an equation derived by integrating the equation of continuity (2) from 
7 the surface down to a depth a6 
The preceding vnalysis covers ‘tthe principal part of the theory of 
upwelling discussed by the author recently as a special case when the 
depth of the ses is very large, In that case we had Y¥ (\) > Z 80 
only the secozd term in the right-hand member of (19) wes considered. A 
complete nursrical computation involving three components of velocity and 
the surfaces slope wild be achieved oniy acter a tedious work of very long 
period. We shall give in this report only the computations as to how the 
slope «f the sea surface varies as we go away from the coast. The author 
pents to express his desire tio extend the computations to all three com= 
ponents of the motion of water in the future because this promises a great 
number cf practical applications, The comparison of computed motion to 
that, actually observed wiil enable us to estimate the approximate intensity 
of botn vertical and horizontal turbulence in the sea, thus making it 
possible to predict the wind currents in the sea more eccurately. 
IV. Gomputation of Sey Surface Slope and Horizontal, Veriation of Sea Level. 
It is a question of practical calculations to cerry the analysis to 
numerical resvits, A rather elaborate computation has been carried out by 
the author durixg the summer of 1953 when he stayed in the Department of 
Ocean-craphy, Agricultural and Mechanical College of Texas. 
The greater part of the work consisted of mmerical evaluation of the 
function OX as given by (22). Because the components of wind stress are 
given in advances we have only to evaluate the two functions EG. N) and 
LG, A) given by (26) and (27). They have been computed for 
& = 1/16, 1/8, 4, 1/2, 1, 2 and 4 
yee 
“10s 
