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  • In Honor of Bach-Lien Hua: Ocean Scale Interactions x
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Audrey Delpech, Claire Ménesguen, Yves Morel, Leif N. Thomas, Frédéric Marin, Sophie Cravatte, and Sylvie Le Gentil

limit, while Qiu et al. (2013) interpreted the formation of EEJs in their simulations as the destabilization of annual Rossby waves through resonant triad interactions (corresponding to the weak nonlinear limit of Gill’s theory) and to further nonlinear adjustments involving potential vorticity fluxes. In addition, all the numerical studies exploring the formation of EEJs from waves have focused on a limited set of wave periods. A general continuous framework to analyze the potential contribution

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C. Ménesguen, S. Le Gentil, P. Marchesiello, and N. Ducousso

1. Context Ocean dynamics is largely studied through the prism of numerical models. The increase of computational capabilities led recent studies to implement very high-resolution simulations with up to three decades of grid points in the three directions, giving way to new dynamical regimes. High-resolution numerical simulations provide the representation of a wide range of scales in the study of energy spectra and fluxes. Questioning

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Nils Brüggemann and Carsten Eden

1. Introduction Turbulent flows in quasigeostrophic balance show a kinetic energy transfer from smaller to larger scales ( Charney 1971 ; Rhines 1977 ). In contrast, turbulent flows on much smaller scales feature a kinetic energy flux in the opposite direction, that is, from larger toward smaller scales, where the energy is finally dissipated on molecular scales ( Kolmogorov 1991 ). On the other hand, most of the energy input into the ocean occurs on scales characteristic for quasigeostrophic

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A. M. Treguier, C. Lique, J. Deshayes, and J. M. Molines

Gulf Stream, which flows poleward along the western boundary of the North Atlantic. The oceanic heat transport can be inferred from air–sea surface fluxes ( Large and Yeager 2009 ), and these estimates show that despite its relatively small width compared to the Pacific, the Atlantic Ocean performs half the global oceanic heat transport in the 20°–40°N latitude range. This has been recently confirmed at 26.5°N by the in situ measurements of the RAPID array, which gave an Atlantic heat transport of

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W. K. Dewar, J. C. McWilliams, and M. J. Molemaker

mean potential energy at the depths of the CUC are argued to average O (0.5) mW m −2 with local maxima reaching 3.4 mW m −2 . The rates computed here are comparable to those estimated in M15 . Modern global energetics budgets routinely estimate the flux of kinetic energy to small scales needed to maintain the observed stratification at roughly 6 mW m −2 . Of this, 1.0 mW m −2 is thought to create the potential energy stored in the mean stratification. This comparison argues that centrifugal

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Carsten Eden

1. Introduction In this note, the thermodynamics and energetics of the ocean in Boussinesq approximation are revisited. The aim is to formulate a consistent energy cycle for the ocean in Boussinesq approximation with a nonlinear equation of state and to formulate explicit conservation equations of the relevant thermodynamic quantities that have been previously discussed involving the correct exchange terms and molecular fluxes of heat and salt. Such a formulation is a prerequisite for

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Benjamin A. Storer, Francis J. Poulin, and Claire Ménesguen

lower row corresponds to the small Burger case. Recall that the large Bu case presents a net transfer of KE to PE. Throughout the linear regime ( Figs. 9a,b ), KE increases at deformation scales and decreases at vortex scales, while PE increases at both deformation and vortex scales. Both KE and PE present positive energy fluxes to smaller scales. The beginning of the nonlinear regime ( Figs. 10a,b ) is marked with a positive flux toward small scales in both KE and PE, the magnitudes of which well

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Yang Jiao and W. K. Dewar

upwelling and high-latitude downwelling. The accompanying buoyant flux balances the ocean global heat budget. As fluctuations in the MOC are thought to participate in multidecadal to centennial climate variability, small-scale mixing is of interest to global climate. As suggested by the above, a convenient language for the quantitative discussion of mixing is that of energetics. Buoyant fluids are mixed downward and heavy fluids are mixed upward in the scenario, and this requires energy. Recent reviews

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Alain Colin de Verdière and Michel Ollitrault

controlled by the equilibrium between eddy fluxes and bottom friction, our determination could be used to tune the bottom friction. The barotropic circulation of the ACC is of course the major product of the reconstruction. The ACC narrows down and therefore accelerates at several key points: the Drake Passage, north of the Kerguelen Plateau, and north of the Ross Gyre. The largest part (132 Sv) flows north of the Kerguelen Plateau while a branch (175–132 = 43 Sv) flows south of the plateau. By

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Thomas Meunier, Enric Pallàs Sanz, Miguel Tenreiro, José Ochoa, Angel Ruiz Angulo, and Christian Buckingham

.e., having increased spice) anomaly between the 24.5 and 26.5 kg m −3 isopycnals ( Fig. 1 ). Since the Yucatan Strait is the GoM’s only entrance for subsurface water, the thermohaline anomalies found in LCE’s cores have a large impact on the GCW characteristics ( Vidal et al. 1992 ; Elliott 1982 ; Meunier et al. 2018b ). GCW is believed to be transformed SUW, through surface heat fluxes, river discharge, evaporation, precipitation, and diapycnal mixing ( Hamilton et al. 2018 ). Of particular interest

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