Titlebook: Ice in the Climate System; W. Richard Peltier Conference proceedings 1993 Springer-Verlag Berlin Heidelberg 1993 Eis.Orbit.Scale.Snow.Tide

消散

Modelling of the Fennoscandian Ice Sheetpproximation), mass balance, and bedrock isostasy. The mass balance is based on the balance of atmospheric humidity, and takes into account the effect of orographically induced precipitation, which causes zones of high precipitation to shift with the ice edge (Sanberg and Oerlemans, 1981). The ablat

ENDOW

Plastic Modelling of Glaciers and Outlets basic in the model has been that the bottom shear stress is assumed constant along a flowline (Orowan, 1949). This gives a simple calculation scheme for an ice sheet profile with an arbitrary bed surface. The unit “force” that cause this bottom shear stress is popularly called “driving stress”.

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FACT

Asseverate

Observations and Simulations of Temperature and Ice Accumulation at the Surface of Antarcticar the large polar ice caps, observation of these parameters is sparse and not reliable. This is a limitation to studying the current mass balance of the ice sheets. This is also a major obstacle to calibrating and validating models of the polar atmosphere necessary for any attempt to simulate the ev

Thyroiditis

World Sea Level and the Present Mass Balance of the Antarctic Ice Sheetes, particularly in the iceberg-calving flux, are too great. Using the observed rise in world sea level may be a better method. Two recent studies of tide-gauge data, world-wide, corrected for post-glacial rebound and excluding data from regions where tectonic plates converge, give a rate of rise of

预感

冒失

Heinrich Events: Triggers of Ocean Circulation Change?einrich, 1988; Broecker et al., 1990). Based on their geographic pattern and composition, these layers appear to be debris released during the melting of armadas of icebergs (Bond et al., 1992). Abundant limestone fragments in the ice-rafted debris and the exceptionally high .K — .Ar ages for the cl

拥护

Heinrich Events: Chronology and Processes, East-Central Laurentide Ice Sheet and NW Labrador Sea(see Imbrie, this volume). Research over the last few years shows that the climate system also changes at much higher frequencies. Examples of rapid climate changes include the Younger Dryas cold period of NW Europe (Mangerud, 1987; Rind, et al., 1986; Wright, 1989), the “Dansgaard-Oeschger” oscilla

让步

Transport of Freshwater into the Deep Ocean by the Conveyorly two-thirds is released to the atmosphere in the northern part of the basin as a result of deepwater formation. If all of this heat were taken up in melting ice, it would yield approximately 60,000 km. of meltwater per year. Thus it is conceivable that peak deglacial melting rates of 5,000–15,000