The Eastern Bering Sea Shelf The Eastern Bering Sea Shelf : oceanography and resources / edited by Donald W. Hood and John A. Calder . easternberingsea00hood Year: 1981 Ice as marine mammal habitat 785 the central and northern Bering Sea as well as along the mainland shores from 56° or 57° N latitude to the Bering Strait. In the southern parts of the Bering it is frequently short-lived, occurring only during periods of extreme cold. In the central and northern Bering it persists from December to late May or early June, usually attaining its maximum extent in April. It varies in width from a f
The Eastern Bering Sea Shelf The Eastern Bering Sea Shelf : oceanography and resources / edited by Donald W. Hood and John A. Calder . easternberingsea00hood Year: 1981 Ice as marine mammal habitat 785 the central and northern Bering Sea as well as along the mainland shores from 56° or 57° N latitude to the Bering Strait. In the southern parts of the Bering it is frequently short-lived, occurring only during periods of extreme cold. In the central and northern Bering it persists from December to late May or early June, usually attaining its maximum extent in April. It varies in width from a few meters to several kilo- meters, depending on both latitude (weather) and configuration of the coastline (exposure to prevailing winds and ocean currents). It is most extensive where it is protected by some physiographic feature from strong winds, currents, and the drifting pack. In some parts of the Bering these same forces drive thick ice into shallows, where it becomes grounded and serves to protect and stabilize the thinner, floating fast ice surrounding grounded floes. However, the latter process is more important in the Chukchi and Beaufort seas. Embayments such as the numerous fjords of the eastern Chukotsk Peninsula, as well as Norton Bay, Golovnin Bay, Port Clarence, and Grantly Harbor, are protected areas in which an extensive, continuous, relatively flat cover of floating ice develops and remains in place until late spring. Unprotected shorelines such as eastern and western St. Lav\rrence Island, King and Diomede islands, and exposed capes accumulate little persistent fast ice. Fast ice develops along the remaining shoreline to a greater extent, depending on weather and interaction with the pack. The pack, by definition in constant motion, is highly dynamic and geographically variable. From the onset of freezing conditions its net transport is southward, driven by prevailing northeasterly vdnds and probably intensified by current reversals. Southward drift is slo
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