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1. Introduction General circulation in the open ocean is constrained to the upper layer and thus hardly feels the abyssal topography, and the pressure anomaly away from the equator propagates westward due to Earth’s curvature, i.e., the planetary β effect. On reaching the shelf, the steep topography serves as a waveguide and deflects the oceanic information equatorward, i.e., the topographic Rossby wave, before it reaches the coastal region. In this case, the bathymetric slope, i.e., the
1. Introduction General circulation in the open ocean is constrained to the upper layer and thus hardly feels the abyssal topography, and the pressure anomaly away from the equator propagates westward due to Earth’s curvature, i.e., the planetary β effect. On reaching the shelf, the steep topography serves as a waveguide and deflects the oceanic information equatorward, i.e., the topographic Rossby wave, before it reaches the coastal region. In this case, the bathymetric slope, i.e., the
of sustained glider observations ( Rudnick and Cole 2011 ) provide the mean current patterns and their variability around the island of Palau in the tropical North Pacific on horizontal scales of 10–100 km, vertical scales of 10 m, and temporal scales as short as a week. For flows with rotation, a reasonable measure of eddy intensity is the Rossby number Ro, here defined as the ratio of relative to planetary vorticity (Ro = ζ / f ). Here Ro is a signed quantity, as used in, for example, Whitt
of sustained glider observations ( Rudnick and Cole 2011 ) provide the mean current patterns and their variability around the island of Palau in the tropical North Pacific on horizontal scales of 10–100 km, vertical scales of 10 m, and temporal scales as short as a week. For flows with rotation, a reasonable measure of eddy intensity is the Rossby number Ro, here defined as the ratio of relative to planetary vorticity (Ro = ζ / f ). Here Ro is a signed quantity, as used in, for example, Whitt
