Atmosphere-ocean InteractionClarendon Press, 1972 - 275 pages |
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Page 27
... Fourier expansion of the basic data , it is sometimes more convenient to derive first the autocorrelation function ( 1.56 ) . For stationary processes , the two functions are related by the Fourier transform 00 ∞ G ( w ) = √ R ( d ) e ...
... Fourier expansion of the basic data , it is sometimes more convenient to derive first the autocorrelation function ( 1.56 ) . For stationary processes , the two functions are related by the Fourier transform 00 ∞ G ( w ) = √ R ( d ) e ...
Page 28
... Fourier transform of the cross - correlation function . Because the cross - correlation is not necessarily even , this generally yields a complex number JR , ( d ) e -iwd d8 = C'ƒg ( w ) —¿Qƒ , ( w ) . ( 1.67 ) The real part C ,, ( w ) ...
... Fourier transform of the cross - correlation function . Because the cross - correlation is not necessarily even , this generally yields a complex number JR , ( d ) e -iwd d8 = C'ƒg ( w ) —¿Qƒ , ( w ) . ( 1.67 ) The real part C ,, ( w ) ...
Page 35
... Fourier amplitude in the wave number domain . In the absence of non - linear interactions , each Fourier component in eqn ( 1.85 ) propagates independently and may be viewed as an inde- pendent monochromatic wave . The rate of ...
... Fourier amplitude in the wave number domain . In the absence of non - linear interactions , each Fourier component in eqn ( 1.85 ) propagates independently and may be viewed as an inde- pendent monochromatic wave . The rate of ...
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