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  • The Diapycnal and Isopycnal Mixing Experiment in the Southern Ocean (DIMES) x
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Ru Chen, Sarah T. Gille, Julie L. McClean, Glenn R. Flierl, and Alexa Griesel

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

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Emma J. D. Boland, Emily Shuckburgh, Peter H. Haynes, James R. Ledwell, Marie-José Messias, and Andrew J. Watson

tracer level and the surface velocity may not be constant in space and/or time. For the simulations to be analyzed later in the paper, the velocity fraction was chosen as 0.33. Justification for this choice is given in section 2d . Before use in the advection–diffusion calculation, these velocity fields were interpolated onto finer resolution grids, (1/20° or 1/50°) as appropriate, and rendered nondivergent at the boundaries before use. The boundaries were provided by the maximum land mask from the

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Matthew R. Mazloff, Raffaele Ferrari, and Tapio Schneider

-dimensional pathways of ocean water masses. Here we use a synthesis of observations, a numerical model, and theory to investigate the force balance of the SO limb of the MOC. Standard scaling analysis for the large-scale ocean circulation assumes a small Rossby number, leading to the thermocline equations based on the linearized planetary geostrophic equations ( Robinson and Stommel 1959 ; Welander 1959 ; Phillips 1963 ; Pedlosky 1987 ). But in the Drake Passage latitude band of the SO, at depths where there

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