average pressure gradient force and C the vector of the Coriolis 

 force. Then from figure 6, 



G sina = rM cosp (26) 



and G cosa = 2a> sincp M + rM sinp , (27) 



since the components of the forces in the direction of M and per- 

 pendicular to it must balance. K«<M - M is proportional to the 



o 



average "dragging force", according to Sprung. 

 From (26) and (27) 



tanp = etna - ^^ (29) 



In the case where p -» 



~ 2oo sin© 

 etna = j— * . (30) 



So far, no direct computations of r have been made in dynamic 



oceanography, and it seems that the only estimates of a are those 



used in this report (Neumann, 1952). 



Whether (30) can be used instead of (28) to calculate r from 

 a, depends on the order of magnitude of p. However, data which are 

 accurate enough to compute p are not available. 



The mass transport of the Antarctic Circu m Polar Current between 

 65°S and 45°S, is given by 



M * 10 14 [gr sec" 1 ] , 

 approximately, according to Sverdrup et al (1946). (This value may 

 be even a little larger.) The average meridional pressure gradient 

 G can be estimated fairly well from the "Meteor" data published by 

 G. Wust (1939). Using "Meteor" Stations Mt 130, 124, 60, and 10, 

 the following pressure values, p, in decibar are obtained, relative 

 to the sea surface where p = 0: 



33 



