and a compensating equatorward flow very likely develops at a slightly 

 greater deptho 



Apparently there is a circulation cell to the north of and immediately 

 adjacent to the equator which is in some respects similar to that described 

 by Sverdrup (1938) for the California coastal waters during periods of 

 upwelling» In our case^ the plane of the equator acts as a "coastline". 

 The intensity of this circulation will depend on the relatively local wind 

 conditions as will the position of the convergent zone. 



At the northern boundary of the countercurrent there is no evidence of 

 a major upwelling. That the thermocline approaches nearest to the surface 

 at this boundary is evident, Defant (1936) explains that this must be true 

 in the presence of the existing horizontal currents. It is necessary to 

 the dynamic balance within northern hemisphere currents that relatively 

 dense water lie to the left of an obseirver facing downstream. 



There is a horizontal eddy at the north boundary of the countercurrent 

 on the eastern station line. Its precise size is not known for there is no 

 assurance that the SMITH crossed along its greatest diameter. 



The countercurrent may "meander" as does the Atlantic Gulf Stream. An 

 eddy of the size encountered at the countercurrent boundary was probably 

 formed in the way that eddies of comparable size are formed along the 

 boundaries to the Atlantic Gulf Stream as described by Iselin (19-^8) . 

 According to Iselin, "These eddies appear to be actual segments of the 

 main stream that have broken away from the parent body when the Gulf 

 Streamj, in its raeanderings, formed an excessively large loop in its 

 path". The existence of this eddy is, therefore, indirect evidence that 

 the countercurrent "meanders" o 



8 



