274 G. F- McEwen. 



The estimated deviations of the directions of the coast from a north 

 and south line at stations 1, 2, 3, and 4 are respectively (35), (30), 

 (25), and (0) to the north west, and for stations 1 and 2, (x 2 ) = (2x 1 ), 

 but for stations 3 and 4, (x 1 ) = 0. From this data, and the values of 



( x i ~f" "sT**) obtained from formula (22) the corresponding distances 



(xi-J-Xo) were found to be 1670, 1120, 910, and 525 kilometers. An 

 estimate based upon the isothermes of Thorade's charts, of the 

 distances out from the coast to where the cooling effect was negligible 

 gave the following series of values: 2150, 1450, 710, and 600 kilo- 

 meters. In (Fig. 14, curves 3 and 1) these results are shown graphi- 

 cally. These curves 1 and 3 would coincide if the theory and the ob- 

 servations were correct. And the observed increase in width of the 

 cold-water area agrees well with the results deduced from the observed 

 winds. 



In (Fig. 15) are shown the contours of the ocean bottom perpen- 

 dicular to the coast at each station. Recalling the effect on temper- 

 ature distribution of the slope of the ocean bottom, and of the depth 

 adjacent to the coast, we would expect the variation in the character 

 of these contours to give rise to an increasing temperature reduction, 

 as the distance north of station (1) increases, as is shown by (Fig. 14, 

 curve 4). 



Finally, from the general system of winds over the North Pacific 

 Ocean we would expect from Ekman's theory, a "mid water-current" 

 bordering the coasts of Japan, Asia, and North America, having a 

 clockwise motion corresponding to that of the wind, the surface flow 

 being continually directed toward mid-ocean. Thus a movement of 

 water in a belt several hundred kilometers in width from the equatorial 

 regions north along the western borders of the Pacific then to the east 

 and south along the North American coast is in harmony with Ek- 

 man's theory. But a cold arctic surface-current, if started southward 

 would be deflected to the right of its path and would therefore flow 

 away from the coast of North America. Hence, such a current could 

 not give rise to a cooling effect in-shore. 



Considering the complexity of the circulation and temperature 

 distribution and the many factors influencing them, it is rather sur- 

 prising that the computed temperatures should agree so well with the 

 observed ones at each of the stations where the conditions differed so 

 widely, even tho the method used has been shown to give approxima- 

 telv the same results as tho the actual character of the flow was 



