Atmosphere-ocean InteractionClarendon Press, 1972 - 275 pages |
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Page 147
... drag coefficient C2 2 = U * U 2 = K ( In z / zo + α1 ( z - 20 ) / L ) 2 ( 5.35 ) If C2 denotes now the drag coefficient for neutral conditions as specified 2 in ( 5.17 ) and if higher powers of z / L are negligible as postulated , we ...
... drag coefficient C2 2 = U * U 2 = K ( In z / zo + α1 ( z - 20 ) / L ) 2 ( 5.35 ) If C2 denotes now the drag coefficient for neutral conditions as specified 2 in ( 5.17 ) and if higher powers of z / L are negligible as postulated , we ...
Page 158
... drag coefficient U * and 20 . a = a and Са = ( ( U2 - Ua ) k ) Ua ln ( b / a ) 2 α This formula is derived directly from ( 5.16 ) and ( 5.2 ) . In practice , it is preferable to measure at more than two levels . The stress and the drag ...
... drag coefficient U * and 20 . a = a and Са = ( ( U2 - Ua ) k ) Ua ln ( b / a ) 2 α This formula is derived directly from ( 5.16 ) and ( 5.2 ) . In practice , it is preferable to measure at more than two levels . The stress and the drag ...
Page 162
... Drag coefficients in hurricanes from observations of ageostrophic transports ... coefficient with velocity at a rate C10 / V0-075 × 10-3 m - 1 s . Miller ... drag coefficient could easily be in error by a factor of 2 or 3. 162 ...
... Drag coefficients in hurricanes from observations of ageostrophic transports ... coefficient with velocity at a rate C10 / V0-075 × 10-3 m - 1 s . Miller ... drag coefficient could easily be in error by a factor of 2 or 3. 162 ...
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