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Yair De Leon and Nathan Paldor

various waves can only be determined when boundary conditions are imposed on the general solutions of the (ordinary) differential equations. The imposed boundary conditions are either regularity (or vanishing) of the meridional velocity component at infinity, or its vanishing at two walls that are assumed to exist at some given latitudes. While the infinite domain is hard to justify on the β plane [where only first terms of f  ( y ) are retained], the assumption that two walls exist in the ocean is

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Antoine Hochet, Thierry Huck, and Alain Colin de Verdière

1. Introduction During the last 20 yr, the measurements of the ocean surface properties by satellite instruments have allowed us to significantly increase our knowledge of ocean dynamics. Chelton and Schlax (1996) were among the first to show that large-scale anomalies, propagating to the west, were observable in the altimetry. Since then, a large number of authors have described these anomalies, generally depicted as Rossby waves, using various techniques such as a Hovmöller diagram

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Jaclyn N. Brown, J. Stuart Godfrey, and Susan E. Wijffels

1. Introduction The ocean currents in the equatorial Pacific are significantly nonlinear. Contributing to this nonlinearity are eddies, such as tropical instability waves (TIWs) (e.g., Legeckis 1997 ; McCreary and Yu 1992 ; Baturin and Niiler 1997 ). TIWs appear as oscillations of the currents, sea level, and sea surface temperature in the eastern equatorial Pacific. These disturbances are mixed barotropic/baroclinic instabilities feeding on the kinetic and potential energy of the mean

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Jamie MacMahan

1. Introduction Over land, the geometric roughness k and corresponding aerodynamic roughness z o for surface features can be considered temporally constant. Over the open ocean, z o is a function of both surface texture (associated viscous surface stresses) and the local wave field (associated form drag and flow separation). The associated stresses are dynamically coupled with the wind, can evolve together, and transition from viscous stresses to wave stresses. Nonlocal wave fields

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Riccardo Farneti

approaches have been used and different results, sometimes in disagreement, have been found. Nevertheless, there are a few key findings that can be pointed out. There is some evidence that the ocean can interact through feedback mechanisms (e.g., Latif and Barnett 1994 , 1996 ; Barsugli and Battisti 1998 ; Pierce et al. 2001 ; Hogg et al. 2006 ; Kravtsov et al. 2006 ), and it has also been suggested that oceanic Rossby waves play a major role in the coupling physics (e.g., Jin 1997 ; GM99

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Robert H. Weisberg and Thomas J. Weingartner

NOVEMBER 1988 ROBERT H. WEISBERG AND THOMAS J. WEINGARTNER 1641Instability Waves in the Equatorial Atlantic Ocean ROBERT H. WEISBERG AND THOMAS J. WEINGARTNERDepartment of Marine Science, University of South Florida, St. Petersburg, Florida(Manuscript received 28 December 1987, in final form 17 May 1988) ABSTRACT Evidence is presented for the generation of planetary waves by barotropic

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Julien Jouanno, Frédéric Marin, Yves du Penhoat, and Jean-Marc Molines

associated with the tropical instability waves (TIWs), which are triggered by the instabilities of the tropical oceanic currents (e.g., von Schuckmann et al. 2008 ; Perez et al. 2012 ). Besides the observational evidence that the 15-day variability of the meridional surface velocities is forced by the wind, the dynamical response of the upper ocean to 15-day wind fluctuations is still not fully understood. As mentioned by Picaut (1984) , there is a discrepancy between the zonal wavelengths of the

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Lars Czeschel, Carsten Eden, and Richard J. Greatbatch

-driven stratified ocean is initially strongly modified by variable topography, and it is only when most baroclinic Rossby waves emitted from the wind forcing have reached the western boundary that flat-bottom Sverdrup balance tends to be reached ( Anderson and Killworth 1977 ). Anderson and Corry (1985a) show that transport variation can be related to barotropic Rossby waves generated by wind stress and wind stress curls acting over variable bottom topography. In addition, baroclinic Kelvin waves from the

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Juan M. Restrepo

Komen et al. (1984) ]. A dynamic of whitecapping that has an obvious cause and effect is the dissipation it imparts on the waves and currents. The effective dissipation sometimes changes dramatically when a sudden change in wind strength and/or wind direction occurs. Whitecapping has no complete theory, and inclusion of its effects in ocean dynamics models is accomplished via parameterizations, some of which can be very sophisticated [ WAMDI Group (1988) ; Alves and Banner (2003) ; Komen et al

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Christopher J. Zappa, Michael L. Banner, Russel P. Morison, and Sophia E. Brumer

central role of surface and breaking waves in upper ocean dynamics and air–sea fluxes, wave and breaking measurements are paramount. The dissipation of wave energy in the energetic part of the spectrum has attracted considerable recent interest. Presently, parametric versions of S ds based on satellite data are used in the context of active whitecap fraction ( Anguelova and Hwang 2016 ), of ocean swell dissipation ( Ardhuin et al. 2009 ), and of the TKE dissipation rate due to breaking ( Hwang and

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