Geology of the basement complex, Western Queen Maud Mountains, Antarctica

Wade, F. Alton; Cathey, C.A.

doi:10.1029/ar036p0429

Cited by 11 publications

(4 citation statements)

References 15 publications

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“…The Shackleton Glacier area possesses a strong north-to NWtrending structural grain that is defined by the traces of folds, cleavage and shear zones (McGregor 1965;McGregor & Wade 1969;Stump 1985;Wade & Cathey 1985). The following sections outline our structural analysis in the area that extends from the western side of Shackleton Glacier to the western side of Liv Glacier (Fig.…”

Section: Structure Of the Shackleton Glacier Areamentioning

confidence: 98%

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Structure and timing of transpressional deformation in the Shackleton Glacier area, Ross orogen, Antarctica

Paulsen

Encarnación

Grunow

2004

JGS

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Basement of the Transantarctic Mountains comprises the Ross orogenic belt, a Neoproterozoic to Ordovician mobile belt located along the palaeo-Pacific margin of Gondwana. Our structural analysis of deformation in the Liv Group, a sequence of Cambrian volcanic, volcaniclastic, clastic and carbonate rocks, and nearby plutonic rocks indicates that the Shackleton Glacier area has a polyphase deformation history that includes development of both contractional and strike-slip structures. We describe evidence for synchronous contraction and strike-slip movement, and suggest that the structural suite in this area developed, at least in part, within a sinistral transpressive kinematic regime. Deformation in the Shackleton Glacier area is inferred to be at least in part younger than 505 Ma, based on the deformation of the well-dated Taylor Formation. New 40 Ar/ 39 Ar cooling ages from metamorphosed igneous and sedimentary rocks range from c. 500 to 470 Ma and are interpreted to date orogenic cooling. Based on our structural results, and on consideration of the tectonic environment represented by the Liv Group, we propose that shortening across a subduction-related volcanic arc system caused deformation of the Liv Group and associated plutonic rocks. Oblique convergence and thus, transpression, may have ultimately been related to left-oblique plate subduction.

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Section: Structure Of the Shackleton Glacier Areamentioning

confidence: 98%

“…Geology compiled from Grindley & Laird (1969), McGregor & Wade (1969), Mirsky (1969) and Stump (1992Stump ( ). 1965Stump 1974Stump , 1985Wade 1974;Wade & Cathey 1985). Sedimentary and volcanic rocks of the Taylor, Greenlee and Fairweather formations make up the Liv Group (Stump 1982).…”

Section: Geological Setting Of the Ross Orogenmentioning

confidence: 99%

Structure and timing of transpressional deformation in the Shackleton Glacier area, Ross orogen, Antarctica

Paulsen

Encarnación

Grunow

2004

JGS

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“…4) (Stump, 1982(Stump, , 1985Wade and Cathey, 1986). Zircons from the sample typically have subangular to subrounded shapes with oscillatory and unzoned interiors.…”

Section: Greenlee and Taylor Formations Shackleton Glaciermentioning

confidence: 98%

Detrital mineral ages from the Ross Supergroup, Antarctica: Implications for the Queen Maud terrane and outboard sediment provenance on the Gondwana margin

et al. 2015

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“…Mountains extend from the Byrd Glacier southward to the Scott Glacier (Figure 1). The geology of this area is described in a series of publications based on reconnaissance mapping [e.g., Grindley, 1963Grindley, , 1981Grindley and Warren, 1964;Faure et al, 1968;Mirsky, 1969;Grindley and Laird, 1969;McGregor and Wade, 1969;Laird et al, 1971;Stump, 1976;Wade and Cathey, 1986;Stump et al, 1988]. The Precambrian and Paleozoic stratigraphy is summarized by Stump [1982].…”

Section: The Central Transantarcticmentioning

confidence: 99%

Isotopic structure and tectonics of the central Transantarctic mountains

Borg¹,

DePaolo²,

Smith³

1990

J. Geophys. Res.

144

130

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Regional patterns of Nd, Sr, and O isotopic ratios of ∼500 Ma granitic rocks are used to identify the ages and areal extents of three crustal provinces in the central Transantarctic Mountains. One of the provinces is the edge of the East Antarctic Craton, which isotopic analyses show is composed of Archean rocks thrust over Proterozoic rocks. The other two provinces compose the Beardmore microcontinent, which we deduce was allochthonous to East Antarctica and was emplaced in late Precambrian or early Paleozoic time. Evidence for a former ocean basin between the Beardmore microcontinent and East Antarctica is provided by basalt and gabbro of mid‐ocean ridge character, dated by Sm‐Nd at ∼760 Ma, associated with marine sediments now located at the suture. The granitic rocks formed over a westward‐dipping subduction zone that was active at ∼500 Ma. The East Antarctic Craton is exposed in the Miller Range, which is a tectonic composite of reworked Archean and early Proterozoic material containing ∼500 Ma peraluminous granites with model ages (TDM) of 2.0 Ga, high δ18O (+11 to +12‰) and high initial 87Sr/86Sr (0.7324 to 0.7417). East of the Marsh Glacier the granitic rocks are metaluminous to weakly peraluminous with model ages of 1.3 to 1.8 Ga, high δ18O (+9 to +13‰) and lower 87Sr/86Sr (0.7068 to 0.7191). East of the Shackleton Glacier, gabbro, tonalite, diorite, and granodiorite have low δ18O (+6 to +7‰), low initial 87Sr/86Sr (0.7045 to 0.7059) and high ϵNd (+0.4 to +1.7). These isotopic provinces correspond to differences in age and composition of the middle and lower crust at the time of formation of the granitic magmas. The boundaries of the isotopic provinces also correspond to discontinuities in provenance, lithology, structural style, and grade of metamorphism of prebatholithic metasedimentary rocks. The isotopic data indicate that the granitic magmas were formed mostly by crustal anatexis in the areas west of the Shackleton Glacier. This is typical of early Paleozoic granitic batholiths elsewhere in the world and has led to speculation that subduction was not involved in granitic magmatism at that time of earth history. However, the granitic rocks located west of the Shackleton Glacier, by virtue of their mantle‐like isotopic compositions and their association with metavolcanic rocks, appear to be subduction‐related. The tectonic history deduced for the Gondwana margin, as represented in the central Transantarctic Mountains, began with deposition of sediments on an Atlantic‐type rifted margin at ∼760 Ma. The Beardmore microcontinent was most likely accreted in association with folding of the clastic sedimentary rocks before middle Early Cambrian time (550 Ma). Carbonate sedimentation and volcanism along the eastern margin of the Beardmore microcontinent commenced in Cambrian time. Folding and metamorphism of all older units occurred in late Cambrian time followed by emplacement of granitic rocks at ∼500 Ma.

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Geology of the basement complex, Western Queen Maud Mountains, Antarctica

Cited by 11 publications

References 15 publications

Structure and timing of transpressional deformation in the Shackleton Glacier area, Ross orogen, Antarctica

Structure and timing of transpressional deformation in the Shackleton Glacier area, Ross orogen, Antarctica

Detrital mineral ages from the Ross Supergroup, Antarctica: Implications for the Queen Maud terrane and outboard sediment provenance on the Gondwana margin

Isotopic structure and tectonics of the central Transantarctic mountains

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