. Collected reprints / Atlantic Oceanographic and Meteorological Laboratories [and] Pacific Oceanographic Laboratories. Oceanography layer of a moving vortex, as originany derived by Chow (1971). This nxsdel is based on the nu- merical integration of the vertically averaged (over the depth of the boundary layer) equations of motion that govern a boundary layer subject to horizontal and vertical shear stresses on the rotating earth. In vector form, the equation of motion is written in coordinates fixed to the earth: â VP+v(KuV'V)- P n T^lvlv (5) where v is the vertically averaged
. Collected reprints / Atlantic Oceanographic and Meteorological Laboratories [and] Pacific Oceanographic Laboratories. Oceanography layer of a moving vortex, as originany derived by Chow (1971). This nxsdel is based on the nu- merical integration of the vertically averaged (over the depth of the boundary layer) equations of motion that govern a boundary layer subject to horizontal and vertical shear stresses on the rotating earth. In vector form, the equation of motion is written in coordinates fixed to the earth: â VP+v(KuV'V)- P n T^lvlv (5) where v is the vertically averaged horizontal velocity, ^ is the Coriolis parameter, p is air pressure, h is the depth of the boundary layer, Kh is the horizontal eddy viscosity coefficient, and K(j is the drag coefficient. The equation is resolved in a Cartesian coordinate system the origin of which is allowed to translate at con- stant velocity (v^) with the center of the pres- sure field associated with the vortex (in this case, the hurricane pressure eye). The varia- tions in storm intensity and motion are repre- sented by a series of quasi-steady states. With this representation, the pressure gradient be- comes independent of time and may be simply pre- scribed. This nonlinear system of equations is solved numerically on a fine-mesh nested grid system as an initial value problem for the steady-state solution of the horizontal com- ponent of the vertically averaged velocity; that is, until the wind field on the moving grid becomes approximately steady. A simple transformation then yields the wind field with respect to the fixed-earth coordinate system. The calibration of the model involved the de- velopment of a scaling relationship between the anemometer level wind speed and the integrated boundary layer wind speed. This scaling law was developed mainly on the basis of wind data from a rig In the path of Camille, 1969, but it appears to be valid rather generally. The adoption of the pressure specifi- catio
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