to the Gulf Stream at 36°N). The volume transport offshore during the south- 

 west monsoon can reach 38 to 42 x 10^ m^ sec"^ (0-400 dbar, rel . 400 dbar). 



In the mixed layer (upper 100 m) along the XBT section (20N to 12°N) heat 

 is gained in late Spring until the commencement of the southwest monsoon, after 

 which a rapid heat loss occurs. At the same time the loss takes place in the 

 mixed layer, however, there is a comparable gain in heat in the 100 to 200 m 

 layer caused by a deepening of the isotherms, thus the heat loss for to 200 m 

 appears to be small, if any, during the southwest monsoon. After the southwest 

 monsoon at the end of the year both layers show a heat loss. 



The surface dynamic topography of western Indian Ocean equatorial water 

 (480E to 50OE) shows strong seasonal signals: an increase in dynamic height 

 during each interim between monsoons (at the times the Wyrtkie jet should 

 occur) and a decrease during the northwest and southwest monsoons. 



The patterns of the monthly averages of the wind stress show the magnitude 

 of values during the southwest monsoon (July, off Socotra, > 4 dynes cm"^) are 

 large relative to that of the northeast monsoon (January, off northern Somalia, 

 > 1 dynes cm"2). Sverdrup mass transport determined from values of curl of the 

 wind stress shows agreement (values up to 40 x lO'^ g sec"' to the north) with 

 observations during the southwest monsoon off the Somali coast (6°N). During 

 the northeast monsoon the Sverdrup transport requires a southward flow along 

 the Somali coast south of about S^N (up to 10 x 10^2 g-1 sec). 



n 



