The structure and origin of Prydz Bay and MacRobertson Shelf, East Antarctica

Stagg, H.M.J.

doi:10.1016/0040-1951(85)90019-8

Cited by 142 publications

(170 citation statements)

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“…These convert to spatially averaged erosion rates (including areas of cold-based ice) of 0.0011, 0.0022 and 0.0055 mm yr -1 . The lower two of these calculations compares quite well with estimates of glacigenic sediment volume from Prydz Bay where it is estimated that over the past 12-14 Myrs, average erosion rates were between 0.001-0.002 mm yr -1 Cooper et al, 1991;Jamieson et al, 2005;O'Brien et al, 2001;Stagg, 1985). Therefore, the intermediate integration, which corresponds to a maximum erosion rate of 0.2 mm yr -1 , may be a reasonable first estimate.…”

Section: Linking Patterns Of Erosion To Antarctic Chronologysupporting

confidence: 71%

The evolution of the subglacial landscape of Antarctica

Jamieson

Sugden

Hulton

2010

Earth and Planetary Science Letters

135

129

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Section: Linking Patterns Of Erosion To Antarctic Chronologysupporting

confidence: 71%

The evolution of the subglacial landscape of Antarctica

Jamieson

Sugden

Hulton

2010

Earth and Planetary Science Letters

135

129

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“…The first seismic survey in the region was carried out by Australia in Prydz Bay and on the adjacent continental slope in 1982 (Stagg, 1985). Since then, a number of regional seismic surveys have been carried out in Prydz Bay, on the continental margin and in the Enderby Basin, mainly by Japan and Russia.…”

Section: Geophysical Surveysmentioning

confidence: 99%

“…Structuring beneath the outer edge of Prydz Bay is further complicated by the presence of the major N-S trending Prydz Bay Basin (Figure 18), interpreted by Stagg (1985) to be a failed rift at a triple or four-armed junction that contains at least 5 km of Permian and younger sedimentary rocks deposited on the underlying Lambert Graben. The Cretaceous and Cainozoic section shown in Figure 5b has been dated through a direct tie to ODP site 742 and via other seismic lines to ODP Site 741.…”

Section: Continental Margin Rift Crustmentioning

confidence: 99%

“…The deepseismic lines extend from the mid-continental slope northward to oceanic crust and were regularly spaced at approximately 90 km along the margin. Where they are tied to previously recorded multichannel seismic data (TH99 survey; Joshima et al, 2001; Geoscience Australia Survey 33; Stagg, 1985), they allow transects of the margin to be interpreted from the continental shelf out to oceanic crust emplaced during the separation of India and Antarctica in the Cretaceous.…”

Section: Introductionmentioning

confidence: 99%

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Geology of the Continental Margin of Enderby and Mac. Robertson Lands, East Antarctica: Insights from a Regional Data Set

et al. 2004

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In 2001 and 2002, Australia acquired an integrated geophysical data set over the deep-water continental margin of East Antarctica from west of Enderby Land to offshore from Prydz Bay. The data include approximately 7700 km of high-quality, deep-seismic data with coincident gravity, magnetic and bathymetry data, and 37 non-reversed refraction stations using expendable sonobuoys. Integration of these data with similar quality data recorded by Japan in 1999 allows a new regional interpretation of this sector of the Antarctic margin. This part of the Antarctic continental margin formed during the breakup of the eastern margin of India and East Antarctica, which culminated with the onset of seafloor spreading in the Valanginian. The geology of the Antarctic margin and the adjacent oceanic crust can be divided into distinct east and west sectors by an interpreted crustal boundary at approximately 58°E. Across this boundary, the continent-ocean boundary (COB), defined as the inboard edge of unequivocal oceanic crust, steps outboard from west to east by about 100 km. Structure in the sector west of 58°E is largely controlled by the mixed rift-transform setting. The edge of the onshore ArchaeanProterozoic Napier Complex is downfaulted oceanwards near the shelf edge by at least 6 km and these rocks are interpreted to underlie a rift basin beneath the continental slope. The thickness of rift and pre-rift rocks cannot be accurately determined with the available data, but they appear to be relatively thin. The margin is overlain by a blanket of post-rift sedimentary rocks that are up to 6 km thick beneath the lower continental slope. The COB in this sector is interpreted from the seismic reflection data and potential field modelling to coincide with the base of a basement depression at 8.0-8.5 s two-way time, approximately 170 km oceanwards of the shelf-edge bounding fault system. Oceanic crust in this sector is highly variable in character, from rugged with a relief of more than 1 km over distances of 10-20 km, to rugose with low-amplitude relief set on a long-wavelength undulating basement. The crustal velocity profile appears unusual, with velocities of 7.6-7.95 km s )1 being recorded at several stations at a depth that gives a thickness of crust of only 4 km. If these velocities are from mantle, then the thin crust may be due to the presence of fracture zones. Alternatively, the velocities may be coming from a lower crust that has been heavily altered by the intrusion of mantle rocks. The sector east of 58°E has formed in a normal rifted margin setting, with complexities in the east from the underlying structure of the N-S trending Palaeozoic Lambert Graben. The Napier Complex is downfaulted to depths of 8-10 km beneath the upper continental slope, and the margin rift basin is more than 300 km wide. As in the western sector, the riftstage rocks are probably relatively thin. This part of the margin is blanketed by post-rift sediments that are up to about 8 km thick. The interpreted COB in the eastern sector is the...

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“…A similarly thick upper Cretaceous sedimentary sequence is reported from Prydz Bay (Turner & Padley, 1991) and can be envisaged in the Lambert Graben from the geophysical record (e.g., Fedorov et al, 1982). Kinematic indications obtained from the northern PCM (Boger & Wilson, 2003) and geophysical data from Prydz Bay (Stagg, 1985) indicate that also the Cretaceous sedimentation was triggered tectonically.…”

Section: Discussionmentioning

confidence: 89%

Denudation and uplift of the Mawson Escarpment (eastern Lambert Graben, Antarctica) as indicated by apatite fission track data and geomorphological observation

Lisker

Gibson²,

Wilson³

et al. 2007

Open-File Report

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Analysis of three vertical profiles from the southern Mawson Escarpment (Lambert Graben) reveals apatite fission track (AFT) ages ranging from 102±20 to 287±23 Ma and mean lengths of 12.2 to 13.0 µm. Quantitative thermal histories derived from these data consistently indicate onset of slow cooling below 110°C began sometime prior to 300 Ma, and a second stage of rapid cooling from paleotemperatures up to ≤100°C to surface temperatures occurred in the Late Cretaceous -Paleocene. The first cooling phase refers to Carboniferous -Jurassic basement denudation up to 5 km associated with the initial rifting of the Lambert Graben. The presence of the ancient East Antarctic Erosion Surface and rapid Late Cretaceous -Paleocene cooling indicate a second denudational episode during which up to 4.5 km of sedimentary cover rocks were removed, and that is likely linked to the Cretaceous Gondwana breakup between Antarctica and India and subsequent passive continental margin formation.

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The structure and origin of Prydz Bay and MacRobertson Shelf, East Antarctica

Cited by 142 publications

References 6 publications

The evolution of the subglacial landscape of Antarctica

The evolution of the subglacial landscape of Antarctica

Geology of the Continental Margin of Enderby and Mac. Robertson Lands, East Antarctica: Insights from a Regional Data Set

Denudation and uplift of the Mawson Escarpment (eastern Lambert Graben, Antarctica) as indicated by apatite fission track data and geomorphological observation

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