26H 



WOOSTER AND REID 



[CHAP. 11 



(a) (b) 





 DISTANCE OFFSHORE (km) 



Fig. 11. Profiles west of Australia at 32°S, January, 1951. (a)-(d) as in Fig. 6. (After 

 National Institute of Oceanography, 1957.) 



3. Coastal Upwelling 



Although the low surface temperatures of the eastern boundary currents 

 were at first attributed entirely to their origin in high latitudes (e.g. see Gunther, 

 1936), it gradually became evident that temperatures did not increase mono- 

 tonically downstream, and, thus, that some other process must be operating. 

 The distributions of other properties, such as salinity, oxygen and phosphate, 

 also suggested that vertical motion was present. There evolved a model of 

 coastal upwelling from depths of a few hundred meters, with wind stress parallel 

 to the coast causing an offshore transport of surface water and a compensatory 

 replenishment with deeper lying waters (Sverdrup, Johnson and Fleming, 1942, 

 pp. 500-503). Recent studies (Defant, 1952; Hidaka, 1954; Yoshida, 1955, 

 1958 and 1958a ; Yoshida and Mao, 1957) have attempted to evaluate the model 

 quantitatively. We have examined the time and space variations of upwelling 

 on the basis of a simple relationship between wind stress and the orientation 

 of the coastline. 



