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A tale of two basins? Stratigraphy and detrital zircon provenance of the Paleoproterozoic Turee Creek and Horseshoe basins of Western Australia: Discussion
Accepted Manuscript A tale of two basins? Stratigraphy and detrital zircon provenance of the Paleoproterozoic Turee Creek and Horseshoe basins of Western Australia: Discussion Rajat Mazumder PII: DOI: Reference:
S0301-9268(17)30315-7 http://dx.doi.org/10.1016/j.precamres.2017.06.026 PRECAM 4808
To appear in:
Precambrian Research
Received Date: Revised Date: Accepted Date:
5 June 2017 12 June 2017 29 June 2017
Please cite this article as: R. Mazumder, A tale of two basins? Stratigraphy and detrital zircon provenance of the Paleoproterozoic Turee Creek and Horseshoe basins of Western Australia: Discussion, Precambrian Research (2017), doi: http://dx.doi.org/10.1016/j.precamres.2017.06.026
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A tale of two basins? Stratigraphy and detrital zircon provenance of the Paleoproterozoic Turee Creek and Horseshoe basins of Western Australia: Discussion Rajat Mazumder Department of Applied Geology, Faculty of Engineering and Science, Curtin University Malaysia, CDT 250, Miri 98009, Malaysia. E-mail: [email protected] Tel: +6085 630100 (extension 2520)
1. Introduction The Archean - Paleoproterozoic transition is associated with the rise of atmospheric oxygen (the Great Oxidation event, GOE, 2.45-2.22 Ga; Holland, 2002; Bekker et al., 2004), global glaciation, consequent flourishing of eukaryotic life and paleobiological evolution (Kirschvink et al., 2000; Farquhar et al., 2000). In significant contrast to the other cratonic blocks of the world, the Pilbara craton, Western Australia documents a near continuous depositional record across the GOE within the conformable succession of almost entirely marine Turee Creek Group of rocks (Martin, 1999; Van Kranendonk and Mazumder, 2015; Van Kranendonk et al., 2015) and therefore is unique (Fig. 1). Notwithstanding this, the stratigraphic sequence development and depositional model of the Turee Creek Group and the unconformably overlying Lower Wyloo Group is a matter of conjecture because of inadequate sedimentological facies analysis (Thorne et al., 1991; Krapez, 1996, 1997; Martin et al., 2000; Krapez et al., 2017). Krapez et al (2017) have made an attempt to reassess the existing tectonostratigraphic history of the Pilbara craton during 2.45-2.0 Ga supplemented by detrital zircon provenance study. Although their detrital zircon data is new and significant, they did not provide any new sedimentologic and stratigraphic data and tried to fit the detrital zircon provenance data in the existing foreland tectonostratigraphic model (the Turee Creek basin), without critically analyzing alternative intracontinental rift model recently
suggested by Van kranendonk et al. (2015), Van kranendonk and Mazumder, 2015, and Mazumder et al., 2015. Krapez et al (2017) have cited these papers and made some statements, quoting Mazumder and Van Kranendonk (2013) and Van Kranendonk et al. (2015), which clearly indicates that they have not read the paper critically (discussed below). Krapez et al. (2017) relied heavily on conjectural stratigraphic model that is largely based on paleocurrent studies but lacks adequate sedimentary facies analyses (Goddard, 1992; Krapez, 1996, 1997, 1999; Martin et al., 2000; Krapez et al., 2017 and references therein). The Figure 2 (Krapez et al., 2017, their figure 2) is a generalized stratigraphic succession with inferred depositional environment but surprisingly, without necessary corroborating scientific literature. Herein I have pointed out some sedimentological and stratigraphic issues that deserve closer scrutiny in order to undertake a thorough and critical reassessment of the existing tectonostratigraphic models of the Turee Creek and the Horseshoe basins (Krapez et al., 2017, their fig. 2) as these are essential prerequisite to infer detrital zircon provenance data.
2. Stratigraphy and Sedimentology of the Turee Creek Group i)
Krapez et al. (2017), following the suggestion of Trendall (1979), subdivided the quartz-rich sandstones of the Turee Creek Group into Quartzite 1, Quartzite 2 and Quartzite 3 because these quartzites “best emphasizes that they are unconformity bound depositional sequences”. Surprisingly, they did not explain why they are “unconformity bounded sequence” (Krapez et al., 2017, their fig. 2)? Nor they referred any published literature where this has been explained (Goddard, 1992 has been mentioned in p. 71 which is an unpublished B.Sc honors dissertation). As pointed out by Krapez et al.
(2017), the Turee Creek Group of the Hardey Syncline area was formally divided by Thorne et al. (1995; see also Trendall, 1981) and this division is indeed well justified (Figs. 1, 2). I believe that the lithostratigraphic subdivision of the Turee Creek Group, as recommended by Trendall, 1981 and Thorne et al. (1995), is more appropriate as this is devoid of any ambiguity. Recent high resolution sedimentary facies analysis (Van Kranendonk and Mazumder, 2015; Van Kranendonk et al., 2015; Mazumder et al., 2015; Martindale et al., 2015) also support the stratigraphic scheme proposed by Thorne et al (1995).
ii)
Krapez et al (2017) accepted Koolbye Formation as the formal name of Quartzite 1 and also a fluvial interpretation of their Quartzite 1/Koolbye Formation. It is surprising that they have cited but did not mention that a marine (Fig. 3) to fluvial transition within the Koolbye Formation has been documented by Mazumder et al (2015). To clarify, on the southern limb of the Hardey Syncline (501993N, 7465956E; see Mazumder et al., 2015, their fig. 2), the Koolbye Formation is made of four distinct quartzite (sandstone) ridges separated by fine-grained sandstone-siltstone assemblage (Fig. 4). Here, the Koolbye Formation sandstone conformably overlies the greenish Kungarra Formation shale and is conformably overlain by the Kazput Formation. The transition from tidal flat to beach-aeolian to fluvial depositional environment within the Koolbye Formation indicates a falling stage systems tract (Mazumder et al., 2015). Recent sedimentological facies
analysis clearly reveal at least three falling stage systems tracts within the Kungarra and Koolbye Formations of the Turee Creek Group (Van Kranendonk and Mazumder, 2015; Van Kranendonk et al., 2015; Mazumder et al., 2015). Krapez et al (2017) mentioned about “local unconformity” between Quartzite 1/Koolbye Formation and the Kazput Formation but did not mention why the contact is unconformable and the area where it is exposed. There is no such unconformity between the Koolbye and Kazput Formations in the Hardey Syncline area (Mazumder et al., 2015). iii)
Krapez et al (2017) interpreted Quartzite 2 and Quartzite 3 as fluvial and deltaic deposits respectively solely on the basis of paleocurrent patterns published by earlier researchers (Goddard, 1992; Martin et al., 2000; the stratigraphic levels from which paleocurrent data were collected as well as the sedimentary facies characteristics are largely unknown) without any sedimentological facies analysis. While presenting stratigraphy of the Hardey syncline (Krapez et al., 2017, their figures 6 and 10), they have cited Krapez, (1996, 1999) and Goddard, (1992) and mentioned lithology and sedimentary structures preserved in Quartzites 2 and 3 very briefly. These papers (Krapez, 1996, 1999) are devoid of any field photograph of sedimentary facies but contains a few long measured sections. Thus the inferred depositional settings of Quartzites 2 and 3 are ambiguous. Additionally, Krapez et al (2017, p. 75) assumed that the paleocurrent data presented by Van Kranendonk et al (2015) “were not corrected for tectonic folding”. Krapez et al (2017) did not notice that the results of paleocurrent analysis undertaken
by Van Kranendonk et al (2015) have been presented in their tables 2 and 3 (Van Kranendonk et al., 2015, p. 322 and p. 338) and all the field data are corrected for tectonic folding, following standard methodologies (Ramsay, 1961). It must be noted that all earlier researchers (except Van Kranendonk et al., 2015 and Mazumder et al., 2015) have undertaken paleocurrent analysis without classifying the Turee Creek sedimentary successions into depositional facies and facies associations (cf. Reinick and Singh, 1980; Reading, 1997); ambiguous sedimentary environmental interpretation is therefore an obvious consequence.
3. Stratigraphy and Sedimentology of Horseshoe basin i)
According to Krapez et al (2017), the Horseshoe basin succession (their Horseshoe Supersequence) is made up of the Beasley River Quartzite, the Cheela Springs Basalt and the Wooly Dolomite (Krapez et al., 2017, their fig. 2). The base of the Beasley River Quartzite is indeed an unconformity (Trendall, 1979; Morris, 1980, 1985; Mazumder and Van Kranendonk, 2015). Previous researchers used the lithostratigraphic unit “Lower Wyloo Group” and informally divided the Lower Wyloo Group succession into Beasley River Quartzite and Cheela Springs Basalt which is unconformably overlain by the Upper Wyloo Group (Powell and Horwitz, 1994). The Beasley River Quartzite succession starts with the classic Three Corners Conglomerate which is successively overlain by the sandstone-shale-tuff assemblage, a thick quartzrich sandstone and the Nummana Member (Mazumder and Van Kranendonk, 2013, 2014; Figs. 5-7). The Three Corners Conglomerate is very distinct and
exposed over a large area (Trendall, 1979; Powell and Horwitz, 1994; Van Kranendonk, 2010; Mazumder and Van Kranendonk, 2013, 2014), especially in the Hardy Syncline as well as in the Horseshoe Creek (Figs. 5, 6A). Krapez et al. (2017, their fig. 2, 11) did not mention about the Three Corners Conglomerate while discussing the stratigraphic characteristics of the Beasley River Quartzite but shown in one of the compiled map (Krapez et al., 2017, their fig. 12). Krapez et al. (2017, their fig.15) have shown a considerably thicker quartzolithic conglomerate - quartzsose sandstone association and following the suggestions of previous researchers, have accepted a fluvial origin. Fig. 5 presents a measured section across the Turee Creek - Lower Wyloo Group transition in the Horseshoe Creek region (see Fig. 1; GPS location: N480292, E7474826; Mazumder and Van Kranendonk, 2014). Here the greenish Shale of the Kungarra Formation is unconformably overlain by the
Three
Corners
Conglomerate
(Fig.
6A).
The
Three
Corners
Conglomerate is consists of largely subrounded to rounded, pebble to cobblesized clasts (Fig. 6A) set in a coarse sandy matrix. Clasts are poorly to moderately sorted and locally define crude nearly horizontal stratification. Clasts are mostly made up of banded iron formation, chert and quartz in a coarse sandy matrix. The Three Corners Conglomerate has been interpreted as alluvial fan deposit (Mazumder and Van Kranendonk, 2014). This is overlain by a laterally extensive and thick medium-to fine sandstone with extensive parallel lamination, heavy mineral zonation and local reverse
grading (Fig. 6B-E), indicating a near shore coastal (beach) depositional setting (Mazumder and Van Kranendonk, 2014). This sandstone is overlain by a fining upward conglomerate-sandstone-shale assemblage (Fig. 7). Unlike the Three Corners Conglomerate, this conglomerate is made up largely of angular chert pebbles (Fig. 7A). At places a crude stratification is found. The conglomerate passes gradationally upward into medium grained sandstone and then to shale (Figs. 7A-B). The sandstones are either massive or cross bedded and are overlain by rippled sandstone facies (Fig. 7B). No wave generated sedimentary structures are found in this facies association. Mazumder and Van Kranendonk (2013) have presented a detailed facis analysis of this facies association from the southern limb of the Hardey syncline and have inferred a fluvial depositional environment. In the Horseshoe Creek area, this fluvial facies association is overlain by the Cheela Springs basalt. As documented in Figs. 5-7, there are two distinct conglomeratic horizons, having distinct sedimentological characteristics in the Beasley River Quartzite. As Krapez et al., (2017) did not provide necessary sedimentological data, it is difficult to infer whether the conglomeratesandstone assemblage of Krapez et al. (2017, their fig. 15) is part of the Three Corners Conglomerate-sandstone association or the overlying conglomerate-sandstone–shale association of the fluvial facies association (Fig. 5). ii)
While reassessing the sedimentologic and stratigraphic characteristics of the Beasley River Quartzite, Krapez et al. (2017) commented that the proportion
of finer-grained sedimentary rocks increases upward the succession is mixed fluvial and shallow marine in origin. They have commented “Mazumder and Van Kranendonk (2013) argued inconclusively for aeolian sedimentary structures”. This comment clearly shows that they did not critically read the Mazumder and Van Kranendonk (2013) paper. Fig. 8 represents a detailed measured section on the southern limb of the Hardey Syncline (Fig. 1) (see Mazumder and Van Kranendonk (2013) for detailed sedimentary facies analysis of the braided fluvial and aeolian facies associations). Mazumder and Van Kranendonk (2013) have presented very convincing aeolian dune and interdune (translatent strata and adhesion features) deposits (Fig. 9A-E). Additionally, the sandstones that bear these sedimentary structures are characterized by well-rounded quartz grains (Fig. 9C). Surprisingly, Krapez et al (2017) did not mention why and how the argument of Mazumder and Van Kranendonk (2013) for aeolian origin for these sedimentary structures are “inconclusive. I believe Krapez et al (2017), following the speculation of earlier researchers (Thorne and Seymour, 1986, 1991; Martin et al., 2000), prefer to infer these sedimentary deposits as shallow marine (the Nummana Member?).
4. Tectonic setting Krapez et al (2017) claimed “That the Turee Creek Group relates to a compressive basin (the Turee Creek Basin of Krapez, 1996) is not in doubt”. It must be noted that the Turee Creek Group was interpreted to have been deposited in a foreland basin (the McGrath Trough) (Horwitz, 1982, 1987; Krapez, 1996, 1997; Martin, 1999;
Martin et al., 2000). Van Kranendonk et al (2015) have discussed the problematic aspects with the foreland basin model. Detailed sedimentary facies analysis and mode of stratigraphic sequence building of the Kungarra Formation indicate its generation in an intracratonic rift basin. There is no evidence of of thrusting within the Kungarra and Koolbye Formations (Van Kranendonk et al., 2015; Mazumder et al., 2015). Martindale et al. (2015) reported numerous cm to dm scale synsedimentary normal faults and inferred an active extensional setting during the Kazput sedimentation. As pointed out by Van Kranendonk et al. (2015), the detrital zircon record from the Meteorite Bore Member (see Takehara et al., 2010) is inconsistent with the patterns documented from the foredeeps, especially a dominance of juvenile zircons from accreted and uplifted arc (see Martin et al., 2008). The metamorphic grade of the Turee Creek Group of rocks is very low to low (Smith et al., 1982). Krapez et al. (2017) did not address these issues which are highly incompatible with a foreland setting. The sedimentation pattern, volcanism and the mode of stratigraphic sequence development clearly indicate Lower Wyloo Group was formed in an intracontinental rift setting (Mazumder and Van Kranendonk, 2013; see also Krapez et al., 2017, their Horseshoe Supersequence). Thus, the alternative model is that the entire Turee Creek as well as the Wyloo Group formed in an intracratonic rift basin. It is interesting to note that the zircon age spectra of both the Turee Creek Basin and the Horseshoe basin are very similar although the age of youngest zircon modes are different (Krapez et al., 2017).
5. Conclusions
The reassessment of Paleoproterozoic tectonostratigraphic history across the Hamersley and Ashburton provinces as undertaken by Krapez et al (2017) is not compatible with recent sedimentologic and stratigraphic analysis (Van Kranendonk et al., 2015; Van kranendonk and Mazumder, 2015; Mazumder et al., 2015; Martindale et al., 2015). These recent studies strongly contradict the previously inferred foreland tectonic setting for the Turee Creek Group of rocks. A critical reassessment of the existing tectonostratigraphic model from a process based sedimentology is an essential prerequisite for interpreting detrital zircon provenance of the Paleoproterozoic successions of Western Australia. Acknowledgements I am grateful to the University of New South Wales, Sydney for a postdoctoral fellowship (2012-2013) and subsequently, a Research Fellowship (2014) for undertaking part of this research. I am grateful to M.J. Van Kranendonk for his enthusiasm, support and guidance in the field and to M.R. Walter and A. Knoll for motivation and encouragement. Matthew Aikins provided very helpful assistance in the field during the 2013 winter field season. Curtin University Malaysia provided necessary infrastructural facilities and partial financial support to continue pending research work.
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Farquhar, J., Bao, H.M., and Thiemens, M., 2000, Atmospheric influence of Earth’s earliest sulfur cycle: Science, 289, 756–758. Goddard, A.B., 1992. The depositional style and tectonic setting of the Early Proterozoic Turee Creek Group in the Hardey Syncline, Hamersley Province, Northwestern Australia. BSc Honours Dissertation, University of Western Australia, Perth, 117 pp. Holland, H.D., 2002. Volcanic gases, black smokers, and the Great Oxidation Event. Geochim. Cosmochim. Acta 66, 3811–3826. Horwitz, R.C., 1982. Geological history of the Early Proterozoic Paraburdoo hinge zone, Western Australia. Precambrian Res. 19, 191–200. Horwitz, R.C., 1987. Structural Trends of the Archaean to Lower Proterozoic Hamersley Province, Western Australian Shield. CSIRO Division of Minerals and Geochemistry, Report MG31. Kirschvink, J.L., Gaidos, E.J., Bertani, L.E., Beukes, N.J., Gutzmer, J., Maepa, L.N., Steinberger, R.E., 2000. Paleoproterozoic snowball Earth: extreme climatic and geochemical global change and its biological consequences. Proc. Natl. Acad. Sci. U. S. A. 97, 1400–1405. Krapez, B., 1996. Sequence-stratigraphic concepts applied to the identification of basin filling rhythms in Precambrian successions. Aust. J. Earth Sci. 43, 355-380. Krapez, B., 1997. Sequence-stratigraphic concepts applied to the identification of depositional basins and global tectonic cycles. Aust. J. Earth Sci. 44, 1-36. Krapez, B., 1999. Stratigraphic record of an Atlantic-type global tectonic cycle in the Palaeoproterozoic Ashburton Province of Western Australia. Aust. J. Earth
Sci. 46, 71-87. Krapež, B., Müller, S.G., Fletcher, I.R., Rasmussen, B. 2017. A tale of two basins? Stratigraphy and detrital zircon provenance of the Palaeoproterozoic Turee Creek and Horseshoe Basins of Western Australia, Precambrian Research, 294, 67-90. doi: http://dx.doi.org/10.1016/j.precamres.2017.03.020
Martin, D. M. 1999. Depositional setting and implications of Paleoproterozoic glacio marine sedimentation in the Hamersley Province, Western Australi. Geological Society America Bulletin, 111, 189–203
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Martin, D.M, Powell, C.M., George, A.D. 2000. Stratigraphic architecture and evolution of the early Paleoproterozoic McGrath Trough, Western Australia: Precambrian Research, 99, 33–64. Martin, D.McB., Sircombe, K.N., Thorne, A.M., Cawood, P.C., Nemchin, A.A., 2008. Provenance history of the Bangemall Supergroup and implications for the Mesoproterozoic paleogeography of the West Australian Craton. Precambrian Res.166, 93–110. Martindale, R.C., Strauss, J.V., Sperling, E.A., Johnson, J.E, van Kranendonk, M., Flannery, D., French, K., Lepot, K. Mazumder, R., Rice, M.A., Schrag, D. P.
Summons, R. Walter, M., Abelson, J, Knoll. A. H. 2015. Sedimentology, chemostratigraphy and stromatolites of lower Paleoproterozoic carbonates, Turee Creek Group, Western Australia. Precambrian Research, 266, 194-211. Mazumder, R., Van Kranendonk, M.J. 2013. Paleoproterozoic terrestrial sedimentation in the the Beasley River Quartzite, Lower Wyloo Group, Western Australia. Precambrian Research, 231, 98-105. Mazumder, R., Van Kranendonk, M.J. 2014. Paleoproterozoic sedimentation and contemporary basin tectonics in the Lower Wyloo Group, Western Australia. The Australian Earth Science Convention, Newcastle, 8th July paper 02REP03. Mazumder, R., Van Kranendonk, M. J., Altermann, W. 2015. A marine to fluvial transition in the Paleoproterozoic Koolbye Formation, Turee Creek Group, Western Australia. Precambrian Research, 258, 161-170. Morris, R.C. 1980. A textural and mineralogical study of the relationship of iron ore to banded iron-formation in the Hamersley iron province of Western Australia. Economic Geology, 75, 184-209.
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Thorne, A.M. 1991. Ashburton Basin, in Geology and mineral resources of Western Australia: Geological Survey of Western Australia, Memoir 3, 210–219. Thorne, A.M., Seymour, D.B., 1986. The sedimentology of a tide-influenced fan-delta system in the Early Proterozoic Wyloo Group, on the southern margin of the Pilbara Craton, Western Australia. Prof. Pap. 1984, West. Aust. Geol. Surv., Report 19, 70-82. Thorne, A.M., Seymour, D.B., 1991. Geology of the Ashburton Basin Western Australia: Geological Survey of Western Australia, Bulletin, pp. 139.
Thorne, A.M., Tyler, I.M., Hunter, W.M., 1991. Explanatory notes: Turee Creek, Western Australia Sheet SF50-15, Geological Survey of Western Australia. Thorne, A.M., Tyler, I.M., Blight, D.F., 1995. Rocklea, Western Australia, Geological Survey of Western Australia, 1:100 000 Geological Series. Trendall, A.F. 1979. A revision of the Mount Bruce Supergroup: Geological Survey of Western Australia, Annual Report 1978, p. 63–71. Trendall, A.F., 1981, The Lower Proterozoic Meteorite Bore Member, Hamersley Basin, Western Australia, in Hambrey, M.J., and Harland, W.B., eds., Earth's prePleistocene glacial record: Cambridge University Press, Cambridge, p. 555–557. Van Kranendonk M.J., Mazumder, R. 2015.Two glacio-eustatic cycles in the Paleoproterozoic Turee Creek Group, Western Australia. Bulletin Geological Society of America, doi 10.1130/B31025.1. Van Kranendonk, M. J., Mazumder, R., Yamaguchi, K. E., Yamada, K., Ikehara, M. 2015.Sedimentology of the Paleoproterozoic Kungarra Formation, Turee Creek Group, Western Australia: A conformable record of the transition from early to modern Earth. Precambrian Research, 256, 314-343.
Figure Captions: Figure 1. Geological map of the Hardey Syncline, showing the lithostratigraphic units of the Turee Creek Group and the Lower Wyloo Group of rocks (modified after Van Kranendonk et al., 2015).
Figure 2. Generalized stratigraphy of the Turee Creek Group of rocks in the Hardey Syncline area (after Trendall, 1981; Thorne et al., 1995 and Van kranendonk and Mazumder, 2015). Figure 3. Koolbye sandstone: (A) Nearly straight crested ripples with tuning fork like bifurcation formed on tidal flat (B) Herringbone cross-stratification (see Mazumder et al., 2015 for details) Figure 4.
A 105m thick measured section through the Koolbye Formation on the
southern limb of the Hardey Syncline (501993N, 7465956E) showing the marine to fluvial transition within the Koolbye Formation (see Mazumder et al., 2015, their fig. 2 for the lithounits of the Koolbye Formation). Figure 5. Measured section showing the stratigraphic relationship between the Turee Creek and the Lower Wyloo Groups in the Horseshoe Creek (Fig. 1; GPS location: N480292, E7474826). Figure 6. The alluvial fan-nearshore (beach) facies association of the Beasley River Quartzite in the Horseshoe Creek locality (see Fig. 5 caption for the GPS location): (A) the Three Corners Conglomerate (B) Decimeter-thick, extensive monotonous parallel to low angle stratification bearing sandstone (C) Heavy mineral layering within the parallel laminated sandstone (D) Inversely graded sandstone (E) Photomicrograph showing inverse grading. Figure 7. Fluvial facies association of the Beasley River Quartzite in the Horseshoe Creek area (GPS location mentioned in Fig. 5 caption); (A) Conglomerate-sandstoneshale association (B) cross-bedded sandstone overlain by strongly asymmetric rippled
sandstone. The facies constituents of the fluvial facies association of the Beasley River Quartzite has been discussed in detail by Mazumder and Van Kranendonk (2013) from the southern limb of the Hardey Syncline. Figure 8. Detailed measured section through the quartz-rich sandstone of the Beasley River Quartzite on the southern limb of the Hardey Syncline (see Fig. 1 for location of the section). Stratigraphic position of various aeolian sedimentary facies constituents are also indicated by their respective figure numbers (A-E) (after Mazumder and Van Kranendonk, 2013). Figure 9. Sedimentary features from the aeolian facies association: (A) Large scale aeolian dune facies; (B) Wind streaks preserved on the bedding plane of the aeolian dune facies; (C) Photomicrograph of fine-grained quartz-rich sandstone with pin-stripe lamination; note rounded to well-rounded quartz grains; (D) Fine-grained sandstone with spectacular pin-stripe lamination;arrows indicate dark colored, fine-grained laminae; (E) Adhesion feature preserved on the bedding plane of the fine grained sandstone (after Mazumder and Van Kranendonk, 2013; see the paper for a detailed description of aeolian features and corroborative scientific literature).
116o 50 l
116o 55 l
117o 00 l
0
36
Ho
rse
22o 50 l
1
117o 05 l
2
3
4
5 km
N
sh
45
oe
Creek 65
Nan
utar
ra
50
50
Upper Wyloo Group
HGp
Turee Creek Gp
Three Corners Congl Mbr Kazput Fm
unconformity
27
50 bedding
30
67
anticline
Koolbye Fm
syncline
Meteorite Bore Mbr Kungarra Fm
fault
Boolgeeda Iron Fm Hammersley Group undivided
r ve Ri
30 1
measured section
116o 50 l
22o 55 l
70 ley
Sandstone, shale, tuff
65
30
Para 116o 55 l
burd
as
Quartz-rich sandstone
34
oo
Be
Nummana Mbr
Beasley River Quartzite
lower Wyloo Gp
Dolerite Cheela Springs Basalt
117o 00 l
117o 05 l
BRQ CSB MBM
Kungarra Fm
KF
Kazput Fm
Lr. Wyloo Gr. Turee Creek Group
2.20 Ga
CSB – Cheela Springs Basalt BRQ – Beasley River Quartzite KF – Kungarra Formation MBM – Meteorite Bore Member BIF – Boolgeeda Iron Formation WR – Woongarra Rhyolite
WR BIF
Hamersley Gr.
Kungarra Fm.
Rhyolite Basalt Dolerite Unconformity Stromatolitic dolostone Dolostone Marl Mudstone-siltstone Sandstone-siltstone Sandstone Sandstone-conglomerate Diamictite Banded Iron Formation 2.45 Ga
A
B
100 m
Fluvial deposit
80 m
Beach-aeolian deposit
60 m
Large scale cross bedded medium-grained sandstone Massive medium-grained sandstone Parallel laminated medium-grained sandstone Cross bedded medium-grained sandstone Fine-grained sandstone/ siltstone
40 m
Tidal deposit
20 m
n = 30
0m
fs ms
Cheela Spring Basalt 5m
Turee creek Group
n=9
Beasley River
0
silt
sf
sm
sc conglo
( fluvial) ( nearshore beach)
0m
( alluvial fan)
m.
Quartzite
n=5 50
Exposure gap Cheela Spring Basalt Shale Penecontemporaneously deformed sandstone Medium grained cross laminated sandstone Medium grained massive to plane laminated sandstone conglomerate Unconformity
A
B
D
C
E
Top
A
B
interdune
45 m
AEOLIAN
floodplain channel system
FLUVIAL
interdune dune
AEOLIAN
n=4
Fluvial facies Association cross-stratified medium grained sandstone
flood plain
Trough cross-bedded medium grained sandstone
FLUVIAL
Parallel laminated fine grained sandstone
30 m
n=4
Current rippled fine grained sandstone Medium grained massive sandstone Compound cross-bedded medium grained sandstone Penecontemporaneously deformed medium grained sandstone
channel system
Pebbly sandstone with rounded mud chips Aeolian facies association Dune Translatent strata/Pinstripe lamination/ Adhesion structures (Interdune)
dune 9E
interdune
9C,D
interdune dune interdune
9B 9A
AEOLIAN
dune
15 m
dune n=8
interdune
n=7
channel system
n=6 n=5
0m Fsst
Msst C/Pbsst
bar
FLUVIAL
floodplain
A
B
C
D
E
S0301-9268(17)30315-7 http://dx.doi.org/10.1016/j.precamres.2017.06.026 PRECAM 4808
To appear in:
Precambrian Research
Received Date: Revised Date: Accepted Date:
5 June 2017 12 June 2017 29 June 2017
Please cite this article as: R. Mazumder, A tale of two basins? Stratigraphy and detrital zircon provenance of the Paleoproterozoic Turee Creek and Horseshoe basins of Western Australia: Discussion, Precambrian Research (2017), doi: http://dx.doi.org/10.1016/j.precamres.2017.06.026
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A tale of two basins? Stratigraphy and detrital zircon provenance of the Paleoproterozoic Turee Creek and Horseshoe basins of Western Australia: Discussion Rajat Mazumder Department of Applied Geology, Faculty of Engineering and Science, Curtin University Malaysia, CDT 250, Miri 98009, Malaysia. E-mail: [email protected] Tel: +6085 630100 (extension 2520)
1. Introduction The Archean - Paleoproterozoic transition is associated with the rise of atmospheric oxygen (the Great Oxidation event, GOE, 2.45-2.22 Ga; Holland, 2002; Bekker et al., 2004), global glaciation, consequent flourishing of eukaryotic life and paleobiological evolution (Kirschvink et al., 2000; Farquhar et al., 2000). In significant contrast to the other cratonic blocks of the world, the Pilbara craton, Western Australia documents a near continuous depositional record across the GOE within the conformable succession of almost entirely marine Turee Creek Group of rocks (Martin, 1999; Van Kranendonk and Mazumder, 2015; Van Kranendonk et al., 2015) and therefore is unique (Fig. 1). Notwithstanding this, the stratigraphic sequence development and depositional model of the Turee Creek Group and the unconformably overlying Lower Wyloo Group is a matter of conjecture because of inadequate sedimentological facies analysis (Thorne et al., 1991; Krapez, 1996, 1997; Martin et al., 2000; Krapez et al., 2017). Krapez et al (2017) have made an attempt to reassess the existing tectonostratigraphic history of the Pilbara craton during 2.45-2.0 Ga supplemented by detrital zircon provenance study. Although their detrital zircon data is new and significant, they did not provide any new sedimentologic and stratigraphic data and tried to fit the detrital zircon provenance data in the existing foreland tectonostratigraphic model (the Turee Creek basin), without critically analyzing alternative intracontinental rift model recently
suggested by Van kranendonk et al. (2015), Van kranendonk and Mazumder, 2015, and Mazumder et al., 2015. Krapez et al (2017) have cited these papers and made some statements, quoting Mazumder and Van Kranendonk (2013) and Van Kranendonk et al. (2015), which clearly indicates that they have not read the paper critically (discussed below). Krapez et al. (2017) relied heavily on conjectural stratigraphic model that is largely based on paleocurrent studies but lacks adequate sedimentary facies analyses (Goddard, 1992; Krapez, 1996, 1997, 1999; Martin et al., 2000; Krapez et al., 2017 and references therein). The Figure 2 (Krapez et al., 2017, their figure 2) is a generalized stratigraphic succession with inferred depositional environment but surprisingly, without necessary corroborating scientific literature. Herein I have pointed out some sedimentological and stratigraphic issues that deserve closer scrutiny in order to undertake a thorough and critical reassessment of the existing tectonostratigraphic models of the Turee Creek and the Horseshoe basins (Krapez et al., 2017, their fig. 2) as these are essential prerequisite to infer detrital zircon provenance data.
2. Stratigraphy and Sedimentology of the Turee Creek Group i)
Krapez et al. (2017), following the suggestion of Trendall (1979), subdivided the quartz-rich sandstones of the Turee Creek Group into Quartzite 1, Quartzite 2 and Quartzite 3 because these quartzites “best emphasizes that they are unconformity bound depositional sequences”. Surprisingly, they did not explain why they are “unconformity bounded sequence” (Krapez et al., 2017, their fig. 2)? Nor they referred any published literature where this has been explained (Goddard, 1992 has been mentioned in p. 71 which is an unpublished B.Sc honors dissertation). As pointed out by Krapez et al.
(2017), the Turee Creek Group of the Hardey Syncline area was formally divided by Thorne et al. (1995; see also Trendall, 1981) and this division is indeed well justified (Figs. 1, 2). I believe that the lithostratigraphic subdivision of the Turee Creek Group, as recommended by Trendall, 1981 and Thorne et al. (1995), is more appropriate as this is devoid of any ambiguity. Recent high resolution sedimentary facies analysis (Van Kranendonk and Mazumder, 2015; Van Kranendonk et al., 2015; Mazumder et al., 2015; Martindale et al., 2015) also support the stratigraphic scheme proposed by Thorne et al (1995).
ii)
Krapez et al (2017) accepted Koolbye Formation as the formal name of Quartzite 1 and also a fluvial interpretation of their Quartzite 1/Koolbye Formation. It is surprising that they have cited but did not mention that a marine (Fig. 3) to fluvial transition within the Koolbye Formation has been documented by Mazumder et al (2015). To clarify, on the southern limb of the Hardey Syncline (501993N, 7465956E; see Mazumder et al., 2015, their fig. 2), the Koolbye Formation is made of four distinct quartzite (sandstone) ridges separated by fine-grained sandstone-siltstone assemblage (Fig. 4). Here, the Koolbye Formation sandstone conformably overlies the greenish Kungarra Formation shale and is conformably overlain by the Kazput Formation. The transition from tidal flat to beach-aeolian to fluvial depositional environment within the Koolbye Formation indicates a falling stage systems tract (Mazumder et al., 2015). Recent sedimentological facies
analysis clearly reveal at least three falling stage systems tracts within the Kungarra and Koolbye Formations of the Turee Creek Group (Van Kranendonk and Mazumder, 2015; Van Kranendonk et al., 2015; Mazumder et al., 2015). Krapez et al (2017) mentioned about “local unconformity” between Quartzite 1/Koolbye Formation and the Kazput Formation but did not mention why the contact is unconformable and the area where it is exposed. There is no such unconformity between the Koolbye and Kazput Formations in the Hardey Syncline area (Mazumder et al., 2015). iii)
Krapez et al (2017) interpreted Quartzite 2 and Quartzite 3 as fluvial and deltaic deposits respectively solely on the basis of paleocurrent patterns published by earlier researchers (Goddard, 1992; Martin et al., 2000; the stratigraphic levels from which paleocurrent data were collected as well as the sedimentary facies characteristics are largely unknown) without any sedimentological facies analysis. While presenting stratigraphy of the Hardey syncline (Krapez et al., 2017, their figures 6 and 10), they have cited Krapez, (1996, 1999) and Goddard, (1992) and mentioned lithology and sedimentary structures preserved in Quartzites 2 and 3 very briefly. These papers (Krapez, 1996, 1999) are devoid of any field photograph of sedimentary facies but contains a few long measured sections. Thus the inferred depositional settings of Quartzites 2 and 3 are ambiguous. Additionally, Krapez et al (2017, p. 75) assumed that the paleocurrent data presented by Van Kranendonk et al (2015) “were not corrected for tectonic folding”. Krapez et al (2017) did not notice that the results of paleocurrent analysis undertaken
by Van Kranendonk et al (2015) have been presented in their tables 2 and 3 (Van Kranendonk et al., 2015, p. 322 and p. 338) and all the field data are corrected for tectonic folding, following standard methodologies (Ramsay, 1961). It must be noted that all earlier researchers (except Van Kranendonk et al., 2015 and Mazumder et al., 2015) have undertaken paleocurrent analysis without classifying the Turee Creek sedimentary successions into depositional facies and facies associations (cf. Reinick and Singh, 1980; Reading, 1997); ambiguous sedimentary environmental interpretation is therefore an obvious consequence.
3. Stratigraphy and Sedimentology of Horseshoe basin i)
According to Krapez et al (2017), the Horseshoe basin succession (their Horseshoe Supersequence) is made up of the Beasley River Quartzite, the Cheela Springs Basalt and the Wooly Dolomite (Krapez et al., 2017, their fig. 2). The base of the Beasley River Quartzite is indeed an unconformity (Trendall, 1979; Morris, 1980, 1985; Mazumder and Van Kranendonk, 2015). Previous researchers used the lithostratigraphic unit “Lower Wyloo Group” and informally divided the Lower Wyloo Group succession into Beasley River Quartzite and Cheela Springs Basalt which is unconformably overlain by the Upper Wyloo Group (Powell and Horwitz, 1994). The Beasley River Quartzite succession starts with the classic Three Corners Conglomerate which is successively overlain by the sandstone-shale-tuff assemblage, a thick quartzrich sandstone and the Nummana Member (Mazumder and Van Kranendonk, 2013, 2014; Figs. 5-7). The Three Corners Conglomerate is very distinct and
exposed over a large area (Trendall, 1979; Powell and Horwitz, 1994; Van Kranendonk, 2010; Mazumder and Van Kranendonk, 2013, 2014), especially in the Hardy Syncline as well as in the Horseshoe Creek (Figs. 5, 6A). Krapez et al. (2017, their fig. 2, 11) did not mention about the Three Corners Conglomerate while discussing the stratigraphic characteristics of the Beasley River Quartzite but shown in one of the compiled map (Krapez et al., 2017, their fig. 12). Krapez et al. (2017, their fig.15) have shown a considerably thicker quartzolithic conglomerate - quartzsose sandstone association and following the suggestions of previous researchers, have accepted a fluvial origin. Fig. 5 presents a measured section across the Turee Creek - Lower Wyloo Group transition in the Horseshoe Creek region (see Fig. 1; GPS location: N480292, E7474826; Mazumder and Van Kranendonk, 2014). Here the greenish Shale of the Kungarra Formation is unconformably overlain by the
Three
Corners
Conglomerate
(Fig.
6A).
The
Three
Corners
Conglomerate is consists of largely subrounded to rounded, pebble to cobblesized clasts (Fig. 6A) set in a coarse sandy matrix. Clasts are poorly to moderately sorted and locally define crude nearly horizontal stratification. Clasts are mostly made up of banded iron formation, chert and quartz in a coarse sandy matrix. The Three Corners Conglomerate has been interpreted as alluvial fan deposit (Mazumder and Van Kranendonk, 2014). This is overlain by a laterally extensive and thick medium-to fine sandstone with extensive parallel lamination, heavy mineral zonation and local reverse
grading (Fig. 6B-E), indicating a near shore coastal (beach) depositional setting (Mazumder and Van Kranendonk, 2014). This sandstone is overlain by a fining upward conglomerate-sandstone-shale assemblage (Fig. 7). Unlike the Three Corners Conglomerate, this conglomerate is made up largely of angular chert pebbles (Fig. 7A). At places a crude stratification is found. The conglomerate passes gradationally upward into medium grained sandstone and then to shale (Figs. 7A-B). The sandstones are either massive or cross bedded and are overlain by rippled sandstone facies (Fig. 7B). No wave generated sedimentary structures are found in this facies association. Mazumder and Van Kranendonk (2013) have presented a detailed facis analysis of this facies association from the southern limb of the Hardey syncline and have inferred a fluvial depositional environment. In the Horseshoe Creek area, this fluvial facies association is overlain by the Cheela Springs basalt. As documented in Figs. 5-7, there are two distinct conglomeratic horizons, having distinct sedimentological characteristics in the Beasley River Quartzite. As Krapez et al., (2017) did not provide necessary sedimentological data, it is difficult to infer whether the conglomeratesandstone assemblage of Krapez et al. (2017, their fig. 15) is part of the Three Corners Conglomerate-sandstone association or the overlying conglomerate-sandstone–shale association of the fluvial facies association (Fig. 5). ii)
While reassessing the sedimentologic and stratigraphic characteristics of the Beasley River Quartzite, Krapez et al. (2017) commented that the proportion
of finer-grained sedimentary rocks increases upward the succession is mixed fluvial and shallow marine in origin. They have commented “Mazumder and Van Kranendonk (2013) argued inconclusively for aeolian sedimentary structures”. This comment clearly shows that they did not critically read the Mazumder and Van Kranendonk (2013) paper. Fig. 8 represents a detailed measured section on the southern limb of the Hardey Syncline (Fig. 1) (see Mazumder and Van Kranendonk (2013) for detailed sedimentary facies analysis of the braided fluvial and aeolian facies associations). Mazumder and Van Kranendonk (2013) have presented very convincing aeolian dune and interdune (translatent strata and adhesion features) deposits (Fig. 9A-E). Additionally, the sandstones that bear these sedimentary structures are characterized by well-rounded quartz grains (Fig. 9C). Surprisingly, Krapez et al (2017) did not mention why and how the argument of Mazumder and Van Kranendonk (2013) for aeolian origin for these sedimentary structures are “inconclusive. I believe Krapez et al (2017), following the speculation of earlier researchers (Thorne and Seymour, 1986, 1991; Martin et al., 2000), prefer to infer these sedimentary deposits as shallow marine (the Nummana Member?).
4. Tectonic setting Krapez et al (2017) claimed “That the Turee Creek Group relates to a compressive basin (the Turee Creek Basin of Krapez, 1996) is not in doubt”. It must be noted that the Turee Creek Group was interpreted to have been deposited in a foreland basin (the McGrath Trough) (Horwitz, 1982, 1987; Krapez, 1996, 1997; Martin, 1999;
Martin et al., 2000). Van Kranendonk et al (2015) have discussed the problematic aspects with the foreland basin model. Detailed sedimentary facies analysis and mode of stratigraphic sequence building of the Kungarra Formation indicate its generation in an intracratonic rift basin. There is no evidence of of thrusting within the Kungarra and Koolbye Formations (Van Kranendonk et al., 2015; Mazumder et al., 2015). Martindale et al. (2015) reported numerous cm to dm scale synsedimentary normal faults and inferred an active extensional setting during the Kazput sedimentation. As pointed out by Van Kranendonk et al. (2015), the detrital zircon record from the Meteorite Bore Member (see Takehara et al., 2010) is inconsistent with the patterns documented from the foredeeps, especially a dominance of juvenile zircons from accreted and uplifted arc (see Martin et al., 2008). The metamorphic grade of the Turee Creek Group of rocks is very low to low (Smith et al., 1982). Krapez et al. (2017) did not address these issues which are highly incompatible with a foreland setting. The sedimentation pattern, volcanism and the mode of stratigraphic sequence development clearly indicate Lower Wyloo Group was formed in an intracontinental rift setting (Mazumder and Van Kranendonk, 2013; see also Krapez et al., 2017, their Horseshoe Supersequence). Thus, the alternative model is that the entire Turee Creek as well as the Wyloo Group formed in an intracratonic rift basin. It is interesting to note that the zircon age spectra of both the Turee Creek Basin and the Horseshoe basin are very similar although the age of youngest zircon modes are different (Krapez et al., 2017).
5. Conclusions
The reassessment of Paleoproterozoic tectonostratigraphic history across the Hamersley and Ashburton provinces as undertaken by Krapez et al (2017) is not compatible with recent sedimentologic and stratigraphic analysis (Van Kranendonk et al., 2015; Van kranendonk and Mazumder, 2015; Mazumder et al., 2015; Martindale et al., 2015). These recent studies strongly contradict the previously inferred foreland tectonic setting for the Turee Creek Group of rocks. A critical reassessment of the existing tectonostratigraphic model from a process based sedimentology is an essential prerequisite for interpreting detrital zircon provenance of the Paleoproterozoic successions of Western Australia. Acknowledgements I am grateful to the University of New South Wales, Sydney for a postdoctoral fellowship (2012-2013) and subsequently, a Research Fellowship (2014) for undertaking part of this research. I am grateful to M.J. Van Kranendonk for his enthusiasm, support and guidance in the field and to M.R. Walter and A. Knoll for motivation and encouragement. Matthew Aikins provided very helpful assistance in the field during the 2013 winter field season. Curtin University Malaysia provided necessary infrastructural facilities and partial financial support to continue pending research work.
References: Bekker, A., Holland, H.D., Wang, P.L., Rumble III, D., Stein, H.J., Hannah, J.L.,Coetzee, L.L., Beukes, N.J., 2004. Dating the rise of atmospheric oxygen. Nature 427, 117–120.
Farquhar, J., Bao, H.M., and Thiemens, M., 2000, Atmospheric influence of Earth’s earliest sulfur cycle: Science, 289, 756–758. Goddard, A.B., 1992. The depositional style and tectonic setting of the Early Proterozoic Turee Creek Group in the Hardey Syncline, Hamersley Province, Northwestern Australia. BSc Honours Dissertation, University of Western Australia, Perth, 117 pp. Holland, H.D., 2002. Volcanic gases, black smokers, and the Great Oxidation Event. Geochim. Cosmochim. Acta 66, 3811–3826. Horwitz, R.C., 1982. Geological history of the Early Proterozoic Paraburdoo hinge zone, Western Australia. Precambrian Res. 19, 191–200. Horwitz, R.C., 1987. Structural Trends of the Archaean to Lower Proterozoic Hamersley Province, Western Australian Shield. CSIRO Division of Minerals and Geochemistry, Report MG31. Kirschvink, J.L., Gaidos, E.J., Bertani, L.E., Beukes, N.J., Gutzmer, J., Maepa, L.N., Steinberger, R.E., 2000. Paleoproterozoic snowball Earth: extreme climatic and geochemical global change and its biological consequences. Proc. Natl. Acad. Sci. U. S. A. 97, 1400–1405. Krapez, B., 1996. Sequence-stratigraphic concepts applied to the identification of basin filling rhythms in Precambrian successions. Aust. J. Earth Sci. 43, 355-380. Krapez, B., 1997. Sequence-stratigraphic concepts applied to the identification of depositional basins and global tectonic cycles. Aust. J. Earth Sci. 44, 1-36. Krapez, B., 1999. Stratigraphic record of an Atlantic-type global tectonic cycle in the Palaeoproterozoic Ashburton Province of Western Australia. Aust. J. Earth
Sci. 46, 71-87. Krapež, B., Müller, S.G., Fletcher, I.R., Rasmussen, B. 2017. A tale of two basins? Stratigraphy and detrital zircon provenance of the Palaeoproterozoic Turee Creek and Horseshoe Basins of Western Australia, Precambrian Research, 294, 67-90. doi: http://dx.doi.org/10.1016/j.precamres.2017.03.020
Martin, D. M. 1999. Depositional setting and implications of Paleoproterozoic glacio marine sedimentation in the Hamersley Province, Western Australi. Geological Society America Bulletin, 111, 189–203
Martin, D.M., Morris, P. 2010. Tectonic setting and regional implications of ca. 2.2 Ga mafic magmatism in the southern Hamersley province, Western Australia. Australian Journal of Earth Sciences, 57, 911-931.
Martin, D.M, Powell, C.M., George, A.D. 2000. Stratigraphic architecture and evolution of the early Paleoproterozoic McGrath Trough, Western Australia: Precambrian Research, 99, 33–64. Martin, D.McB., Sircombe, K.N., Thorne, A.M., Cawood, P.C., Nemchin, A.A., 2008. Provenance history of the Bangemall Supergroup and implications for the Mesoproterozoic paleogeography of the West Australian Craton. Precambrian Res.166, 93–110. Martindale, R.C., Strauss, J.V., Sperling, E.A., Johnson, J.E, van Kranendonk, M., Flannery, D., French, K., Lepot, K. Mazumder, R., Rice, M.A., Schrag, D. P.
Summons, R. Walter, M., Abelson, J, Knoll. A. H. 2015. Sedimentology, chemostratigraphy and stromatolites of lower Paleoproterozoic carbonates, Turee Creek Group, Western Australia. Precambrian Research, 266, 194-211. Mazumder, R., Van Kranendonk, M.J. 2013. Paleoproterozoic terrestrial sedimentation in the the Beasley River Quartzite, Lower Wyloo Group, Western Australia. Precambrian Research, 231, 98-105. Mazumder, R., Van Kranendonk, M.J. 2014. Paleoproterozoic sedimentation and contemporary basin tectonics in the Lower Wyloo Group, Western Australia. The Australian Earth Science Convention, Newcastle, 8th July paper 02REP03. Mazumder, R., Van Kranendonk, M. J., Altermann, W. 2015. A marine to fluvial transition in the Paleoproterozoic Koolbye Formation, Turee Creek Group, Western Australia. Precambrian Research, 258, 161-170. Morris, R.C. 1980. A textural and mineralogical study of the relationship of iron ore to banded iron-formation in the Hamersley iron province of Western Australia. Economic Geology, 75, 184-209.
Morris, R.C. 1985. Genesis of iron ore in banded iron formation by supergene and supergene-metamorphic processes: A conceptual model. In: Wolf, K.H. (ed.) Handbook of strata-bound and stratiform ore deposits. Amsterdam, Elsevier Science Publications, 13, 73-235. Powell, C.M., Horwitz, R.C., 1994. L ate Archaean and Early Proterozoic Tectonics and basin formation of the Hamersley Ranges: Australian Geological
Convention, Geological Society of Australia (WA Division), 12th, Perth,1994, Excursion Guidebook, 57 p. Ramsay, J.G., 1961. The effects of folding upon the orientation of sedimentary structures. Journal of Geology, 69, 84–100. Reading, H.G. 1997. Sedimentary Environments: Processes, Facies and Stratigraphy, 3rd Edition, Wiley, 704p. Reineck, H.E., Singh, I.B. 1980. Depositional Sedimentary Environments, Springer. Smith, R.E., Perdrix, J.L., Parks, J.C., 1982. Burial metamorphism in the Hamersley province, Western Australia. J. Petrol. 23, 75–102. Takehara, M. Komure, S. Kiyoakawa, K. Horie, K. Yokoyama 2010. Detrital zircon SHRIMP U–Pb age of 2.3 Ga diamictites of the Meteorite Bore Member in south Pilbara Western Australia In: I.M. Tyler, C.M. Knox-Robinson (Eds.), Fifth International Archean Symposium Abstracts, Geological Survey of Western Australia Record 2010/18, pp. 223–224.
Thorne, A.M. 1991. Ashburton Basin, in Geology and mineral resources of Western Australia: Geological Survey of Western Australia, Memoir 3, 210–219. Thorne, A.M., Seymour, D.B., 1986. The sedimentology of a tide-influenced fan-delta system in the Early Proterozoic Wyloo Group, on the southern margin of the Pilbara Craton, Western Australia. Prof. Pap. 1984, West. Aust. Geol. Surv., Report 19, 70-82. Thorne, A.M., Seymour, D.B., 1991. Geology of the Ashburton Basin Western Australia: Geological Survey of Western Australia, Bulletin, pp. 139.
Thorne, A.M., Tyler, I.M., Hunter, W.M., 1991. Explanatory notes: Turee Creek, Western Australia Sheet SF50-15, Geological Survey of Western Australia. Thorne, A.M., Tyler, I.M., Blight, D.F., 1995. Rocklea, Western Australia, Geological Survey of Western Australia, 1:100 000 Geological Series. Trendall, A.F. 1979. A revision of the Mount Bruce Supergroup: Geological Survey of Western Australia, Annual Report 1978, p. 63–71. Trendall, A.F., 1981, The Lower Proterozoic Meteorite Bore Member, Hamersley Basin, Western Australia, in Hambrey, M.J., and Harland, W.B., eds., Earth's prePleistocene glacial record: Cambridge University Press, Cambridge, p. 555–557. Van Kranendonk M.J., Mazumder, R. 2015.Two glacio-eustatic cycles in the Paleoproterozoic Turee Creek Group, Western Australia. Bulletin Geological Society of America, doi 10.1130/B31025.1. Van Kranendonk, M. J., Mazumder, R., Yamaguchi, K. E., Yamada, K., Ikehara, M. 2015.Sedimentology of the Paleoproterozoic Kungarra Formation, Turee Creek Group, Western Australia: A conformable record of the transition from early to modern Earth. Precambrian Research, 256, 314-343.
Figure Captions: Figure 1. Geological map of the Hardey Syncline, showing the lithostratigraphic units of the Turee Creek Group and the Lower Wyloo Group of rocks (modified after Van Kranendonk et al., 2015).
Figure 2. Generalized stratigraphy of the Turee Creek Group of rocks in the Hardey Syncline area (after Trendall, 1981; Thorne et al., 1995 and Van kranendonk and Mazumder, 2015). Figure 3. Koolbye sandstone: (A) Nearly straight crested ripples with tuning fork like bifurcation formed on tidal flat (B) Herringbone cross-stratification (see Mazumder et al., 2015 for details) Figure 4.
A 105m thick measured section through the Koolbye Formation on the
southern limb of the Hardey Syncline (501993N, 7465956E) showing the marine to fluvial transition within the Koolbye Formation (see Mazumder et al., 2015, their fig. 2 for the lithounits of the Koolbye Formation). Figure 5. Measured section showing the stratigraphic relationship between the Turee Creek and the Lower Wyloo Groups in the Horseshoe Creek (Fig. 1; GPS location: N480292, E7474826). Figure 6. The alluvial fan-nearshore (beach) facies association of the Beasley River Quartzite in the Horseshoe Creek locality (see Fig. 5 caption for the GPS location): (A) the Three Corners Conglomerate (B) Decimeter-thick, extensive monotonous parallel to low angle stratification bearing sandstone (C) Heavy mineral layering within the parallel laminated sandstone (D) Inversely graded sandstone (E) Photomicrograph showing inverse grading. Figure 7. Fluvial facies association of the Beasley River Quartzite in the Horseshoe Creek area (GPS location mentioned in Fig. 5 caption); (A) Conglomerate-sandstoneshale association (B) cross-bedded sandstone overlain by strongly asymmetric rippled
sandstone. The facies constituents of the fluvial facies association of the Beasley River Quartzite has been discussed in detail by Mazumder and Van Kranendonk (2013) from the southern limb of the Hardey Syncline. Figure 8. Detailed measured section through the quartz-rich sandstone of the Beasley River Quartzite on the southern limb of the Hardey Syncline (see Fig. 1 for location of the section). Stratigraphic position of various aeolian sedimentary facies constituents are also indicated by their respective figure numbers (A-E) (after Mazumder and Van Kranendonk, 2013). Figure 9. Sedimentary features from the aeolian facies association: (A) Large scale aeolian dune facies; (B) Wind streaks preserved on the bedding plane of the aeolian dune facies; (C) Photomicrograph of fine-grained quartz-rich sandstone with pin-stripe lamination; note rounded to well-rounded quartz grains; (D) Fine-grained sandstone with spectacular pin-stripe lamination;arrows indicate dark colored, fine-grained laminae; (E) Adhesion feature preserved on the bedding plane of the fine grained sandstone (after Mazumder and Van Kranendonk, 2013; see the paper for a detailed description of aeolian features and corroborative scientific literature).
116o 50 l
116o 55 l
117o 00 l
0
36
Ho
rse
22o 50 l
1
117o 05 l
2
3
4
5 km
N
sh
45
oe
Creek 65
Nan
utar
ra
50
50
Upper Wyloo Group
HGp
Turee Creek Gp
Three Corners Congl Mbr Kazput Fm
unconformity
27
50 bedding
30
67
anticline
Koolbye Fm
syncline
Meteorite Bore Mbr Kungarra Fm
fault
Boolgeeda Iron Fm Hammersley Group undivided
r ve Ri
30 1
measured section
116o 50 l
22o 55 l
70 ley
Sandstone, shale, tuff
65
30
Para 116o 55 l
burd
as
Quartz-rich sandstone
34
oo
Be
Nummana Mbr
Beasley River Quartzite
lower Wyloo Gp
Dolerite Cheela Springs Basalt
117o 00 l
117o 05 l
BRQ CSB MBM
Kungarra Fm
KF
Kazput Fm
Lr. Wyloo Gr. Turee Creek Group
2.20 Ga
CSB – Cheela Springs Basalt BRQ – Beasley River Quartzite KF – Kungarra Formation MBM – Meteorite Bore Member BIF – Boolgeeda Iron Formation WR – Woongarra Rhyolite
WR BIF
Hamersley Gr.
Kungarra Fm.
Rhyolite Basalt Dolerite Unconformity Stromatolitic dolostone Dolostone Marl Mudstone-siltstone Sandstone-siltstone Sandstone Sandstone-conglomerate Diamictite Banded Iron Formation 2.45 Ga
A
B
100 m
Fluvial deposit
80 m
Beach-aeolian deposit
60 m
Large scale cross bedded medium-grained sandstone Massive medium-grained sandstone Parallel laminated medium-grained sandstone Cross bedded medium-grained sandstone Fine-grained sandstone/ siltstone
40 m
Tidal deposit
20 m
n = 30
0m
fs ms
Cheela Spring Basalt 5m
Turee creek Group
n=9
Beasley River
0
silt
sf
sm
sc conglo
( fluvial) ( nearshore beach)
0m
( alluvial fan)
m.
Quartzite
n=5 50
Exposure gap Cheela Spring Basalt Shale Penecontemporaneously deformed sandstone Medium grained cross laminated sandstone Medium grained massive to plane laminated sandstone conglomerate Unconformity
A
B
D
C
E
Top
A
B
interdune
45 m
AEOLIAN
floodplain channel system
FLUVIAL
interdune dune
AEOLIAN
n=4
Fluvial facies Association cross-stratified medium grained sandstone
flood plain
Trough cross-bedded medium grained sandstone
FLUVIAL
Parallel laminated fine grained sandstone
30 m
n=4
Current rippled fine grained sandstone Medium grained massive sandstone Compound cross-bedded medium grained sandstone Penecontemporaneously deformed medium grained sandstone
channel system
Pebbly sandstone with rounded mud chips Aeolian facies association Dune Translatent strata/Pinstripe lamination/ Adhesion structures (Interdune)
dune 9E
interdune
9C,D
interdune dune interdune
9B 9A
AEOLIAN
dune
15 m
dune n=8
interdune
n=7
channel system
n=6 n=5
0m Fsst
Msst C/Pbsst
bar
FLUVIAL
floodplain
A
B
C
D
E