(right) Central pressure deficit as a function of maximum wind speed [V.sub.m] and a parameter (1/2[fr.sub.8]) that combines storm size [radius (km) of winds exceeding 8 m [s.sup.-1] [r.sub.8]] and latitude (Coriolis parameter
where u(x, y, t) and v(x, y, t) are x and y components of flow velocity and f represents the Coriolis parameter
On the other hand, the Coriolis parameter can be considered to be constant everywhere in the Baltic Sea, thus the [beta]-effect can be excluded.
Here u and v are depth-integrated velocity components, [eta](x, y, t) is the free surface elevation, f and g are Coriolis parameter and gravity, respectively; the depth is given by the formula z = -H(x) Here the subscript means the derivative with respect to the corresponding argument.
We calculated dispersion curves for the Coriolis parameter f = 1.2 x [10.sup.-4] [s.sup.-1] for the characteristic length scale L = 20 km.
This dictates a characteristic horizontal velocity scale U = g'H/fL = [R.sup.2]f/L, where L and H are the horizontal and vertical scales of the basin, R = [(g'H).sup.1/2]/f is the baroclinic Rossby radius of deformation, g' = g [DELTA][rho]/[rho] is reduced gravity, [DELTA][rho]p is the density difference over the vertical scale H, and f is the Coriolis parameter. If we introduce the characteristic scales of vertical movement W = g'[H.sup.2]/[L.sup.2] f (from continuity), and pressure P = [rho] g'H (from the hydrostatic pressure approximation), it is then possible to rewrite the governing equations in dimensionless form:
Supposing the Coriolis parameter to have a value f=[10.sup.-4.s.sup.-1], it follows that the baroclinic Rossby deformation radius is R=9.5x[10.sup.4]m for the Gulf.