mineral Resources Tasmania. Program. Mount Read Volcanics Compilation. Updating the geology of the Mount Read Volcanics belt. Record MOORE, W. R. 1971. Geological investigation of the Quamby Geological Survey Tasmania 2002/19. Brook No. 11 dam site. Technical Reports Department of Mines Tasmania 14:70–75. CORBETT, K. D.; MCCLENAGHAN, M.P. 2003. A review and interpretation of the Lower Palaeozoic geology of the Que MURPHY, F. C.; DENWER, K.; MCNEILL, A.; PARFREY, O. C. River–Sheffield area, with particular reference to the 1999. Lake Barrington EL 3/98. Annual report, March 1999. Cambrian volcanic sequences. Record Geological Survey Pasminco Exploration Limited [TCR 99-4306]. Tasmania 2003/17. PEMBERTON, J.; VICARY, M. J. 1989. Mt Read Volcanics Project Map Series. Map 9. Geology of the Winterbrook–Moina area. DENWER, K. P. 2000. Lake Barrington EL 3/98, annual report, April 2000. Pasminco Exploration Limited [TCR 00-4445]. Department of Mines, Tasmania. PIKE, G. P. 1973. Geological Atlas 1 Mile Series. Sheet 46 DICKSON, T. W. 1992. Analytical data from drill holes DD84BB4, (8214N). Quamby. Explanatory Report Geological Survey DD84BB5, Beulah area, EL 7/73. CRA Exploration Pty Ltd Tasmania. [TCR 92-3390]. POLTOCK, R.A. 2002. Western Tasmanian Regional Minerals DOYLE, M. G. 1990. The geology, mineralisation and alteration of Program. Ground truthing aeromagnetic and radiometric the Jukes Proprietary Prospect, western Tasmania. B.Sc. features, northern Tasmania. Record Geological Survey (Hons) thesis, University of Tasmania. Tasmania 2002/20.

HERRMANN, W. 1991. Annual Report to 3/8/91. EL 16/90 — PORTER, T. M. 1973. The McClarm Syndicate’s EL 11/70, Beulah. Deloraine. Outokumpu Exploration Australia Pty Ltd Geological-geochemical reconnaissance. CRA Exploration Pty [TCR 91-3277]. Ltd [TCR 74-991].

HICKS, D. J. 1989. The geology and mineralization of the Cethana RAND, S. W. 1989. Exploration Licence 43/85 Beulah, Tasmania. Pyrite Zone, northwest Tasmania. B.Sc. (Hons) thesis, Progress report for the year ended April 29, 1989. Aberfoyle University of Tasmania. Resources Limited [TCR 89-2999].

Tasmanian Geological Survey Record 2008/01 15 RAND, S. W. 1990. Exploration Licence 11/88, Gowrie Park, VICARY, M. J. (compiler). 2008b. Digital Geological Atlas Tasmania. Progress report for the year ended 1 July, 1990. 1:25 000 Scale Series. Sheet 4639. Deloraine. Mineral Aberfoyle Resources Limited [TCR 90-3153]. Resources Tasmania. VICARY, M. J.; JACKSON, S. 1993. Exploration Licence No. 15/92 RAND, S. W.; NOONAN, D. J. 1989. Exploration Licence 11/88, (Beulah). Annual report, August 1992–July 1993. RGC Gowrie Park, Tasmania. Progress report for the year ended July Exploration Pty Ltd [TCR 93-3488]. 1, 1989. Aberfoyle Resources Limited [TCR 89-3004]. VICARY, M. J.; MCCLENAGHAN, M. P. 2007. Digital Geological STOCKWELL, R. 1997. Annual report Jan. 1997–Jan. 1988. Atlas 1:25 000 Scale Series. Sheet 4242. Castra. Mineral Tasmanian Basemetals Project EL 32/94 Gowrie Park. RGC Resources Tasmania. Exploration Pty Ltd [TCR 97-4099]. WELLS, A. T. 1957. Geology of the Deloraine–Golden Valley area, Tasmania. Records Queen Victoria Museum NS 8. TEMBY, P. A. 1985. EL 10/76 Cethana area, northern Tasmania. WOODWARD, N. B.; GRAY, D. R.; ELLIOTT, C. G. 1993. Report on exploration for 12 months to 28 February 1985. CRA Repeated Palaeozoic thrusting and allochthoneity of Exploration Pty Ltd [TCR 85-2333]. Precambrian basement, northern Tasmania. Australian Journal of Earth Sciences 40:297–311. VICARY, M. J. (compiler). 2008a. Digital Geological Atlas 1:25 000 Scale Series. Sheet 4640. Montana. Mineral [9 July 2008] Resources Tasmania.

Tasmanian Geological Survey Record 2008/01 16