Atmosphere-ocean InteractionClarendon Press, 1972 - 275 pages |
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Page 14
... inertial forces predominate is then indicated by the ratio · U v L D2 = UL D2 UZ ( 2 ) 2 = Re ( 2 ) . V L ( 1.35 ) Viscosity cannot affect the motion significantly if that ratio is at least one order larger than unity . In small - scale ...
... inertial forces predominate is then indicated by the ratio · U v L D2 = UL D2 UZ ( 2 ) 2 = Re ( 2 ) . V L ( 1.35 ) Viscosity cannot affect the motion significantly if that ratio is at least one order larger than unity . In small - scale ...
Page 225
... inertial period 23.6 h . ( Supplied by Dr. F. Webster , Woods Hole Oceanographic Institution . ) quadrature , with about equal amplitude . A review of these marine , inertial oscillations , which occur in all latitudes , has been ...
... inertial period 23.6 h . ( Supplied by Dr. F. Webster , Woods Hole Oceanographic Institution . ) quadrature , with about equal amplitude . A review of these marine , inertial oscillations , which occur in all latitudes , has been ...
Page 226
... inertial frequency w f are possible only when k = 0. Such infinitely long waves cannot exist on a bounded ocean . In fact , it can be seen from Fig . 7.4 that the oceans of this earth simply are not large enough for barotropic gravity ...
... inertial frequency w f are possible only when k = 0. Such infinitely long waves cannot exist on a bounded ocean . In fact , it can be seen from Fig . 7.4 that the oceans of this earth simply are not large enough for barotropic gravity ...
Contents
INTRODUCTION | 1 |
THE STATE OF MATTER NEAR THE INTERFACE | 41 |
RADIATION | 71 |
Copyright | |
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advection air-sea amplitude angle approximately atmosphere average baroclinic barotropic bubbles cause changes circulation cloud components constant convection convergence Coriolis force decrease denotes diffusion direction dissipation drag coefficient eddy effect Ekman layer equation equilibrium expression flow fluctuations fluid flux Fourier frequency friction function geostrophic gravity waves group velocity height horizontal hurricane increase inertial integral interaction interface kinetic energy larger latitude linear mean mixed layer moisture molecular momentum motion observations ocean parameter perturbations phase velocity planetary boundary layer potential temperature processes propagation radiance ratio region relatively represents resulting Reynolds number Reynolds stress Rossby waves salinity scale sea surface sea water sensible heat shear specific humidity specified spectral spectrum storm term thermocline transport tropical turbulent unstable upwelling vapour pressure variable variations vector vertical viscosity vorticity wave number wavelength wind stress wind velocity yields zero дх