FORMATION OF THE MODEL 

 Consider coastal waters in which a balance between Coriolis, pressure 

 gradient, and frictional forces are of primary importance such i;hat the steady 

 linear equations of motion reduce to 



(0 



A y W- ^ _ f 





K% - pf- 



-- O 



with the boundary conditions 





u 



^-i^ = ° :' v^=., - ° 



In the above equations, (n,s) are horizontal Cartesian coordinates and (u, v) 



are the corresponding A^elocity magnitudes, n is positive toward the 



shelf-breakfwith n=o at the 10 meters isobath) and s is positive 90° to 



the left of n. Also, Z is the vertical coordinate positive upwards. The 



free surface is at 2=^ (n, s) and the bottom at Z=-h (n, s) (fig. 1]. i^ and 



n 



T^ are the components of the wind stress acting on the sea surface. The mean 

 s 



density, p, is considered constant in a vertical column, but allowed to changS 



at a constant rate in the cross-shelf direction (i.e., -ItL - constant.) The 



3n 



pressure, p, is hydrostatic. Lateral friction and non-linear acceleration terms 

 are neglected. 



