By Ian S. F. Jones, Yoshiaki Toba
ISBN-10: 0511552076
ISBN-13: 9780511552076
ISBN-10: 0521090490
ISBN-13: 9780521090490
ISBN-10: 0521662435
ISBN-13: 9780521662437
Parameterization of the wind stress--drag--over the sea is important to many elements of air-sea interplay, which in flip is key for versions of climate prediction and weather modeling. Wind rigidity over the sea brings jointly thirty of the world's major specialists in air-sea interplay, lower than the auspices of the medical Committee on Oceanic study. The contributed chapters come up with the money for a radical reexamination of the actual techniques that move momentum among the ambience and the sea. as well as overlaying verified basics, the booklet additionally explores energetic components of study and controversy for researchers and graduate scholars in actual oceanography, meteorology, fluid dynamics, and coastal engineering.
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Extra resources for Wind Stress over the Ocean
Example text
There is the suggestion by Csanady (1974) that for low winds the interface may act as a flexible surface that can damp turbulence and reduce the drag coefficient. Drag coefficients less than that of a smooth flat plate have been observed. Incipient ice formation in cold conditions may be another complication. The surface tension at the air-water interface is influenced by biological processes. Waves of length order 2 cm travel at the slowest speed and shorter waves travel faster and are increasingly dominated by surface tension.
8 and the phase speed of the peak components travel more quickly. This effect has been called "downshifting". The empirical rules show that the characteristic wind-wave becomes less steep with increasing fetch. It is not the frequency spectrum that is actually needed in the form drag calculation of Eq. 8) but rather the wavenumber spectrum. Let us define the spectrum F(k) as that dependent on the wavenumber magnitude and averaged over all wave directions. This quantity is discussed in some detail in Chapter 4.
Initially the wind-wave spectrum is undersaturated and demands more momentum. The phase speed of the peak frequency slowly increases and the windsea ages. For unsteady falling winds, oversaturation follows and there seems to be some empirical evidence, discussed in Chapter 9, that zog/ul takes on a lower value than in the steady case. One would think this question could be resolved from an examination of the measured drag values. 13 shows a selection of drag measurements, with steady and unsteady winds, young and old wind-waves.
Wind Stress over the Ocean by Ian S. F. Jones, Yoshiaki Toba
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