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WEATHERING and MORPHOSTRATIGRAPHIC EVIDENCE for FOUR GLACIATIONS in the HENTY RIVER BASIN, WESTERN TASMANIA by Paul C

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WEATHERING and MORPHOSTRATIGRAPHIC EVIDENCE for FOUR GLACIATIONS in the HENTY RIVER BASIN, WESTERN TASMANIA by Paul C Papers and Proceedings of the Royal Society of Tasmania, Volume 129, 1995 53 WEATHERING AND MORPHOSTRATIGRAPHIC EVIDENCE FOR FOUR GLACIATIONS IN THE HENTY RIVER BASIN, WESTERN TASMANIA by Paul C. Augustinus and Eric A. Calhoun (with two tables and three rext-figures) AucGSTIMJS, P.C. & Cor.HOUN, E.A., 1995 (30:vi): Weathering and morphostratigraphic evidence for four glaciations in the Henry River Basin, western Tasmania. Pap. Proc. R. Soc. Tasm. 129: 53-58. https://doi.org/10.26749/rstpp.129.53 ISSN 0080-4703. Department of Physical Sciences, University of Tasmania, PO Box 1214, Launceston, Tasmania, Australia 7250 (PCA); Departmem of Geography, University of Newcastle, Callaghan, NSW, Australia 2'.308 (EAC). The Quaternary glacial histories of the Picman and Hemy River Basins have largely been developed by using post-depositional weathering criteria to identify and map the drift sheets. Application of relative dating techniques, such as percentage absorption and specific gravity of Cambrian volcanic clasts, forces a reinrerprctation of palaeomagnetic evidence previously offered for the age of the Henty Drift, so that at least three pre-Last Glacial Maximum (LGM) drift sheets can be recognised. The deeply weathered and most extensive (but with limited exposure) Berry Creek Drift is possibly a correlative of the Bulgobac/Linda Drift and can be clearly distinguished from the slightly less extensive but more widely exposed Henty Drift. A minimally weathered and spatially restricted drift, termed the Julia Drift, is exposed beyond and pre-dates the LGM end moraines. Keywords: glaciation, Henty Basin, relative dating, correlation, driftsheets, Tasmania. INTRODUCTION Correlations between the sequences from each of the basins have necessarily been made on the basis of post­ The Late Cenozoic glacial history of western Tasmania has depositional weathering criteria, such as thickness of been reviewed in a number of studies (Colhoun 1985a, weathering rinds developed on clasts of Jurassic dolerite, Colhoun & Fitzsimons 1990, Kiernan 1990a, Fitzsimons et and relative degrees of till matrix alteration and soil al. 1993). Although the essential elements of glacial histories development. Use of these relative dating (RD) techniques of each major drainage basin have been elucidated (Pieman enabled the discrimination of the sediments deposited by Basin - Augusrinus & Colhoun 1986, Augustinus et al, differentglacial events. However, use of RD criteria (such 1994; Henry Basin - Colhoun, 1985a,b; the King Basin - weathering rind thickness variations) for correlation of Fitzsimons & Colhoun 1991, Fitzsimons et al. 1993), the glacial sequences between even adjacent drainage basins is timing of the identified glacial events from each basin is hampered by the general absence of dolerite in the glacial poorly constrained, due to the general absence of datable sediments from some valleys. In addition, climatic and material. As a consequence of this uncertainty, correlations topographic drainage differencespertaining between basins between glacial sequences, even from adjacent valleys are influencethe rate of weathering and, hence, the validity of problematical. correlations made on the basis of such criteria (Kiernan 19906). .. This paper assesses the use of several post-depositional 145' 30' Mt Murc I weathering criteria in mapping the glacial drifts of the '- ���� Mt Read '- Moxon ',,�, ( Henty River Basin (fig. 1) and attempts to correlate the 2.5 km .. \Saddle ',, ° drift sheets defined with those mapped in the adjacent Study� 40 s Area Pieman Basin. Since Jurassic dolerite is absent from most er0 14S E of the Henty Basin Drifts,alternative RD criteria had to be used, including percentage absorption and specific gravity variations in Cambrian volcanic clasts from glacial diamictons. We combine the RD information with palaeo­ magnetic evidence to construct a correlation of the glacial sequences between the basins that is more reliable than any hitherto. Huntley GLACIAL HISTORY OF THE HENTY RIVER BASIN The glacial history of the Henry Basin was first studied by Bowden (1974), and glacial landforms were mapped as the product of one glaciation. The firstevidence that more than one glaciation had occurred in the Henry Basin came from 14C dates on lacustrine organic clays overlying weathered till at Henty Bridge (fig. 1) (Colhoun 19856). Dates of23 640 FIG. I-Location map, Henty River Basin ± 1030 yrs (GaK 5597) to >34 600 yrs BP (GaK 5595) 54 PC and EA. Colhoun confirmed that the USED IN STUDY The of discovered interglacial at indicated a mixed wer forest at the site llleans that The site IS located 1 km so successful in the mapping of dsewhere in western Tasmania (i.e. Kiernan 1983, Kiernan 1989) was not here. The degree of of Cam brian volcanic clasts from the Pieman Basin was & Colhoun (1')86) to discriminate bet\ivecn drift of different relative ages 'AliIh d Llnge of other C:an1LJrjan volcdlilcs I-Ience l vve of Cam brian volcanic clast alre;'ation identification of drift sheets of Basin, and from both the of date removed. The variations in %Ab and SC reflect development, and indicate the host drifr 198 Where possible, clast samples Selina were taken from a uniform 1 m in the drift exposures. The than the from last interstadial to the commencement of of clast alteration deterioration and onset of the LGM has been inferred at depth probably 25 000 YIS SF at Tullabardine & van de Geer influence on the One to two 1 with the end of the LGM at Lake Selina dated at of 4-8 crn di3meter Cambrian volcanic BP variations between the criteria used for the include till matrix did not penetrate west of the West in the d.rift, dolerite Coast Range, unlike the older and far more extensive Boco rind thicknesses appropriate) and tile Boco 2 Glaciation & Calhoun moraine morphology,. The derails of these techniques were , Bobaciil (formerly the Boco 1 Glaci,uion of in Augustinus & Colhoun (1 and are used here & Calhoun 1986) and Bulgobac ill the .to drift: separation based on observations Pieman Basin & C:olhouu 1 Augustinus of degrees of drift m od.ification. et ai. 1994). Sharp-crested LGM end moraines are found below Mrs Read and Murchison and at the southern end of the '1' Plateau (the Hamilton End Moraine) (fig. RESULTS AND DISCUSSION CV'UC=l1LC {'or an early Last Glacial advance, such as that the King Valley (Chamouni Glaciarion) by Observations on the relative degree of weathering of the Fitzsimons & Colhoun (1991), has been recognised from drifts fi'om the Henty River Basin suggest the development the Henty Basin. of at least three distinct drift sheets of differing relative age beyond the LGM limits. The most useful methods for separating the drift sheets were quantitative evaluation of state of clast alteration, degree of iron panning and clast Fe oxide topographic position and degree of modification morphology (table 1). in the River Basin 55 TABLE 1 Late Cenozoic glacial stratigraphy, Henty River Basin, western Tasmania -~-.----.---.. ---- of events isation acid rind thickness Fe oxide front max. (mm) 18.8 none Interstadial=; Julia Drift minor Fe <2 Langdon >41.9 7 Drift >34.G~ 15 2.10- 2,A-') thin Fe: 2. ·4 >783 Creek Drift reversed" 3nu l4.4-20.8 1.95--2.05 thick not >4 " ~ dolerite. :t Colhoun et al. (i § Calhoun et al. ~ Calhoun ( ( 199 Creek and Creek contains up to 40% dolerite clasts with rims of up to 3 em but ary, and no morame Calhoun (1 the Glaciation. Grid Reference 5SG CP 80161 limit ofthe LGM moraines on the and the >33 950 yrs BP date from 145" 30' at. 1 indicates that the N fVl1 Read is the most 2.5 km drift sheets -~ the 1 erate, with the former degree of clast alteration Drift. No dolerite was ll"-l1LtHJ.C: is COllllnOfl, vilth on volcanic clasts 1). reddish brown a continuous cover is maintained, without clear end mor::lines. This drift sheet is best displayed at the and at the Darn Road- Zeehan intersection and is considered to represent thc Henty described Calhoun (l985a, b), Con- sequently, the name Henty is maintained for the drift at 42"S this site, and Henty remains the type site. One kilometre north Henty Bndge, on the Zeehan Highway, the drift exposures moderate degrees of ~ Giacicr flow direction Margaret CHacintion limits weatberingway to a deeply altered diamicton containing 0, Organic site -- Julia Creek Glaciation totally decomposed Cambrian volcanic clasts of up to Henly Glaciation CirquefneadwaU 0.25 m diameter. The till matrix is weathered to bright """""""~,, Berry Creole Glaciation yellowish brown (1 and strong Fe oxide panning 1S (table The depth to the weathering front in this drift. The drift exposure at Tom HG. 2-Glacial RiIJer Basin 56 (md E.A. Colhoun here t:he Berry Creek afrel' its type sirc north of Creek 011 the Zeehan 3635 -- 1 :25 000; UGR SSG (1985) altered clasrs in rill at Professor Creek (fig. and suggested (hat the at this sile pre-d ate the till at Henty with the Ltnda from the King similar gross stdte of clast lienee. the altered tiU from [his site probably correlates with the Berry Creek Drift on 'the . Zeehan and further supports the subdivision the Hentv least two glacial drift sheets of . SUPPORT DRIFT SHEET USING PERCENTAGE D SPECIFIC GRAVITY 30 • Borry Creek Drift Augustinus & Colhoun (1 %Ab SG El Li!lda Drill c .. values from Cambrian volcanic in the Pieman River 0 20 Basin as a scatter graph, and obtained a line e-o relationship with three identifiable populations. These group­ (fJ .n ings supported other post-depositional weathering evidence « 10 for at least three distinct drift sheets (Augusrinus & Colhoun eR- 1986). The %Ab and SG data showed that the penultimate Boco Glaciation Drift could be discriminated clearly from 0 the much more extensively altered Bulgobac Drift. The 1.6 1.8 2.0 2.2 2.4 2.6 2.8 latter displays reversed detrital magnetisation and is hence > 783 kyrs old (Pollington 1991, Baksi etal.
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