Titlebook: Dynamics of the West Antarctic Ice Sheet; Proceedings of a Wor C. J. Veen,J. Oerlemans Conference proceedings 1987 D. Reidel Publishing Com

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Clinton Jeffery,Jafar Al-Gharaibehcan be fitted reasonably well by making a number of simplifying assumptions. In addition, velocities are known at the grounding line of the Rutford Ice Stream and across the ice rumples between Korff and Henry ice rises. Velocity profiles can be deduced along the two relevant flowlines using the pri

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Evaluating Complex Development Programsure evolution of the Ross Ice Shelf, and of the stress regime at the grounding line of ice streams B and C are simulated to assess the response to impulsive removal of the Crary Ice Rise. This simulation shows that the forces restraining Ice Stream B do not change by a significant amount even after

monochromatic

https://doi.org/10.1007/978-1-4614-4797-9d ridges instead of the smoother surface of Ice Stream C. Regions of Ice Stream B with a lower surface elevation move faster than higher elevation regions, presumably because the lower-elevation ice is thinner and experiences less basal friction. Surface strain rates at Ice Stream B vary on a scale

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https://doi.org/10.1007/978-1-4614-9123-1und to be the cause of the 1982–1983 surge of Variegated Glacier in Alaska, may be typical of the flow regime of this ice stream. The bed model and inferred subglacial water pressures are consistent with (1) the calculated subglacial water flux, (2) the thickness of a porous water-saturated subglaci

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Daniel B. Cornfield,Randy Hodson pattern of steady-state mean water-film thickness is then interpreted in terms of its possible relationships to the basal sliding rates and the basal shear stress particularly under the major ice streams.

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0924-5006 centimeters (e. g. thermal expansion, change in mass balance of glaciers and ice sheets). But the picture of the carbon dioxide problem has frequently be made m978-94-010-8171-9978-94-009-3745-1Series ISSN 0924-5006

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