3. SOLUTION FOR STEADY FORCING
The response to the steady forcing can be also solved by analogy to the periodic forcing case. Only the term v/ t in (2.2) is replaced by rv/h, where r is the coefficient of the bottom friction. The problem is a mere “arrested waves” version of the periodic solution described in section 2.
We calculate the alongshore velocity υ for the given depth prfile (Figure 4c) as in section 2. Figure 4a and 4b show the cross-shelf structure of the alongshore velocity and sea level at y = 2000km for the cases of m = 55km and m = 0km (no fast ice) with a wind-strees of 0.15m/s and r = 0.05cm/s. The structure of v is quite different between them even for the same wind forcing. Near the coast the current direction is the same as the wind stress direction in the case of no fast ice while it is reversed in the case of m = 55km. At the coast sea level becomes higher in the case of no fast ice.
REFERENCES
Clarke, A. J., 1978: On wind-driven quasigeostrophic water movements near fast-ice edges, Deep Sea Res., 25, 41-51.
Gill, A. E., and E. H. Schumann, 1974: The generation of long shelf waves by the wind. J Phys. Ocaanogr.,4,83-90,1974.
