## Atmosphere-Ocean InteractionOxford University Press, 1994 M11 10 - 384 pages With both the growing importance of integrating studies of air-sea interaction and the interest in the general problem of global warming, the appearance of the second edition of this popular text is especially welcome. Thoroughly updated and revised, the authors have retained the accessible, comprehensive expository style that distinguished the earlier edition. Topics include the state of matter near the interface, radiation, surface wind waves, turbulent transfer near the interface, the planetary boundary layer, atmospherically-forced perturbations in the oceans, and large-scale forcing by sea surface buoyancy fluxes. This book will be welcomed by students and professionals in meteorology, physical oceanography, physics and ocean engineering. |

### From inside the book

Results 1-5 of 39

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**average**of the horizontal velocity in an incompres- sible fluid of limited depth D , then the vertical integral of ( 1.6 ) , after division by D , can be expressed in the form 1 dD V · Û + 0 . D dt ( 1.7 ) The velocities of individual ... Page 10

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**average**density near the sea surface or an overall density**average**. With the Boussinesq approximation and ( 1.25 ) and ( 1.26 ) , the first equation ( 1.22 ) can be written as d 22 az2 ) ] w W - fcU = 1 др ' Pr dz + g g ' ) . ( 1.27 ) ... Page 11

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**average**of ( 1.30 ) over a layer of depth D , one can use ( 1.7 ) and df / dt = 0 , to derive the vorticity equation d î z + ƒdD ( ñ1⁄2 + ƒ ) - D dt D dt d ( î z + dt D = vv2 . ( 1.31 ) A mechanical energy equation , which relates the ... Page 14

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**averages**of the variables will be taken over time , assuming that this will give a good representation of the ensemble**average**. The**average**is indicated by an overbar and the fluctuating component by a prime . Thus we have T = f + T ... Page 15

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**average**and that it is relatively stationary in time . This is not always the case . When the equation of continuity is averaged we get , with the specified notation , др a + ρί ; Ət ах ; др at д дх ́ ( p + p ' ) ( U ; + u ; ) др a + at ...### Contents

3 | |

2 THE STATE OF MATTER NEAR THE INTERFACE | 36 |

3 RADIATION | 75 |

4 SURFACE WIND WAVES | 103 |

5 TURBULENT TRANSFER NEAR THE INTERFACE | 137 |

6 THE PLANETARY BOUNDARY LAYER | 182 |

7 ATMOSPHERICALLY FORCED PERTURBATIONS IN THE OCEANS | 238 |

8 LARGESCALE FORCING BY SEA SURFACE BUOYANCY FLUXES | 292 |

REFERENCES | 326 |

Author Index | 351 |

Subject Index | 356 |

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### Common terms and phrases

advection air-sea amplitude approximation Atmos atmosphere average baroclinic barotropic boundary layer bubbles buoyancy buoyancy flux Businger circulation cloud coefficient component constant convection Coriolis Coriolis force decreases density depth diffusivity discussed dissipation eddy effect Ekman Ekman layer Ekman transport energy entrainment equation equatorial equilibrium flow fluid force frequency function Geophys geostrophic gradient gravity waves group velocity height horizontal hurricane increases indicated instability interactions interface internal waves irradiance Kelvin waves latitude long-wave measurements meridional mixed layer mixed-layer molecular momentum motion observations parameterization perturbations phase planetary boundary layer potential temperature pressure processes propagate radiance radiation ratio relatively represents resulting Rossby waves salinity sea surface sea water Section sensible heat shear short-wave specific specific humidity spectra spectrum storm surface layer surface temperature surface waves tends term thermocline transport turbulent upwelling vector viscosity water vapour wavelength wavenumber wind stress windspeed дх

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Page 74 - The radiation energy per unit time coming from a specific direction and passing through a unit area perpendicular to that direction is called the radiance, I.