The Eastern Bering Sea Shelf The Eastern Bering Sea Shelf : oceanography and resources / edited by Donald W. Hood and John A. Calder easternberings00hood Year: 1981 Shelf environment 465 Figure 29-9. Tidal currents (cm/sec) calculated from numerical tidal model for (a) four hours before high tide, and (b) four hours before low tide at the eastern boundary (from Hastings 1975). of anomaly of dynamic height computed from the surface relative to 50 db (0/50 db) suggest several major features of flow (Fig. 29-10). Northwestward flow is indicated over the basin between Unimak Island and Cape Na
The Eastern Bering Sea Shelf The Eastern Bering Sea Shelf : oceanography and resources / edited by Donald W. Hood and John A. Calder easternberings00hood Year: 1981 Shelf environment 465 Figure 29-9. Tidal currents (cm/sec) calculated from numerical tidal model for (a) four hours before high tide, and (b) four hours before low tide at the eastern boundary (from Hastings 1975). of anomaly of dynamic height computed from the surface relative to 50 db (0/50 db) suggest several major features of flow (Fig. 29-10). Northwestward flow is indicated over the basin between Unimak Island and Cape Navarin and a component veers to the right around Anadyr Bay, eastward to St. Law- rence Island, and finally northward through Bering Strait. There is a suggestion of a weak westward cross-shelf flow just north of St. Matthew Island and also a northeastward flow into Bristol Bay along the north coast of the Alaska Peninsula, with a westward meandering return flow out of northern Bristol Bay. Although the action of surface winds could result in markedly different flows in the upper and lower portions of this 0-50 m layer, which are well isolated in summer by thermal and haline stratification, these results are interesting and should form the basis for further investigations. VARIABILITY McLain and Favorite (1976) have presented monthly anomalies of air and sea surface temperature in the vicinity of the Pribilof Islands (57°N, 170°W) from 1967 to 1975, which reflect not only a long- term downward trend (which reversed itself in 1977) but also considerable monthly and annual variability. Mean monthly north and south geo- strophic wind components computed for 1946-75 for the grid point 57°N, 170°W (Fig. 29-11) indicat- ing potential periods of cooling (and ice advance in winter and spring) and warming (and ice retreat in winter and spring) reflect the extreme variability of meteorological conditions; and the 12-month running mean indicates an approximate three-year cycle and a lo
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