Late Proterozoic Tectonics in the Prydz Bay AreaEntry ID: ASAC_519
Abstract: From the abstracts of some of the referenced papers:
The East Antarctic mobile belt as exposed in Prydz Bay presents an excellent example of a poly-metamorphic terrain where complicated high-grade structures can be grouped on the basis of lineation direction, sense of shear and metamorphic grade. In this way local intricacies resulting from truncating and interfering foliations and ... folds can be simplified by ordering structures with respect to their kinematic connotation. The resulting deformation scheme is simple and facilitates regional correlations, and simultaneously places metamorphic textures in a kinematic-structural background.
The mobile belt in Prydz Bay is exposed along 200km of coastline, and consists of granulite-facies gneiss in which low- to mid-crustal, compressional D1-2 structures, and mid- to upper-crustal, extensional D3-6 structures and related decompression cooling textures are best explained in an exhumation model involving extensional collapse of upper crust in an overall compressional tectonic setting. This implies that compression and extension structures are genetically related. However, D3-6 structures in the Larsemann Hills appear to have formed between 550 and 500 Ma, whilst D2 structures in the Rauer Group have been dated at 1100-1000 Ma. Reinterpretation of the latter dates is possible, implying that most high-grade deformation in Prydz Bay is early Palaeozoic.
Meta-sediments in the Larsemann Hills that preserve a coherent stratigraphy, form a cover sequence deposited upon basement of mafic-felsic granulite. Their outcrop pattern defines a 10 kilometre wide east-west trending synclinal trough structure in which basement-cover contacts differ in the north and the south, suggesting tectonic interleaving during a prograde, D1, thickening event. Subsequent conditions reached low-medium pressure granulite grade, and structures can be divided into two groups, D2 and D3, each defined by a unique lineation direction and shear sense. D2 structures which are associated with the dominant gneissic foliation in much of the Larsemann Hills, contain a moderately east-plunging lineation indicative of west-directed thrusting. D2 comprises a co-linear fold sequence that evolved from early intrafolial folds to late upright folds. D3 structures are associated with a high-strain zone, to the south of the Larsemann Hills, where S3 is the dominant gneissic layering and folds sequences resemble D2 folding. Outside the D3 high-strain zone occurs a low-strain D3 window, preserving low-strain D3 structures (minor shear bands and upright folds) that partly re-orient D2 structures. All structures are truncated by a series of planar pegmatites and parallel D4 mylonite zones, recording extensional dextral displacements.
D2 assemblages include coexisting garnet-orthopyroxene pairs recording peak conditions of ~ 7 kbar and ~ 780 degrees C. Subsequent retrograde decompression textures partly evolved during both D2 and D3 when conditions of ~ 4-5 kbar and ~750 degrees C were attained. This is followed by D4 shear zones which formed around 3 kbar and ~550 degrees C.
It is tempting to combine D2-4 structures in one tectonic cycle involving prograde thrusting and thickening followed by retrograde extension and uplift. The available geochronological data, however, present a number of interpretations. For example, D2 was possibly associated with a clockwise P-T path at medium pressures around ~1000Ma, by correlation with similar structures developed in the Rauer Group, whilst D3 and D4 events occurred in response to extension and heating at low pressures at ~550 Ma, associated with the emplacement of numerous granitoid bodies. Thus, decompression textures typical for the Larsemann Hills granulites maybe the combined effect of two separate events.
The Larsemann Hills represent a low-pressure granulite terrain with a complex structural-metamorphic history that comprises two parts: 1) granulite facies D1 structures transposed within an early form surface that probably formed at 1000 Ma, and 2) a sequence of progressive, upper amphibolite to lower granulite facies D2-D6 structures that formed during the Pan-African at 500 Ma and were associated with the emplacement of granites and pegmatites with high-grade alteration zones. D2-D6 events comprise an early form surface that has been tightly folded and sheared twice after which it was warped and transected by discrete mylonites. D2-D6 assembalges are associated with decompression textures on D1 peak-assemblages, such as cordierite coronas on garnet + sillimanite in metapelite and plagioclase coronas on garnet in metabasite. This suggests that D2-D6 formed at slightly lower pressures than D1 structures. However, the spatial correlation between the coronas and alteration zones around pegmatitc intrusives indicates that the apparent decompression textures may have partly resulted from transient fluxes in water pressure following melt crystallisation. Throughout East Antarctica tectonic provinces have been recognised in which the 1000 Ma tectonothermal events are identified as the main stage in the evolution, and Pan-African events are dismissed as a minor thermal overprint. Although the Larsemann Hills are small in area, they are representative of a great many granulite terrains in East Antarctica, and suggest that great care is needed in the structural-metamorphic analysis of such terrains to ensure the separation of tectonic stages before an interpretation of the tectonic path is attempted.
Start Date: 1991-09-30Stop Date: 1994-03-31
Paleo Temporal Coverage
Paleo Start Date: 1100 Ma
Paleo Stop Date: 500 Ma
ISO Topic Category
Quality Values provided in temporal and spatial coverage are approximate only.
Access Constraints PDF copies of three of the referenced papers (Carson et al 1995, Dirks and Wilson 1995, Dirks et al 1993) are available for download from the provided URL.
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Role: TECHNICAL CONTACT
Phone: +61 3 9344 6538
Fax: +61 3 9344 7761
Email: c.wilson at earthsci.unimelb.edu.au
School of Earth Sciences University of Melbourne
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Postal Code: 3052
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Phone: +61 3 6232 3244
Fax: +61 3 6232 3351
Email: dave.connell at aad.gov.au
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Carson C.J., Dirks P.G.H.M., Hand M., Sims J.P., Wilson C.J.L. (1995) Compressional and extensional tectonics in low-medium pressure granulites from the Larsemann Hills, East Antarctica. Geological Magazine 132(2). 151-170
Dirks P.H.G.M., Wilson C.J.L. (1995) Crustal evolution of the East Antarctic mobile belt in Prydz Bay: continental collision at 500 Ma? Precambrian Research 75. ... 189-207
Stuwe K., Braun H.-M., Peer H. (1989) Geology and structure of the Larsemann Hills area, Prydz Bay, East Antarctica Australian Journal of Earth Sciences 36. 219-241
Stuwe K., Hand M. (1992) Geology and structure of Depot Peak, MacRobertson Land. More evidence for the continuous extent of the 1000 Ma event of East Antarctica. Australian Journal of Earth Sciences 39. 211-222
Dirks P.H.G.M., Hoek J.D., Wilson C.J.L., Sims J. (1994) The Proterozoic deformation of the Vestfold Hills Block, East Antarctica: implications for the tectonic development of adjacent granulite belts. Precambrian Research 65. 277-295
Dirks P.H.G.M., Carson C.J., Wilson C.J.L. (1993) The deformational history of the Larsemann Hills, Prydz Bay: the importance of the Pan-African (500 Ma) in East Antarctica. Antarctic Science 5(2). 179-192
Hand M., Dirks P., Buick I., Powell R. (1992) How well established is isobaric cooling in Proterozoic metamorphic belts. Geology 14. 649
Carson C.J., Fanning C.M., Wilson C.J.L. (1996) Timing of the Progress Granite, Larsemann Hills: additional evidence for Early Palaeozoic orogenesis within the east Antarctic Shield and implications for Gondwana assembly. Australian Journal of Earth Science 43. 539-553
Dirks P.H.G.M., Hand M. (1994) Clarifying P-T paths via structures in granulite from the Bolingen Islands, Antarctica. Australian Journal of Earth Science 42. 157-172
Carson C. (1992) Geochemical aspects of mafic dykes in the Prydz Bay area, East Antarctica. SGTSG Meeting, Melbourne, October
Dirks P., Hoek H., Passchier C., Wilson C. (1992) An extensional-compressional tectonic cycle in the late- Proterozoic of East Antarctica: constraints from the Vestfold Hills, Prydz Bay (Abstract). 29th International Geologial Congress, Japan, August Aug.
Dirks P., Passchier C. (1992) The influence of deformation fabrics on the nucleation and growth of shear zones (Abstract). 29th International Geological Congress, Japan 11-6-6. 443
Hoek H., Passchier C. (1991) Carbonate breccias and pseudotachylites, structurally related to alkaline lamprophyre dykes in the Vestfold Hill: A possible Phanerozoic event in the east Antarctic Shield. Sixth International Symposium on Antarctic Earth Sciences, Ranzan-machi, Japan, September
Hoek H., Passchier C. (1991) The Proterozoic evolution of the Vestfold Hills, an Archaean craton in a Proterozoic metamorphic belt, east Antarctic shield. 6th International Symposium on Antarctic Earth Sciences, Ranzan-machi, Japan, September
Sims J. (1992) The relationship of mafic dykes, transpositions and gneissic layering in the Rauer Group, East Antarctica (Abstract). SGTSG Meeting, Melbourne, October
Wilson C., Dirks P. (1992) Structural-metamorphic correlations in Prydz Bay, east Antarctica, or what determines the repeated structural and thermal reactivation of high grade mobile belts? (Abstract). SGTSG Meeting, Melbourne, October
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Creation and Review Dates
DIF Creation Date: 2000-07-31
Last DIF Revision Date: 2014-01-10