. Collected reprints, Essa Institute for Oceanography. Oceanography September 1967 I000 Bernhard Lettau. 6 7 8 Wind Speed Parallel to Surface Wind Direction (mps —4 —3 —2 —I Wind Speed Normal to Surface Wind Direction (mps) Figure 5.—Observed ambient mean wind profile and computed linear geostrophic wind profile separated into components parallel and normal to the surface wind direction. North winds in winter. winter and summer. For the most part the differences among the four cases are minor, and related to directional rather than seasonal differences, suggesting that the ice su
. Collected reprints, Essa Institute for Oceanography. Oceanography September 1967 I000 Bernhard Lettau. 6 7 8 Wind Speed Parallel to Surface Wind Direction (mps —4 —3 —2 —I Wind Speed Normal to Surface Wind Direction (mps) Figure 5.—Observed ambient mean wind profile and computed linear geostrophic wind profile separated into components parallel and normal to the surface wind direction. North winds in winter. winter and summer. For the most part the differences among the four cases are minor, and related to directional rather than seasonal differences, suggesting that the ice surface produces its own characteristic wind distribution. The component parallel to the surface wind increases with height immediately above the surface in all four cases, but reaches a maximum below 400 m. and decreases slowly with height above that level. The geostrophic wind decreases continuously in the boundary layer indicating that this component of the thermal wind is antiparallel to the surface wind. Its magnitude however is relatively small, ranging from to m. ;1 The height at which tt reaches a maximum is approximately 160 m., with the exception of southerly winds in summer when tx reaches a maximum at 200 m., and the maximum value attained ranges from and The component normal to the surface wind shows a definite directional difference, caused by the relatively fixed thermal wind vector. For the southerly winds this component increases from the surface to roughly 500 m., then decreases to the top of the boundary layer, the devia- tion being to the left of the surface wind. For the northerly winds the component value in summer increases con- tinuously to the left of the surface wind through the boundary layer; in winter the profile is very similar with the exception of a slight relative maximum at 600 m. The geostrophic wind increases to the left for the northerly components, and to the right for the southerly compone
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