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Warren B. White

1. Introduction Masumoto and Meyers (1998) observed interannual Rossby waves with periods ranging from 3 to 5 yr in the tropical Indian Ocean from 6° to 14°S for 10 years from 1984 to 1993 in anomalous depth of the 20°C isotherm. This was made possible by expendable bathythermograph temperature profiles made along repeated sections by volunteer observing ships transiting the Indian Ocean. These interannual Rossby waves were not generated at the west coasts of Indonesia and Australia, but were

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Anthony Wise, Chris W. Hughes, Jeff A. Polton, and John M. Huthnance

1. Introduction The propagation of waves along ocean boundaries occurs as part of the oceanic adjustment to variability in environmental forcing, such as wind stress or buoyancy. Over a period of time, wave propagation enables changes in forcing to be communicated over large distances along boundaries and between the open ocean and coast. The characteristics of these waves, often referred to as coastal trapped waves (CTWs) because of their decaying away from the boundary, are therefore

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Marc P. Buckley and Fabrice Veron

1. Introduction Small-scale dynamics at the wavy air–sea interface strongly influence the exchanges of heat, momentum, mass, and energy between the ocean and the atmosphere. These fluxes may in turn impact large-scale weather patterns, sea state, and climate and are, as such, key components of recent oceanic and atmospheric models (e.g., Breivik et al. 2015 ). The complex feedback mechanisms involved in the coupling between wind and waves and their effects on the atmospheric and oceanic

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Nirnimesh Kumar and Falk Feddersen

. In Part I , the wave-resolving Boussinesq model funwaveC is coupled to a wave-averaged, depth- and stratification-resolving model, Coupled Ocean–Atmosphere–Wave–Sediment Transport (COAWST), to allow both Stokes drift effects and 3D TRCs on an unstratified inner shelf. Relative to simulations without TRCs, TRCs induced significant changes in the mean overturning Lagrangian circulation, velocity variability, mean eddy viscosity, momentum balances, and exchange velocity out to 5 L SZ offshore

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R. Lalbeharry, J. Mailhot, S. Desjardins, and L. Wilson

coupling on the evolution of the surface ocean wave field. The development of the third generation (3G) wave model called WAM described in The WAMDI Group (1988) has led to a gradual replacement of earlier 1G and 2G wave models in most but not all deep water prediction systems since 1988. The current Cycle-4 version of WAM (hereinafter referred as WAM4) is based on the ideas of Janssen (1991) in which the winds and waves are coupled; that is, there is feedback of growing waves on the wind profile

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Yalin Fan, Isaac Ginis, Tetsu Hara, C. Wayne Wright, and Edward J. Walsh

hurricane directional wave spectra for both open ocean and landfall cases using the National Aeronautics and Space Administration (NASA) Airborne Scanning Radar Altimeter (SRA). These measurements have provided detailed wave characteristics at a specific place and time. Moon et al. (2003) conducted a detailed comparison between WAVEWATCH III (WW3) wave model simulations and observations of the spatial distribution of hurricane directional wave spectra obtained from NASA SRA in Hurricane Bonnie (1998

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Jan Erik Weber and Arne Melsom

FEBRUARY 1993 WEBER AND MELSOM 193Transient Ocean Currents Induced by Wind and Growing Waves JAN ERIK WEBER AND ARNE MELSOMInstitute of Geophysics, University of Oslo, Blindern, Oslo, Norway(Manuscript received 16 October 1991, in final form 27 February 1992)ABSTRACT A theoretical nonlinear model for wind- and wave-induced currents in a viscous, rotating ocean is developed.The analysis is

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Frederick T. Mayer and Oliver B. Fringer

1. Introduction In the ocean, because lee waves occur on length scales smaller than the resolution of global circulation models (GCMs), the lee wave drag must be parameterized. Existing parameterizations are based on steady-state solutions for the flow above “linear-height” hills, wherein the height of the hill is much smaller than the wavelength of the wave ( Bell 1975b ; Gill 1982 ). Most common among the unresolved bathymetric features of the deep ocean are the abyssal hills which are

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Jesse M. Cusack, J. Alexander Brearley, Alberto C. Naveira Garabato, David A. Smeed, Kurt L. Polzin, Nick Velzeboer, and Callum J. Shakespeare

balance a significant fraction of the wind work in the ocean interior ( Ferrari and Wunsch 2009 ). The relative importance of these mechanisms is not known, because they are not well constrained by the few observations that exist. For eddy–internal wave interactions in particular, previous observations were made in areas with modest eddy kinetic energy, and none in the Southern Ocean where the mechanism’s potential for global influence is arguably largest ( Marshall et al. 2017 ). A diverse range of

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Lachlan Stoney, Kevin J. E. Walsh, Steven Thomas, Paul Spence, and Alexander V. Babanin

1. Introduction Surface waves can regulate climate by modifying the exchange of heat and momentum between the atmosphere and ocean (see Cavaleri et al. 2012 ; D’Asaro 2014 ; D’Asaro et al. 2014 ). Thermodynamically, the waves can influence climate by altering the characteristics of the air–sea interface, particularly through the generation of bubbles and sea spray during wave breaking ( Babanin 2011 ). Mechanically, the waves can modify vertical mixing processes in

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