Hostname: page-component-78c5997874-94fs2 Total loading time: 0 Render date: 2024-11-12T21:42:28.323Z Has data issue: false hasContentIssue false
  • English
  • Français

Inland Ice-Sheet Thinning Near Dome C, East Antarctica, Caused by Post-Wisconsinan Sea-Level Rise (Abstract)

Published online by Cambridge University Press:  20 January 2017

Richard B. Alley  and
Ian M. Whillans
Richard B. Alley
Affiliation:
Department of Geology and Mineralogy and Institute of Polar Studies, Ohio State University, Columbus, Ohio 43210, U.S.A.
Ian M. Whillans
Affiliation:
Department of Geology and Mineralogy and Institute of Polar Studies, Ohio State University, Columbus, Ohio 43210, U.S.A.
Rights & Permissions [Opens in a new window]

Abstract

An abstract is not available for this content. As you have access to this content, full HTML content is provided on this page. A PDF of this content is also available in through the ‘Save PDF’ action button.
Type
Abstract
Information
Annals of Glaciology , Volume 5 , 1984 , pp. 199 - 200
Copyright
Copyright © International Glaciological Society 1984

A rise of sea-level causes a wave of thinning to move upglacier on an ice sheet ending in the sea, but near-coastal perturbations must be large to affect inland regions significantly. The ice divide at Dome C, East Antarctica, is calculated to have thinned by 110 m owing to the post-Wisconsinan rise of sea-level but thinning has been only 75 m if the accumulation rate increased by 10% from Wisconsinan to modern values.

These results are obtained using an ice-flow model that explicitly includes longitudinal-deviatoric stresses. We assume two-dimensional power-law creep over a horizontal bed, and take the flow-law parameter and longitudinal-deviatoric stress to be weighted averages over depth. The flow-law equations for longitudinal and shear deformation with exponent equal to 3 are then averaged over thickness by integrating explicitly. The two resulting equations, plus the continuity equation and a bottom-sliding relation, describe nonsteady glacial flow. If the bottom-sliding relation is correctly specified, this model is applicable to all grounded ice.

To model response of the East Antarctic ice sheet to a post-Wisconsinan rise of sea-level, a Wisconsinan-maximum ice sheet is generated with the Reference VialovVialov (1958) profile extending to the edge of the continental shelf. Bottom sliding is assumed to be negligible. Values of the flow-law parameter are chosen so that the Wisconsinan-maximum ice sheet is in steady-state with the accumulation-rate distribution selected. Modern accumulation rate is determined from Reference Bull and QuamBull (1971); Wisconsinan-maximum accumulation rate is taken to be some percentage of the modern value. The model is driven by specified thinning near the present coast from Wisconsinan-maximum to modern thickness, occurring at the same time as sea-level rise; this simulates ice-sheet response to sea-level rise and associated isostatic adjustment. This is a fair representation because sea-level rise causes grounding-line retreat and near-coastal thinning with little time delay (Reference Thomas and BentleyThomas and Bentley 1978).

Model results show that a rise of sea-level causes a wave of thinning to propagate upglacier on an ice sheet in which the terminal position is controlled by sea-level. The wave of thinning is strongly slowed, diffused, and damped as it moves upglacier; thus, perturbations near the coast must be large and have long periods to affect inland regions. Perturbations caused by processes not modeled here, such as delayed isostatic adjustment or small-scale oscillations in sea-level, are smaller and have shorter periods than the perturbation caused by the major post-Wisconsinan sea-level rise; thus, modeling these processes would not alter total calculated thinning in inland regions significantly. Longitudinal stresses are found to be relatively unimportant to the nonsteady response of the East Antarctic ice sheet, but may prove to be important in regions such as ice streams.

For linear thinning near the modern Sabrina Coast (67°00'S 119°30'E) from the Wisconsinan-maximum thickness to the modern thickness caused by sea-level rise between 15 and 5 ka BP (Reference Milliman and EmeryMilliman and Emery 1968) we calculate that the ice sheet near Dome C, East Antarctica, has thinned by 110 m, and that the response is now 70% complete. A sensitivity study shows that, for values chosen within reasonable limits, this result is almost independent of assumed flow-line length for the Wisconsinan-maximum ice sheet and of timing of sea-level rise. The result is also almost independent of reasonable variations in the flow-law parameter, such as would be required if the Wisconsinan-maximum ice sheet were not initially in steady-state.

Accumulation rate probably changed at the close of the Wisconsinan, and calculated values of total thinning are sensitive to assumed accumulation rate. Total post-Wisconsinan thinning at Dome C owing to the combined effects of sea-level rise and of a step change in accumulation rate taking place 15 ka BP are shown in Figure 1, along with various estimates of the change in accumulation rate. The effect after 15 ka of change in accumulation rate is only 90% of that predicted by Reference WhillansWhillans (1981) because in this model the position of the outer edge of the ice sheet is controlled and this limits elevation changes of the ice sheet. For a 10% increase in accumulation rate from Wisconsinan to Holocene values, the ice sheet at Dome C has thinned by 110 m owing to post-Wisconsinan rise in sea-level and has thickened by approximately 35 m owing to post-Wisconsinan increase in accumulation rate, resulting in a total thinning of about 75 m over the last 15 ka.

Fig. 1 Total thickness change at Dome C over the last 15 ka owing to sea-level rise and to a step increase in accumulation rate 15 ka BP. Approximate percentage increases in accumulation rate from Wisconsinan-maximum to modern values are: (1) about 10% increase calculated by John Bolzan (personal communication 1983), (2) little change in accumulation rate, based on microparticle data of Reference Thompson, Mosley-Thompson and PetitThompson and others (1981), (3) 33% increase (Reference Lorius, Raynaud, Petit, Jouzel and MerlivatLorius and others 1984), (4Í 50% increase (Reference RobinRobin 1977).

References

Bull, C B B 1971 Snow accumulation in Antarctica. In Quam, L O (ed) Research in the Antarctic. A symposium presented at the Dallas weeting of the American Association for the Advancement of Science — December. 1368. Washington, DC, American Association for the Advancement of Science: 367–421 Google Scholar
Lorius, C, Raynaud, D, Petit, J-R, Jouzel, J, Merlivat, L 1984 Late-glacial maximum Holocene atmospheric and ice-thickness changes from Antarctic ice-core studies. Annate of Glaciology 5: 88–94 CrossRefGoogle Scholar
Milliman, J D Emery, K O 1968 Sea levels during the past 35,000 years. Science 162(3858): 1121–1123 CrossRefGoogle ScholarPubMed
Robin, G de Q 1977 Ice cores and climatic change. Philosophical Transactions of the Royal Society of London Ser B 208(972): 143–168 Google Scholar
Thomas, R H, Bentley, C R 1978 A model for Holocene retreat of the West Antarctic ice sheet. Quaternary Research 10(2): 150–170 CrossRefGoogle Scholar
Thompson, L G, Mosley-Thompson, E, Petit, J-R 1981 Glaciological interpretation of microparticle concentrations from the French 905-m Dome C, Antarctica core. International Association of Hydrological Sciences Publication 131 (Symposium at Canberra 1979 — Sea Level, Ice and Climatic Change): 227–234 Google Scholar
Vialov, S S 1958 Regularities of glacial shields movement and the theory of plastic viscous flow. International Association of Scientific Hydrology Publication 47 (Symposium of Chamonix — Physics of the Motion of Ice): 266–275 Google Scholar
Whillans, I M 1981 Reaction of the accumulation zone portions of glaciers to climatic change. Journal of Geophysical Research 86(C5): 4274–4282 CrossRefGoogle Scholar
Figure 0

Fig. 1 Total thickness change at Dome C over the last 15 ka owing to sea-level rise and to a step increase in accumulation rate 15 ka BP. Approximate percentage increases in accumulation rate from Wisconsinan-maximum to modern values are: (1) about 10% increase calculated by John Bolzan (personal communication 1983), (2) little change in accumulation rate, based on microparticle data of Thompson and others (1981), (3) 33% increase (Lorius and others 1984), (4Í 50% increase (Robin 1977).