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energy sources present in the ocean at low latitude is associated with planetary waves. It has been shown that in the Atlantic and Pacific Oceans, a large source of energy in the deep is associated with annual and semiannual Rossby waves, as well as intra-annual waves: 30-day, 1000-km mixed Rossby–gravity waves, associated with surface tropical instability waves, and short-scale variability, with periods around 70 days and wavelengths around 500 km ( Bunge et al. 2008 ; von Schuckmann et al. 2008
energy sources present in the ocean at low latitude is associated with planetary waves. It has been shown that in the Atlantic and Pacific Oceans, a large source of energy in the deep is associated with annual and semiannual Rossby waves, as well as intra-annual waves: 30-day, 1000-km mixed Rossby–gravity waves, associated with surface tropical instability waves, and short-scale variability, with periods around 70 days and wavelengths around 500 km ( Bunge et al. 2008 ; von Schuckmann et al. 2008
, the setup considered in this study intends to simulate horizontally isotropic turbulence since we assume constant values of vertical and horizontal stratification as well as a constant planetary vorticity. Especially for larger scales, however, a change of the planetary vorticity causes a development of zonal jets and thus a highly anisotropic flow. A characteristic length scale of these zonal jets is the Rhines scale , where β is the change of planetary vorticity and U is a characteristic
, the setup considered in this study intends to simulate horizontally isotropic turbulence since we assume constant values of vertical and horizontal stratification as well as a constant planetary vorticity. Especially for larger scales, however, a change of the planetary vorticity causes a development of zonal jets and thus a highly anisotropic flow. A characteristic length scale of these zonal jets is the Rhines scale , where β is the change of planetary vorticity and U is a characteristic
of both topography and oceanic motions (mesoscale eddies, internal waves). Difficulties in such estimations in the atmosphere have been explored by Smith (1978) , who emphasizes the topographic scales that need to be resolved for reliable estimates of the mountain drag. Because the spectrum of topographic slopes in the ocean is typically white at wavenumbers between 10 −2 and 10 cycles km −1 ( Bell 1975 ), the question of the choice of topography and velocity to be used for the evaluation of
of both topography and oceanic motions (mesoscale eddies, internal waves). Difficulties in such estimations in the atmosphere have been explored by Smith (1978) , who emphasizes the topographic scales that need to be resolved for reliable estimates of the mountain drag. Because the spectrum of topographic slopes in the ocean is typically white at wavenumbers between 10 −2 and 10 cycles km −1 ( Bell 1975 ), the question of the choice of topography and velocity to be used for the evaluation of
