Transactions Roy Soc /Records

Transactions of the Royal Society of South Australia (2010), 134(1): 113–122

THE DAWSON HILL MEMBER OF THE GRINDSTONE RANGE SANDSTONE IN THE FLINDERS RANGES, SOUTH AUSTRALIA J.B. JAGO 1, C.G. GATEHOUSE2, C.MCA. POWELL3, T. CASEY4 & E.M. ALEXANDER5 1. Barbara Hardy Centre, School of Natural and Built Environments, University of South Australia, Mawson Lakes, SA 5095 2. 4 Frontignac Avenue, Wattle Park, SA 5066 3. Deceased July 21, 2001 4. P.O. Box 1011, Clayton South, Victoria 3169 5. Petroleum section, Primary Industries and Resources South Australia, GPO Box 1671, Adelaide, SA 5001.

Abstract

The Dawson Hill Member of the Grindstone Range Sandstone is the uppermost unit of the Lake Frome Group, and the highest exposed unit in the Neoproterozoic to Cambrian sedimentary succession in the Flinders Ranges, South Australia. It is formally defined herein from a 190m thick type section that has no exposed top. The Dawson Hill Member comprises mainly poorly sorted, cross-bedded sandstone which, at some levels, contains abundant well rounded pebbles and cobbles of quartzite and quartz derived from an unknown source area to the southwest in the early stages of the Delamerian Orogeny. The age of the unit is poorly constrained. It is probably of late early Cambrian or early middle Cambrian age.

KEY WORDS: Dawson Hill Member, Lake Frome Group, Delamerian Orogeny, Cambrian, Flinders Ranges, definition, stratigraphy.

Introduction

The Cambrian sedimentary succession of the Adelaide Fold Belt of the Flinders and Mt Lofty Ranges represents the end of a long period of Neoproterozoic to Cambrian sedimentation that commenced about 850Ma. Details of the Neoproterozoic and Cambrian successions are available in Preiss (1987), Jago & Moore (1990), Preiss et al. (1993), Gravestock (1995) and Zang et al. (2004). The Cambrian stratigraphy of the Arrowie Basin in the Flinders Ranges is summarized in Fig. 1 which shows that there is an unconformity at the base of the Cambrian. The bottom part of the Cambrian, the Hawker Group, is carbonate dominated, although some clastics are present; lateral and vertical facies changes within the Hawker Group are quite rapid (Daily 1976). The Hawker Group is overlain by shallow marine to deltaic red sandstones and siltstones of the Billy Creek Formation and the overlying shallow marine Wirrealpa Limestone. Several authors (Daily 1969, 1976, 1990; Shergold et al., 1985; Gravestock 1995; Zang et al., 2006) consider that the change from the carbonate dominated Hawker Group to the clastic dominated Billy Creek Formation reflects the Kangarooian Movements of Daily & Forbes (1969). Alternatively, Jenkins (1990) and Haines & Flöttmann (1998) suggested that an early phase of the Delamerian Orogeny uplifted the present area of the Adelaide Hills and thus provided a source of terrigenous sediments for the Billy Creek Formation. This view is not supported here. The Wirrealpa Limestone is conformably overlain by the marginal marine deposits of the Moodlatana Formation, the basal unit of the Lake Frome Group, a thick succession of siliciclastics, that comprise the highest part of the Cambrian succession in the Flinders Ranges. Deposition in the Adelaide Fold Belt ceased due to uplift caused by the Delamerian Orogeny, details of which are given in Preiss (1995) and Foden et al. (2006).

The uppermost formation of this very thick Cambrian succession is the Grindstone Range Sandstone of Mawson (1939). During field work in 1989-1991, C. Powell (then of Macquarie University, New South Wales) and C. Gatehouse recognized that the top part of the Grindstone Range Sandstone was clearly different from the bottom part of the formation. On June 21, 1989 they reserved the name Dawson Hill Member 113

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(Australian Stratigraphic Units Database) with the Stratigraphic Nomenclature Committee of the Geological Society of Australia (now the Australian Stratigraphic Units Database of the Australian Stratigraphy Commission). Subsequently Preiss (1999) and Reid & Preiss (1999), in the interests of an up-to-date map, used the name and provided an abbreviated description of the unit (supplied at the time by Powell 'DZVRQ +LOO 0HPEHU and Gatehouse). It should be noted that C. Powell died *ULQGVWRQH 5DQJH 6DQGVWRQH in 2001, but while in the field with C. Gatehouse he discussed his ideas concerning the environment of 3DQWDSLQQD 6DQGVWRQH deposition, the source of the clasts in the Dawson Hill Member and their possible provenance. In addition, because of C. Powell’s death, the paper referred to as Powell and Gatehouse (in prep.) in Preiss (1999) was %DOFRUDFDQD )RUPDWLRQ never completed. The information obtained by Powell and Gatehouse is incorporated in the present paper, the purpose of which is to describe, define and discuss the 0RRGODWDQD )RUPDWLRQ significance of the Dawson Hill Member. (

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Figure 1. Stratigraphic column through the Cambrian of the Flinders Ranges.

Lack of evidence has meant that a reliable age for the Grindstone Range Sandstone is not available. Daily (1956) suggested an undefined age within the middle Cambrian; Daily (1976) and Moore (1990) suggested an Ordovician age; Jago in Shergold et al. (1985) postulated a late middle or early late Cambrian age while Gravestock (1995, fig. 7.2) suggested a late middle Cambrian (Boomerangian) age. Retallack (2008, 2009) suggested a Tremadocian (earliest Ordovician) based on a combination of the identification of a possible agnostoid trilobite (see below) in the Balcoracana Formation, published SHRIMP radiometric dates using the SL13 standard

114

DAWSON HILL MEMBER OF GRINDSTONE RANGE SANDSTONE IN THE FLINDERS RANGES

and assuming a uniform rate of sedimentation within the Cambrian of the Flinders Ranges. However, the identification of the agnostoid is doubtful (see below), the reliability of the relevant SL13 dates has been seriously questioned (Black et al.1, Jago & Haines 1998, Paterson 2005), and given that there is considerable variation in depositional environments within the Cambrian of the Flinders Ranges (e.g. reefs, tidal flats, shelf carbonates, fluvial, below wave base silts that are in part turbidites) a uniform rate of sedimentation is highly unlikely.

The highest reliably dated fossiliferous horizon within the Lake Frome Group occurs within a thin, dark platy limestone in the top part of the Moodlatana Formation, about 2000 metres below the base of the Grindstone Range Formation. This horizon occurs in several localities in the eastern Flinders Ranges (Jago et al. 2006a). Jell in Bengston et al. (1990) described the metadoxidid trilobite Onaraspis rubra from this level and suggested correlation with the late Early Cambrian Lungwangmiaoan Stage of China. Geyer & Shergold (2000) suggested that this correlates with the latest Toyonian of Siberia.

Abundant trace fossils occur within the Moodlatana and Balcoracana Formations; some also occur in both the Pantapinna Sandstone and the Grindstone Range Sandstone (Gravestock & Cowley 1995, Preiss 1999) but are much less common. The highest known body fossils within the Cambrian of the Flinders Ranges are unidentified shelly fossils low in the Balcoracana Formation found by T. Casey and J. Jago as part of a study of the Lake Frome Group. However, neither these fossils nor the trace fossils give a reliable indication of age. Daily & Forbes (1969) reported the presence of a single specimen of an effaced agnostoid trilobite, cf. Lejopyge sp., from what they regarded as Balcoracana Formation from Lake Frome 3 drill core, about 65km ENE of the Grindstone Range. If this identification was correct this would suggest a late middle Cambrian age. However, the specimen is missing, and the identification can not be confirmed (Jago et al., 2006b); identification of single partial specimens of effaced agnostoids is difficult. Despite this and without seeing the specimen, Retallack (2008) suggested that this agnostoid was ?Lejopyge laevigata and then (Retallack 2009, p. 357) misquoted Jago et al. (2006) and suggested that it was definitely Lejopyge laevigata, a well known late middle Cambrian zone fossil. This is simply not in accord with the facts as outlined by previous authors. We would also suggest that most, if not all, of the possible body fossils described and figured by Retallack (2009) are of inorganic origin. Given the late early Cambrian age of the Moodlatana Formation, a late middle Cambrian age of the Balcoracana Formation is improbable, with a late early or very early middle Cambrian age much more likely. This is equivalent to Stage 4 (Cambrian Series 2) or Stage 5 (Cambrian Series 3) of the revised Cambrian stratigraphic scale as outlined in Ogg et al. (2008) and available on the website of the International Commission on Stratigraphy at http://www.stratigraphy.org/upload/ISChart2009.pdf. Jago et al. (2006a, b) indicate a middle Cambrian age for the Grindstone Range Sandstone, but it is not possible to give an exact age. As discussed by Jago et al. (2006) there are no reliable radiometric dates within the Cambrian sedimentary successions of the Flinders Ranges. Stratigraphy of the Grindstone Range Sandstone

The type section of the Grindstone Range Sandstone is at the southern end of the Grindstone Range, about 4.5km SSE of Dawson Hill. It extends from latitude 31°13´53˝S, longitude 138°57´29˝E (GDA94) at the base to latitude 31°13´49˝S, longitude 138°58´07˝E at the top. Its location is shown on the Blinman 1:63 360 map sheet (Dalgarno et al., 1964) and the Parachilna 1:250 000 map sheet (Preiss & Reid 1999). The base of the Dawson Hill Member is at latitude 31°13´49˝S, longitude 138°57´52˝E.

We have produced a stratigraphic log through the type section. This includes both the lower part of the Grindstone Range Sandstone (Fig. 3) and the Dawson Hill Member (Fig. 4). In the type section, the lower part of the Grindstone Range Sandstone is about 368m thick. In this area the contact between the Grindstone Range Sandstone and the underlying Pantapinna Sandstone is not exposed. However, an inspection of aerial photographs of the area suggests that the measured section contains most, if not all, of the Grindstone Range Sandstone. Further north, near Dawson Hill (Fig. 2), the contact between the Pantapinna Sandstone and the Grindstone Range Sandstone is gradational. 1. Black, L.P., Seymour, D.B., Corbett, K.D., Cox, S.E., Streit, J.E., Botrill, R.S., Calver, C.R., Everard, J.L., Green, G.R., McLenaghan, M.P., Pemberton, J., Taheri, J. & Turner, N.J. (1997). Dating Tasmania’s oldest geological events. Australian Geological Survey Organisation Record, 1997/15.

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Figure 4. Stratigraphic column through the type section of the Dawson Hill Member.

The lower part of the Grindstone Range Sandstone is essentially a well-bedded, well sorted fine-grained sandstone that as a whole coarsens upwards. Bedding thicknesses range from 5mm to over a metre. There are several intervals where the beds are about 10mm thick; these are generally laminated and overlain by beds up to a metre thick. Planar cross-bedding is abundant, although there is also some trough cross-bedding. The cross-bedding sets are up to one metre thick. Palaeocurrent data (n=58) derived from cross-bedding measured by C. Powell and C. Gatehouse from the Dawson Hill area have a bimodal distribution towards 161° and 341° with the predominant direction being towards 161°; these measurements may reflect the influence of tidal activity. Cross-bedding data from the Ten Mile Creek area suggest a current direction generally towards about 140°. A paper on the current directions derived from cross bedding within most of the clastic units within the Cambrian succession of the Wirrealpa area is in preparation. There is at least one horizon of wet sediment slumping. Siltstone intraclasts up to 10mm across occur at several levels. Ripple marks occur all the way through the bottom part of the Grindstone Range Sandstone; they include truncated ripples, very small-scale ripples, interference ripples and asymmetric ripples with the trace fossil ?Planolites. Gravestock (1995) records the presence of trilobite tracks in the basal part of the Grindstone Range Sandstone. In addition we have observed some horizontal trails. However, we would regard most of the body and trace fossils figured by Retallack (2009) from the bottom part of the Grindstone Range Sandstone as being of inorganic origin. A few desiccation cracks are present. In at least two places, within the bottom part of the Grindstone Range Sandstone, C. Powell observed sporadic, well rounded, larger frosted grains within the fine sandstone; these may be of aeolian origin. The above information suggests that the bottom part of the Grindstone Range Sandstone was deposited in very shallow marine conditions; this is in accord with Gravestock (1995) who suggested low intertidal deposition at the base of the formation. 116


Dawson Hill Member

(a) Type section The Dawson Hill Member is named after Dawson Hill, the highest point of the Grindstone Range, located at latitude 31°11´48˝S, longitude 138°55´30˝E (GDA94) on the Wirrealpa 1:50 000 topographic sheet. The base of the Dawson Hill Member is very sharp but conformable (Fig. 5); the top is obscured by Recent gravels shed from the Grindstone Range. However, the eastern side of the Grindstone Range is faulted with evidence of faulting seen at the eastern end of some of the creeks, north of the type section (Fig. 6). Hence, as far as we are aware, a complete section of the Dawson Hill Member, and hence of the Grindstone Range Sandstone is nowhere exposed. The type section is about 190m thick (Fig. 4).

Figure 5. Base of the Dawson Hill Member at about latitude 31° 11´ 30˝S, longitude 138° 55´ 57˝E. Length of pencil about 15cm.

Figure 6. Faulting on eastern side of the Grindstone Range at about latitude 31° 12´ 33˝S, longitude 138° 57´ 30˝E. The figure is standing immediately beneath a fault.

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The Dawson Hill Member is essentially a fine to medium-grained sandstone with bimodal sorting and numerous pebble and cobble clast horizons (see below for details); on the whole it is much less well sorted than the basal part of the Grindstone Range Sandstone. However, the top few metres of exposure of the Dawson Hill Member is well sorted and well bedded, with bedding planes 10 to 30cm apart (Fig. 7). Tabular cross-bedding is abundant throughout the Dawson Hill Member, with some trough cross-bedding towards the base of the unit; the cross-bedding is less evident towards the top of the exposures. Cross-beds measured by C. Powell and C. Gatehouse from the Dawson Hill area indicate a palaeocurrent direction towards 12.3° ± 8.5° (n = 80). There are at least two horizons that exhibit wet sediment slumping.

Figure 7. Well bedded sandstone close to the top of the Dawson Hill Member type section. Hammer for scale; length about 28cm.

The basal 60m of the Dawson Hill Member is an argillaceous, very poorly sorted fine to coarse feldspathic sandstone. Although some of the grains are well rounded, most are subangular to angular. This is a recessive unit that forms a distinct valley running parallel with strike; it contains a few scattered pebble horizons, although most pebbles occur as isolated clasts of quartz and quartzite up to 2cm across; the largest pebbles here are about 16cm across.

Apart from the top 10m, the remainder of the Dawson Hill Member is essentially a moderately to poorly sorted fine to medium grained sandstone comprising greater than 90% angular clear quartz grains up to 1mm across set in a silica cement. Thin section work indicates that overgrowths are present on some of the quartz grains. In addition there is a small amount of feldspar, about 1% muscovite and a few quartz siltstone clasts up to 1mm across. The feldspar content decreases up section. There are scattered very well rounded pebbles and cobbles (see below). The large clasts, that have been used by previous authors (e.g. Gravestock & Cowley 1995; Preiss 1999) to characterize the upper part of the Grindstone Range Sandstone (i.e., the Dawson Hill Member), occur mainly over a 20 metre interval from about 90 to 110 m above the base of the unit. Here, the clasts are very abundant (Figs 8, 9, 10) and occur within a poorly to moderately well sorted medium to very coarse grained sandstone matrix, over 90% of which comprises angular to rounded clear quartz grains. The lowest horizon with abundant large clasts abruptly overlies the underlying sandstone. These well rounded pebbles and cobbles are concentrated in channels and on the foresets of planar cross-bedding (Gravestock 1995). Many of the clasts, including the largest pebbles, are extremely well rounded; the smaller pebbles tend to be subangular to subrounded. Some of clasts have their long axes aligned parallel to bedding The lithology 118


Figure 8. Well rounded clasts, about 100m above the base of the type section of the Dawson Hill Member near latitude 31°13´49˝, longitude 138°58´00˝E. Note the crude alignment with bedding of some clasts. Scale is in cm.

Figure 9. Well rounded clasts, about 100m above the base of the type section of the Dawson Hill Member. Locality as for Fig. 8. Scale is in cm.

Figure 10. Well rounded clasts, about 100m above the base of the type section of the Dawson Hill Member. Note the crude alignment with bedding of some clasts. Locality as for Fig. 8.Scale is in cm.

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of the clasts is dominated by fine-grained quartzite. In the Dawson Hill area, a count of 668 pebbles by CP and CG indicated that 551 (82.48%) are composed of quartzite, 90 (13.47%) are composed of vein quartz, 15 (2.25%) are chert and 12 (1.8%) are of other lithologies (sandstone, mica schist, siltstone, shale and unidentified lithic fragments). In the type section a count of 138 clasts by TC produced a similar result with 114 (82.61%) quartzite clasts, 22 (15.94%) vein quartz clasts and 2 (1.45%) siltstone clasts. The provenance of the clasts is unclear. Gravestock & Cowley (1995) suggested that they may have been derived from the Pound Subgroup. We have found a single large clast (13cm long) that shows bedding and is similar to the Rawnsley Quartzite (Fig. 11). However, in thin section, the most common lithic clast type is an orthoquartzite comprising well sorted angular quartz grains sutured together. A few of the grains within the orthoquartzite clasts exhibit overgrowths; ~1 to 2% of the rock comprises fine quartzite lithic fragments. There is clear evidence of strain within the rock. As the thin section is rotated, shadows pass through lithic fragments comprising multiple grains. This suggests a source area that had undergone regional metamorphism, which rules out the Pound Subgroup; in any case it is unlikely that any of the Pound Subgroup was exposed for erosion at this time. The cross-bedding data suggest a source area to the south or south west. The clast lithologies are dominated by types (quartzite, vein quartz and chert) that are very resistant to weathering and may be transported long distances, although the large size of some of the clasts, suggests a reasonably close source area. At this stage we are unable to identify a definite provenance for the pebbles. It is possible that they may be derived from an unknown succession of low grade metamorphosed rocks within the eastern part of the Gawler Craton. At the time of the deposition of the underlying Pantapinna Formation, Gravestock (1995, fig. 7.11) suggests that the exposed eastern edge of the Gawler Craton was about 110km to the west of the Grindstone Range. However, to the best of our knowledge, there is no evidence, in this part of the Gawler Craton, of the quartzite found in the clasts.

Figure 11. Large clast showing distinct bedding. From about 100m above the base of the type section of the Dawson Hill Member. Locality as for Fig. 8.

(b) other areas Apart from the Grindstone Range, the only other area of outcrop of the Grindstone Range Sandstone is in the Prism Hill area, 70km to the north east of the Grindstone Range (Vincent2), as shown on the Copley 1:250 000 sheet (Coats et al. 1973). The Dawson Hill Member outcrops in low hills to the south of Prism Hill. In this area large scale trough cross-bedding indicates a current direction towards 105 to 120°. In the Prism Hill area, Vincent2 reported a current direction of about 070° from cross-bedding measurements made across the whole of the Grindstone Range Sandstone. The clast lithology in the Dawson Hill Member at Prism Hill is similar to that in the Grindstone Range. A count of 206 pebbles by TC and JJ indicated that 182 (88.35%) are composed of quartzite, 23 (11.17%) of vein quartz and 1 (0.49%) of siltstone. Gravestock3 reported the presence of about 300m of Grindstone Range Sandstone in Moorowie 1 drillhole, about 50km northwest of the Grindstone Range, but it is not clear if the Dawson Hill Member is present. 2 Vincent, P.W. (1980). The Geology of the Prism Hill area, northern Flinders Ranges, South Australia. Unpublished B.Sc. (hons) thesis, University of Adelaide. 3 Gravestock, D.I. (1997). East Arrowie Basin subsurface correlation. Unpublished report for Beach Petroleum.

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Depositional Environment

The information noted above suggests that the bulk of the Dawson Hill Member was deposited rapidly under fluvial conditions. This is in accord with Gravestock & Cowley (1995) who suggested that the top part of the Grindstone Range Sandstone (i.e., the Dawson Hill Member) was deposited on a “bedload dominated, fluvial, sandy braidplain”. However, as noted above, the top ten metres of the Dawson Hill Member exposed in the type section is much better sorted than the bulk of the member, and may represent a return to littoral and/or shallow marine conditions. The Dawson Hill Member is the only unit within the Cambrian of the Flinders Ranges to contain such large, well rounded pebbles. Their size suggests a source area undergoing uplift during an early phase of the Delamerian Orogeny, the uplift caused by which saw the end of deposition in the Adelaide Geosyncline. Retallack (2008) described what he considered to be 17 different palaeosols within the Cambrian succession in the Wirrealpa area, although it is unclear if any were reported from the Dawson Hill Member. We are unable to confirm the presence of palaeosols within the Dawson Hill Member. Acknowledgements

Warren and Barbara Fargher of Wirrealpa Station kindly allowed access to the sections described herein. David Carver (University of South Australia) ably prepared the thin sections; John Cann (University of South Australia) is thanked for advice on the thin section petrography. Wolfgang Preiss and Peter Haines are thanked for constructive comments. Wayne Cowley (PIRSA) is thanked for advice on stratigraphic nomenclature. References

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