The Eastern Bering Sea Shelf : oceanography and resources / edited by Donald W. Hood and John A. Calder . easternberings00hood Year: 1981 -â °-^ 58° 46,9 N 170= 253 W 36 31 58°469'N I70°25,3'W 36 31 - c ^ '^25,8 â' 25< - 25,9 10 km Figure 13-4. A CTD cross section perpendicular to tiie ice edge showing the meltwater lens typical along the margin of ice. The ice existed in water of about â C and colder. The CTD station numbers correspond to those in Fig. 13-2. DISCUSSION Ice forms in situ during a typical ice-year in late fall (November-December) in Norton Sound, in the Bering Sea
The Eastern Bering Sea Shelf : oceanography and resources / edited by Donald W. Hood and John A. Calder . easternberings00hood Year: 1981 -â °-^ 58° 46,9 N 170= 253 W 36 31 58°469'N I70°25,3'W 36 31 - c ^ '^25,8 â' 25< - 25,9 10 km Figure 13-4. A CTD cross section perpendicular to tiie ice edge showing the meltwater lens typical along the margin of ice. The ice existed in water of about â C and colder. The CTD station numbers correspond to those in Fig. 13-2. DISCUSSION Ice forms in situ during a typical ice-year in late fall (November-December) in Norton Sound, in the Bering Sea north of St. Lawrence Island, along the Alaskan coast, and eventually southward into Bristol Bay (Fleet Weather Facility 1972-1975, 1976, 1977, and 1978). These areas are shallow (less than 30 m), except for the region north of St. Lawrence Island, and water is observed to be isothermal at the freezing point (about â C). Cooling is caused by a negative radiation balance and sensible and latent heat transfer due to offshore winter winds. Under the influence of northerly to easterly winds, the ice floes are trans- ported into warmer water. The leading floes melt, adding relatively cold, fresh water to the existing water column. Under continued northerly winds, the new leading floes encounter colder waters and thus have longer residence times. As the season progresses, regions of ice growth expand and the floes are con- tinuously advected beyond these areas. Satellite and aircraft photographs of the Bering Sea in winter show persistent polynyas in the lee of Cape Nome and St. Lawrence, St. Matthew, and Nunivak Islands during periods of northerly to northeasterly winds (Muench and Ahlnas 1976, and McNutt, Chapter 10, this volume). Less commonly, a polynya can also be observed in eastern Norton Sound during more easterly wind events. Gray streaks, which Martin £ind Kauffman (1979) attrib- ute to grease ice production, are often observed in satellite images of thes
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