The Eastern Bering Sea Shelf : oceanography and resources / edited by Donald W. Hood and John A. Calder . easternberings00hood Year: 1981 Ice dynamics and thermodynamics 215 Figure 13-3. Surveyor. The location of radiosonde launches made during the first two weeks of March 1979 from the NOAA ship amining the change in the distribution of sea surface temperature (Fig. 13-5). All surface measurements during the two-week cruise are plotted on the same chart and contoured for the first and second weeks sepEirately. The eastern end of the figure shows the change observed over a two-week period,
The Eastern Bering Sea Shelf : oceanography and resources / edited by Donald W. Hood and John A. Calder . easternberings00hood Year: 1981 Ice dynamics and thermodynamics 215 Figure 13-3. Surveyor. The location of radiosonde launches made during the first two weeks of March 1979 from the NOAA ship amining the change in the distribution of sea surface temperature (Fig. 13-5). All surface measurements during the two-week cruise are plotted on the same chart and contoured for the first and second weeks sepEirately. The eastern end of the figure shows the change observed over a two-week period, while the western end shows almost steady-state conditions. Note that while the — C isotherm moved about 35-40 km south during the cruise, the + C iso- therm did not move appreciably. The salinity field showed the same trend; although the contouring is less significant with only half as many samples (Fig. 13-6), the advance of meltwater is strikingly apparent. It is possible that movement of meltwater toward the south could be due to advection of the water mass itself. However, the mean currents on the shelf are weak and northwesterly, generally in opposition to the advance of meltwater (Kinder and Schumacher, Chapter 5, this volume). Contours of dynamic height during the March cruise period also suggest weak flow toward the northwest (Fig. 13-7). Although this dynamic topography has less relief than that shown previously by Charnell et al. (1979), it is similar in inferred speed and direction. Also, the pattern suggested by Figs. 13-5, 13-6, and 13-7 is coherent over periods longer than a tidal cycle. The amount of ice melt required to lower temper- ature to observed values (Fig. 13-4) was estimated by assuming that the water had been + C and that the ice had already warmed to its freezing point. Under these assumptions, enough heat was extracted to melt a 60-km-long, strip of ice of 15°/oo salinity. This melt estimate was probably too high since off-i
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