viscosity. Still the result has some advantages over the classical theory 
in explaining various fentures encountered in the actual sea, especially 
in enabling us to Imow the horizontal variation of the velocity components 
and surface slope. If the complete mmerical computation could be worked 
out, this problem would give a complete structure of water motion produced 
by the stress of the winds in both decp and shallow seas. However, this 
would require a great amount of tedious calewlation so the complete dis= 
eussion is left for the future and only the digeriuation of the surface 
slope and the change of level in an offshore direction will be treated in 
this paper. It gives the steady surface seve developed by wind in a sea 
of finite depth and will be especially applicable to the problem of wind~ 
produced piling=-up or lowering of water in continental shelves such as 
found in the Gulf of Mexico or the North Siberian Shelf. 
II. Theory 
Consider a straight coast coincident with the axis of y, with the . 
x-axis perpendicular to it in the offshore direction. (Figure 1) Suppose 
a wind of constant. force and direction is bl. wing steadily in ae belt of 
limited width L at a certain angie with the coast. Take the | ieee | 
vertically downward. 
If a constant wind blews for a sufficiently long time, a steady state 
will be attained in which the motion of water is independent of time. We 
assune that the wind stress cannot vary in the y-direction, but may be a 
function of Z . This means that the wind can vary in an offshore direction 
only. In such a steady state all the vertical and horizontal components of 
the currents can be detcrmined as functions of x and g only. Of course, the 
ate 
