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. Spectra from the simulation ( Fig. 9 shows the vertically integrated kinetic and available potential energy spectra) indicate a well-resolved enstrophy cascade and a typical eddy radius of about 40 km. The inverse cascade in this simulation is present but short: the eddies equilibrate at only about three times the deformation radius. Physical space fields (not shown) indicate that the flow is horizontally homogeneous—no jets form—consistent with a drag-based cascade-halting mechanism ( Smith et al
. Spectra from the simulation ( Fig. 9 shows the vertically integrated kinetic and available potential energy spectra) indicate a well-resolved enstrophy cascade and a typical eddy radius of about 40 km. The inverse cascade in this simulation is present but short: the eddies equilibrate at only about three times the deformation radius. Physical space fields (not shown) indicate that the flow is horizontally homogeneous—no jets form—consistent with a drag-based cascade-halting mechanism ( Smith et al
structure of multiple zonal jets with small meridional scale, compared to within the no-slip boundary layer, where the perturbations are oriented more perpendicular to the boundary and span the boundary layer width. The temperature field at 15-m depth is dominated by narrow bands of dense water below the convergence zones in the surface layer ( Fig. 9c ). The vertical velocity in these regions is downward, bringing down the more dense waters with negative potential vorticity formed at the surface
structure of multiple zonal jets with small meridional scale, compared to within the no-slip boundary layer, where the perturbations are oriented more perpendicular to the boundary and span the boundary layer width. The temperature field at 15-m depth is dominated by narrow bands of dense water below the convergence zones in the surface layer ( Fig. 9c ). The vertical velocity in these regions is downward, bringing down the more dense waters with negative potential vorticity formed at the surface
