Impact of waves on air-sea exchange of sensible heat and momentum

Makin, V. K.; Mastenbroek, C.

doi:10.1007/bf00119442

Cited by 70 publications

(77 citation statements)

References 34 publications

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“…The main motivations to revise our original approach [Makin et al, 1995] were to introduce the correct description of MODEL, 1 turbulence in the boundary layer above waves and to develop much simpler model based on explicit (integral) equations as an alternative to the differential model by Makin and Mastenbroek [1996]. When this scheme is to be used as a module in models for different applications, for example, in a coupled sea surface-atmosphere model, described in part 2, in atmospheric circulation models to calculate surface fluxes above sea, Or in wave prognostic models to calculate the sea drag, such a simplification becomes a matter of principle.…”

Section: Discussionmentioning

confidence: 99%

Coupled sea surface‐atmosphere model: 1. Wind over waves coupling

Makin¹,

Kudryavtsev²

1999

J. Geophys. Res.

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153

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Abstract. A wind over waves coupling scheme to be used in a coupled wind waves-atmosphere model is described. The approach is based on the conservation of momentum in the marine atmospheric surface boundary layer and allows to relate the sea drag to the properties of the sea surface and the properties of the momentum exchange at the sea surface. Assumptions concerning the local balance of the turbulent kinetic energy production due to the mean and the wave-induced motions, and its dissipation, as well as the local balance between production and dissipation of the mean wave-induced energy allow to reduce the problem to two integral equations: the resistance law above waves and the coupling parameter, which are effectively solved by iterations. To calculate the wave-induced flux, the relation of Plant [1982] for the growth rate parameter is used. However, it is shown by numerical simulations that the local friction velocity rather than the total friction velocity has to be used in this relation, which makes the growth rate parameter dependent on the coupling parameter. It is shown that for light to moderate wind a significant part of the surface stress is supported by viscous drag. This is in good agreement with direct measurements under laboratory conditions. The short gravity and capillary-gravity waves play a significant role in extracting momentum and are strongly coupled with the atmosphere. This fact dictates the use of the coupled short waves-atmosphere model in the description of the energy balance of those waves.

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Section: Discussionmentioning

confidence: 99%

Coupled sea surface‐atmosphere model: 1. Wind over waves coupling

Makin¹,

Kudryavtsev²

1999

J. Geophys. Res.

Self Cite

153

160

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“…The influence of the waves on the air flow in the surface layer is often neglected or limited to a schematic approach. While comprehensive models are available for the air flow over periodic waves [e.g., Makin and Mastenbroek, 1996], the modeling of the air flow over breaking waves remains difficult. Consequently, the maximum in droplet concentrations at 1-2 m above the surface as observed by De Leeuw [1990a] has been explained both in terms of recirculation of droplets in wave rotors [De Leeuw, 1990b] and in terms of the spume mechanism inherently producing droplets at the height of the wave crests [Monahan et al, 1986].…”

Section: Introductionmentioning

confidence: 99%

SeaCluse: Numerical simulation of evaporating sea spray droplets

Eijk¹,

Tranchant²,

Mestayer³

2001

J. Geophys. Res.

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Abstract. The SeaCluse computer code calculates the nonlinear interactions between sea spray droplet concentrations and the scalar fields of water vapor concentration and temperature in the marine atmospheric surface layer. The code simulates most of the dynamics of the evaporating sea spray droplets in the turbulent air flow over a wavy surface, the thermodynamic transformations of the spray droplets, and the influence of the droplets on the structure of the lower marine atmosphere. The main processor computes along the vertical the horizontally averaged budgets of droplet concentration, water vapor concentration, and sensible heat, including the dynamic and thermodynamic air-droplet interactions. This paper presents the first simulations of evaporating sea spray droplets made with the SeaCluse model. It is shown that common assumptions such as exponential vertical concentration profiles and the evaporation of all droplets to their equilibrium radius do not necessarily hold for droplets with a radius larger than -30 pm. The present results also demonstrate the importance of the nonlinear interactions between sea spray droplets and the scalar fields of water vapor and temperature. Most droplets evaporate close to the surface, in a layer of -2-3 times the wave height. The impact of evaporating sea spray droplets increases rapidly with increasing wind speed. IntroductionIn recent years, the interest in aerosols has grown appreciably as the scientific community addresses questions related to the local and global climate, visibility and health studies, airsea exchange of matter (e.g., pollutants), and the development Despite their interest and despite considerable effort, our knowledge of sea spray droplets and their role in various processes is still far from complete. This is due, in part, to the difficulties in making accurate measurements above the waves. Measurements of the vertical distribution of sea spray are still 2573

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“…The parameters of the logarithmic boundary layer can be obtained from the measurements in the wake part of the turbulent boundary layer, first, retrieving the parameters of turbulent boundary layer (U max and G) from best fit of the experimental data by equation (10) for z/G>0.15 and then calculating the parameters of the logarithmic boundary layer by the following expressions: …”

Section: The Determination Of Heat and Momentum Flows On The Velocitymentioning

confidence: 99%

“…In numerical weather prediction and climate modeling, the air-sea fluxes are parameterized through mean-flow meteorological parameters. Turbulent momentum 2 * ' u w u c , heat ' T wc and moisture ' q wc fluxes are expressed via bulk formulas through the following meteorological parameters measured at a reference level (usually h 10 =10 m above the water surface): the 10 m wind speed U 10 , the difference between the 10 m air and water temperature ǻT 10 and the difference of relative moisture at the water level and 10 m above the water surface ǻq 10 : …”

Section: Introductionmentioning

confidence: 99%

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Laboratory modelling of the transfer processes between the ocean and atmosphere in the boundary layers

et al. 2017

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Abstract. The processes of momentum and heat transfer between ocean and atmosphere in the boundary layer were investigated within laboratory modeling for a wide range of wind speed and surface wave including hurricane conditions. Experiments were carried out on the Wind-Wave Flume of the Large Thermostratified Tank of IAP RAS. A special net located under the surface at different depths allows to vary parameters of surface waves independently on wind parameters. Theory of self-similarity of air flow parameters in the flume was used to calculate values aerodynamic and heat transfer coefficients from the measured velocity and temperature profiles by Pito and hotfilm gauges respectively. Simultaneous measurements of surface elevation with system wire allow to obtain spectra and integral parameters of waves. It was demonstrated that in contrast to the drag coefficient, heat transfer coefficient is virtually independent of wind speed and wave parameters to the moment of the beginning of spray generation and then increases rapidly.

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Impact of waves on air-sea exchange of sensible heat and momentum

Cited by 70 publications

References 34 publications

Coupled sea surface‐atmosphere model: 1. Wind over waves coupling

Coupled sea surface‐atmosphere model: 1. Wind over waves coupling

SeaCluse: Numerical simulation of evaporating sea spray droplets

Laboratory modelling of the transfer processes between the ocean and atmosphere in the boundary layers

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