Isaacs 



sea- surface temperatures. Figure 11 shows the correlation between 

 the sea- surface temperature as derived from monthly averages of hourly 

 readings from deep-moored stations and the sea- surface temperatures 

 from the published contoured charts from the Bureau of Commercial 

 Fisheries for the same station and month. The relationships, 

 unexpectedly, is excellent, with deviations between the two measure- 

 ments less than 1/2° F. The prima-facie evidence is thus that the 

 ships' data is very good and the instrument stations will delineate 

 the same type of temperature anomaly (as well as, of course, obtain- 

 ing comparable data beneath the surface). 



We therefore plan that within the next two years we will 

 establish a series of clusters of deep-moored stations, spread across 

 the North Pacific, in some such an array as shown in Figures 12 and 

 13. The cluster configuration in contrast to a regular grid is 

 required in order to ascertain the direction of any discontinuity or 

 wave-like motion passing through the area. 



The four peripheral moorings will record meteorological 

 data, and sea-water temperatures well into the thermocline. In 

 addition, insolation will be recorded. The central station is to be 

 a completely submerged recorder, measuring current in the mixed layer. 



Some of these clusters may also include a large telemeter- 

 ing station such as the Convair buoy. 



In preparing for the instrumentation of this program, we 

 are reviewing the traditional meteorological measurements to see if 

 other measurements may more directly relate to the interaction of 

 atmosphere and ocean. For example, measurements of humidity are 

 related to the evaporation or condensation of fresh water. A 

 measurement of evaporation or condensation related to the local sea 

 water would be more direct. This, in effect, would be a wet and dry 

 bulb measurement using sea water for the wetting agent. Of course, 

 such a simple approach as this would not be feasible because of the 

 changing concentrations of the wetting agent as evaporation 

 proceeded. 



Wind velocity is ordinarily recorded and converted into the 

 square of the mean velocity for evaluating its interaction with the 

 sea surface. Clearly the mean velocity squared of a turbulent wind 

 may be quite different from the mean square velocity, whereas in a 

 steady wind they will be much the same. It is perhaps more direct 

 and meaningful therefore to measure and record V2 rather than V. 



These are some of the instrumentation problems that we 

 hope to resolve in the near future. We plan then to launch a 

 significant attack on the unknown nature and causes of the large- 

 scale fluctuations in sea conditions that have been instrumental in 

 generating much uncertainty in man' s meteorological forecasts and in 

 his fisheries, agriculture, marine transport, underwater sound 



156 



