. Collected reprints / Atlantic Oceanographic and Meteorological Laboratories [and] Pacific Oceanographic Laboratories. Oceanography 300- 150- Topographic Case BxlO3 (meters) f= 1800 hrs. BxlO3 (meters) r* 2400hrs. Fig. 16. The barotropic height (B), in meters, for the topo- graphic case (lower panels) and non-topographic case (upper panels), at the time steps 2=1800 h (left panels), and 2 = 2400 h (right panels).. H (meters) t = 500 hours H(meteis) t = 1000 hours Fig. 17. The upper layer height (H), in meters, for the case of non-normal flow at the eastern input boundary, at 2 =
. Collected reprints / Atlantic Oceanographic and Meteorological Laboratories [and] Pacific Oceanographic Laboratories. Oceanography 300- 150- Topographic Case BxlO3 (meters) f= 1800 hrs. BxlO3 (meters) r* 2400hrs. Fig. 16. The barotropic height (B), in meters, for the topo- graphic case (lower panels) and non-topographic case (upper panels), at the time steps 2=1800 h (left panels), and 2 = 2400 h (right panels).. H (meters) t = 500 hours H(meteis) t = 1000 hours Fig. 17. The upper layer height (H), in meters, for the case of non-normal flow at the eastern input boundary, at 2 = 500 h (left panel), and 2=1000 h (right panel). The upper layer changes noted after the initiation of the lower layer motion do not significantly affect the western boundary current, suggesting that topography is not an important factor in the baroclinic intensifica- tion. The beta-effect and advection as indicated in the Charney-Morgan inertial theories are sufficient to account for the baroclinic accelerations. In contrast, the model barotropic component is very dependent on topographic influences. Once initiated, barotropic intensification does not occur in the vicinity of the Strait but rather along the continental slopes of the boundaries. This suggests that topography rather than the beta-effect is the prime mechanism responsible for the barotropic boundary current. The observed topographic trapping of the current (Cochrane, 1966; Molinari and Cochrane, 1972) and the model trapping of the barotropic mode of the flow suggest that, particularly at shallow depths, the barotropic com- ponent can contribute significantly to the current. However, the magnitude of this barotropic component is sensitive to changes of u or a'. The influence of Cuba on the intensification process can be obtained from consideration of the flow through the Strait. Both the model and the observed data have countercurrents present at the western tip of Cuba. This separation of the main northerly flow
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