Atmosphere-ocean InteractionClarendon Press, 1972 - 275 pages |
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Page 86
... radiance : 9 Bo ΧΥ 1. = B2 ( 1 + xx ( 2 + 008 ) ) = B. ( 1+ cos 4 ) . I 2π cos β 2π z = 0 β For normal viewing of the sea surface , this becomes Bo 14- = B. ( 1 + 27 ) . I 2π β ( 3.24 ) ( 3.25 ) The value of the normal monochromatic sea ...
... radiance : 9 Bo ΧΥ 1. = B2 ( 1 + xx ( 2 + 008 ) ) = B. ( 1+ cos 4 ) . I 2π cos β 2π z = 0 β For normal viewing of the sea surface , this becomes Bo 14- = B. ( 1 + 27 ) . I 2π β ( 3.24 ) ( 3.25 ) The value of the normal monochromatic sea ...
Page 87
... radiance is enhanced by the reflection of atmospheric radiation . Saunders ( 1968 ) , in a careful investigation , expressed the infrared radiance of a flat , calm ocean as a function of the viewing angle in the form where I¿ = rI ...
... radiance is enhanced by the reflection of atmospheric radiation . Saunders ( 1968 ) , in a careful investigation , expressed the infrared radiance of a flat , calm ocean as a function of the viewing angle in the form where I¿ = rI ...
Page 88
... radiance at the surface temperature ( 15 ° C ) . The lower scale represents black - body temperatures that would produce the radiance marked on upper scale . is therefore less than unity , and its infrared radiance differs discon ...
... radiance at the surface temperature ( 15 ° C ) . The lower scale represents black - body temperatures that would produce the radiance marked on upper scale . is therefore less than unity , and its infrared radiance differs discon ...
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