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Glacial Geology Near Mcmurdo Sound and Comparison with the Central Transantarctic Mountains Paul Andrew Mayewski University of Maine, [email protected]

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Glacial Geology Near Mcmurdo Sound and Comparison with the Central Transantarctic Mountains Paul Andrew Mayewski University of Maine, Paul.Mayewski@Maine.Edu The University of Maine DigitalCommons@UMaine Earth Science Faculty Scholarship Earth Sciences 7-1972 Glacial Geology Near McMurdo Sound and Comparison with the Central Transantarctic Mountains Paul Andrew Mayewski University of Maine, [email protected] Follow this and additional works at: https://digitalcommons.library.umaine.edu/ers_facpub Part of the Glaciology Commons, Hydrology Commons, and the Sedimentology Commons Repository Citation Mayewski, Paul Andrew, "Glacial Geology Near McMurdo Sound and Comparison with the Central Transantarctic Mountains" (1972). Earth Science Faculty Scholarship. 209. https://digitalcommons.library.umaine.edu/ers_facpub/209 This Article is brought to you for free and open access by DigitalCommons@UMaine. It has been accepted for inclusion in Earth Science Faculty Scholarship by an authorized administrator of DigitalCommons@UMaine. For more information, please contact [email protected]. river level to the tops of the ice wedges. The remain­ et al., 1970; and 0.6 million years, Behling, 1971 ). ing 90 centimeters of fill above is ice free, and the This past season, the authors located an abundance of transition from ice wedge to sand wedge is abrupt. basaltic bombs on the surface of an Alpine II lateral The sand-wedges capping the ice are of coarse and moraine of Meserve Glacier. These should provide a fine sand (figs. 1 and 2), little different from alluvium minimum age for the Alpine II glacial event if the in one wedge and noticeably finer in another. material proves satisfactory for potassium-argon A feature of the overlying alluvial fan surface is the dating. The Alpine II event is known to have oc­ total lack of disturbance of any kind. No polygonal curred after an eruptive event dated at 2.5 to 3.4 ground is present at the surface, despite the presence million years (our interpretation of a potassium-argon of open cracks in ice at depth. This implies wedge age by Dr. Robert Fleck, in Behling, 1971). growth and decay prior to fan development. Adjacent The evidence suggests that the ice wedges are no to the fan, large, well developed polygons occur, and longer active, being totally deprived of a viable mois­ all surface cracks show signs of recent collapse of sand ture source. Degradation of the ice-cemented layer into them. There is no difference in the amount of and ice wedges with simultaneous replacement of ice water available to these two areas, and the margins wedge by sand infilling has produced sand casts of the of the fan clearly can be seen to overlap the wedged former ice wedges. At least some of the abundant surface. sand wedges in the dry valley area must be degraded The contrast in surface between the fan and the ice wedges, and many are of great antiquity. surrounding area would be less striking if the well­ This work was supported by National Science Foun­ developed lag gravel surface on the alluvial fan did dation grant GV-28804. not also possess many good ventifacts, demonstrating that it too is of considerable age. The degree of References faceting of the lag gravel and the apparent source Behling, R . E. 19 71. Chemical weathering in Wright of the fan strongly suggest that the alluvial fan over­ Valley. Antarctic' Journal of the U.S., VI(5): 214-215. lying the Onyx River alluvium is of Alpine II age Calkin, P. E., R. E. Behling, and C. Bull. 19 70. Glacial (Calkin et al., 1970) . history of Wright Valley, southern Victoria Land, Antarc­ Alpine II materials are considered to be of the order tica. Antarctic Journal of the U.S., V ( 1) : 22- 27. of 0.5 million years in age. Current estimates of the age are trending upward (0.5 million years, Calkin - Glacial geology near McMurdo Sound and comparison with the central Transantarctic Mountains P. A.MAYEWSKI Institute of Polar Studies The Ohio State University Work begun in 1970-1 971 in the central Trans­ antarctic Mountains from camps at McGregor and Amundsen Glaciers (Elliott and Coates, 1971) was extended during December 1971 and January 1972 into the ice-free areas between Mount Feather and the Convoy Range (fig. 1). Six tent camps were es­ tablished during the 1971-1972 season : transport and reconnaissance were supplied by the VXE-6 helicop­ ters, and the author was assisted in the field by Robert S. Wilkinson. Glacial geologic results of the 1970-1971 season were twofold. Three systems of lateral moraines were differentiated within each of the valleys of the Shackleton, Amundsen, and Scott Glaciers as part of a broad geologic mapping program. Also, new infor­ mation was collected about the Sirius Formation, as M . J. M cSaueney named by Mercer (in press). The semilithified Sirius Fig ure 2. Ice wedge beneath coarse-sand wedge to left of blade Formation is composed of two parts-a lower massive of ice axe till and an upper mixture of massive till and stratified July-August 1972 103 0 o 78°5 7 °S 160 E Q P Figure 1 lIeftl. Locations of the Sirius Formation in the McMurdo Sound region . ., ~ Figure 2 (righll. Locations of the Sirius Formation in the central Transantarctic Mountains. McMurdo Sound • Sirius Fm. Location 165"E lenses. The Sirius Formation occurs stratigraphically This nomenclature holds in the areas of the Shackle­ below and topographically above the lateral moraines ton, Amundsen, and Scott Glaciers and can be ex­ mentioned above, thus predating them. tended to the lateral moraines of the adjacent The principal objective of the 1971 -1972 season Beardmore Glacier where they can be referred to involved searching for a semilithified till equivalent formally, for example in the Beardmore Glacier, as to the Sirius Formation. In the central Transantarctic the Beardmore H igh Moraine, the Beardmore Mid­ Mountains, the Sirius Formation is almost exclusively dle Moraine, and the Beardmore Low Moraine. A confined to elevations above 2000 meters. Correspond­ map of this area is being prepared. ing areas above 2000 meters in the McMurdo region The low moraines of the Shackleton, Amundsen, include the ice-free hills west of the valleys between and Scott Glaciers include deposits up to 30 meters Mount Feather and the Convoy Range. Five outcrops above the present ice surface. The profiles of the low of semilithified till in this area (fig. 1 and table 1) moraines parallel present ice profiles. This system were found that are believed to be equivalent to shows evidence of a minor readvance, in the form of the Sirius Formation of the central Transantarctic a push moraine, 10 to 20 meters above the present Mountains (fig. 2 and table 2). ice surface. R esults of the 1970-1971 and 1971-1972 seasons. Longitudinal profiles of the high and middle mo­ In the central Transantarctic Mountains three sys­ raines (fig. 3) in the 1970-197 1 study area imply tems of lateral moraines were differentiated by the synchronous and marked thickening of both the pla­ degree of weathering of surficial boulders, by the teau ice at the heads of the glaciers and of the outlet degree of soil development (Everett and Behling, glaciers themselves. The long profiles of the high and 1970) and by their elevations. These three moraine middle moraines roughly parallel present ice slopes systems are called, from oldest to youngest, the high from the heads of the glaciers to within 65 to 80 moraine, the middle moraine, and the low moraine. kilometers of the Ross Ice Shelf, but then flatten 104 ANTARCTIC JOURNAL 145°W 155°W 165°W 87°5175°W 175°E 86°5 j;,Mt r;, Howe ~9 87°5 . '" ~ock C1 Roaring 'Ot> Volley "0 ~tWisting \l , Devils Glacier Mt Hassel ':" Ro th 83°5 ICE SHE L F R 0 S S • Sirius Fm Location 85°5 145°W 155°W 165°W 84°5 175°W 83°5 175°E Table 1. Sites of the Sirius Formation Table 2. Sites of the Sirus Formation in the in the McMurdo region. central Transantarctic Mountains. Location (first observed by) Elevation at top of deposit (meters) Elevation at top of deposit t* Mt. Feather (D. Elliot, pers. comm.) 2,800 Location (first observed by) (meters) Area t* Shapeless Mts. (P. Barrett, pers. comm.) 2,400 t* Coombs Hills (P. Barrett, pers. comm.) 1,900 t* Dominion Range (Oliver, 1964) 2,200 B t*O Carapace Nunatak (H. Borns and 2,000> t* Otway Massif (D. Elliot, pers. comm.) 2,400 B B. Hall, pers. comm.) t Mount Sirius (Barrett, 1969) 2,300 B t* Allan Nunatak (H. Borns and B. Hall, 1,750 t Mount Deakin (S. Etter and D. Coates, 2,800 B pers. comm.) pers. comm.) t* Mount Block (D. Elliot, pers comm.) 2,700 B t* Roberts Massif (Wade et al., 1965) 2,100 S Symbols for tables 1 and 2. * Dismal Buttress (Wade et at., 1965) 2,300 S Half Century Nunatak 2,600 S * site investigated by this author t* Bennett Platform (Wade et ai., 1965) 2,150 S t sample obtained by this author t Mount Roth (E. Stump and 800 S o deposit not in situ V. Wendland, pers. comm.) deposit questionable ot* Mount Wisting 2,000 " A B Beardmore Glacier area Mount Blackburn area (Doumani and S Shackleton Glacier area Minshew, 1965) 3,000 Sc A Amundsen Glacier area Mount Saltonstall (Doumani and Sc Scott Glacier area ° Minshew, 1965) 2,200 Sc 0 Mount Innes-Taylor (Doumani and markedly toward the coast. The flattening may imply Minshew, 1965) 2,200 Sc grounding of the Ross Ice Shelf, possibly as suggested by Hollin (1962). Thus, evidence suggesting that the consists of both a lower massive till and an upper Ross Ice Shelf was grounded exists in the McMurdo assemblage of interlayered till and stratified lenses.
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