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al. 1992 ; Wilkin and Morrow 1994 ; Griesel et al. 2009 ; Chen et al. 2014 ). Fig . 5. Float-based diffusivities in the cross-stream direction at (a) 400–600 and (b) 900–1400 m. Dots indicate the location of the centroid of each adaptive bin used to obtain the diffusivity estimates. We carried out convergence tests using the method from Chen et al. (2014) and only converged diffusivities are shown here. Black lines indicate the barotropic streamlines. Gray regions denote land, and white
al. 1992 ; Wilkin and Morrow 1994 ; Griesel et al. 2009 ; Chen et al. 2014 ). Fig . 5. Float-based diffusivities in the cross-stream direction at (a) 400–600 and (b) 900–1400 m. Dots indicate the location of the centroid of each adaptive bin used to obtain the diffusivity estimates. We carried out convergence tests using the method from Chen et al. (2014) and only converged diffusivities are shown here. Black lines indicate the barotropic streamlines. Gray regions denote land, and white
do not apply. Held and Schneider (1999) , Schneider et al. (2003) , and Schneider (2005) showed that nonquasigeostrophic effects at the boundaries (specifically, relatively large isopycnal slopes) modify the overall residual circulation of the atmosphere. Similar issues may arise in the ocean. Plumb and Ferrari (2005) extended the planetary geostrophic system in (1) – (4) to account for nonquasigeostrophic effects. However, their momentum and buoyancy equations involve terms that are
do not apply. Held and Schneider (1999) , Schneider et al. (2003) , and Schneider (2005) showed that nonquasigeostrophic effects at the boundaries (specifically, relatively large isopycnal slopes) modify the overall residual circulation of the atmosphere. Similar issues may arise in the ocean. Plumb and Ferrari (2005) extended the planetary geostrophic system in (1) – (4) to account for nonquasigeostrophic effects. However, their momentum and buoyancy equations involve terms that are
