Data for high wave conditions observed by the OWS “Weather Reporter” in December 1959

Bretschneider, Charles L.; Crutcher, Harold L.; Darbyshire, J.; Neumann, Gerhard; Pierson, Willard J.; Walden, Hans; Wilson, Basil W.

doi:10.1007/bf02314740

Cited by 19 publications

(11 citation statements)

References 6 publications

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“…For the same wind speed at two different times the significant wave height can be significantly different. A similar conclusion was made by Crutcher[Bretschneider et al, 1962] for other weather situations.…”

supporting

confidence: 86%

“…Also, high resolution is obtained for the power spectra, so that different interpretations of the way that power spectra change during a storm at sea can be checked against each other. The for•mat of the presentation of the results from this storm follows closely that of the 1959 North Atlantic storm as reported by Bretschneider et al [1962] and of the 1968 North Atlantic storm as reported by Snider and Chakrabarti [1973]. Other storms in this area have been analyzed by Moskowitz et al [1962Moskowitz et al [ , 1963Moskowitz et al [ , 1965.…”

supporting

confidence: 66%

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High-wave conditions observed over the North Atlantic in September 1961

Chakrabarti¹

1976

J. Geophys. Res.

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The Ocean Weather Ship Weather Reporter, underway from the United Kingdom to assume her position at station J (near 53°N, 18°W) on the North Atlantic, encountered heavy seas over a 4‐day period from September 12–15, 1961. The ship measured the sea state during this period with a shipborne wave recorder at 3‐hour intervals. The wave energy spectra are computed from these records and are presented. The upper and lower confidence limits in the estimation of these energy spectra are discussed. Such statistical quantities as the significant wave height and the average period are presented.

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supporting

confidence: 86%

supporting

confidence: 66%

High-wave conditions observed over the North Atlantic in September 1961

Chakrabarti¹

1976

J. Geophys. Res.

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“…For light winds, the gravity waves are usually higher than would be predicted for a fully developed sea, and for high winds, they are usually lower [Moskowitz, 1964]. Gravity waves generally lag the wind as the wind increases and lead the wind as it decreases [Bretschnieder et al, 1962]. The behavior of the slope spectrum has not been routinely measured.…”

Section: Departures From the Fully Developed Spectrum Of The Modelmentioning

confidence: 93%

Radar scattering and equilibrium ranges in wind‐generated waves with application to scatterometry

1987

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A composite divided scale model for radar backscatter from the ocean surface is constructed. The primary scattering mechanism is assumed to be Bragg scattering for which the normalized radar backscattering cross section is proportional to the spectral density of the resonant Bragg water waves. The form of the high-wave number equilibrium spectrum is derived on the assumption that the shortwave energy density reflects a balance between direct wind forcing and dissipation due to breaking and to viscosity. This theoretical equilibrium spectrum links the wave spectrum to the wind. This spectrum is then used in a two-scale Bragg-scattering model to link backscattering cross section to the full wave spectrum, which is this high-wave number spectrum plus a gravity wave spectrum for fully developed seas. The effects of tilt and modulation of the Bragg resonant waves by the longer waves are included along with the contribution from specular reflection at low incidence angles. The model is tested against aircraft circle flight K u band radar backscatter measurements with encouraging results for vertical polarization. It is demonstrated that particularly at low wind speeds, scatterometry is sensitive to surface water temperature through its effect on the viscous dissipation of short waves. Also for low wind speeds and low incidence angles (20 ø or so) an additional source of specular backscatter needs to be considered: that due to gravity waves that may be left over from previously higher winds or that enter the area as swell. For high incidence angles and high winds, the two-scale Bragg model yields values that are somewhat low compared with the data for vertical polarization. For horizontal polarization the model is somewhat low for a 40 ø incidence angle and much too low for higher incidence angles by amounts that cannot be explained by a combination of possible wind speed measurement errors and bias errors in the measurement of the backscatter. An explanation for these results is offered in terms of recent studies of backscatter from wedges and spilling breakers for Ku band. The model is then exercised over a much wider wind speed range from L band to K a band. For high wind speeds at anemometer height, except at L band, according to the model, the backscattering cross section becomes less sensitive to wind speed and at very high speeds decreases as the wind speed increases. The wind speed at which this "rollover" occurs is dependent on radar wavelength and incidence angle, being as low as 30 m s-• for K• band for vertical polarization at some incidence angles. The effect of wedges and breakers may overcome the predicted "rollover," especially for horizontal polarization, but there are data to support a tendency toward saturation for vertical polarization at perhaps a somewhat higher wind speed. The two-scale model does not appear to be sensitive to variations in the slopes of the tilting waves that would be present for nonfully developed seas. The number and size of wedges and spilling breakers will be a function of fe...

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“…This effect, which is de. scribed by the term, "dead sea," is illustrated by Bretschneider et al [1962]. Waves higher than those associated with the locally measured wind can also propagate to the measurement site not only as swell from a distant source but also from areas of higher wind a few hundred kilometers away.…”

Section: The Three Data Setsmentioning

confidence: 99%

The dependence of wind stress on wave height and wind speed

Blake¹

1991

J. Geophys. Res.

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2l•ree near-neutral boundary layer data sets were investigated with the aim of finding a dependence of wind stress on both wind speed and significant wave height. The data set most representative of open ocean wave height, wind speed, and momentum flux conditions, was selected and analyzed by means of the least squares method to produce a new parameterization for the wind stress as a function of both wind speed and significant wave height. This study shows that the wind stress, and consequently the drag coefficient, decreases with increasing wave height for a fixed wind speed. The study also shows that the curvature of the wind profile decreases with increasing wave height and that the Co• = A + B0(10) form for the drag coefficient parameterization is inadequate. A drag coefficient that applies to both smooth and rough flows is proposed. These results are more applicable for open ocean, deep water conditions and less applicable for sheltered, closed, shallow water sites.

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Data for high wave conditions observed by the OWS “Weather Reporter” in December 1959

Cited by 19 publications

References 6 publications

High-wave conditions observed over the North Atlantic in September 1961

High-wave conditions observed over the North Atlantic in September 1961

Radar scattering and equilibrium ranges in wind‐generated waves with application to scatterometry

The dependence of wind stress on wave height and wind speed

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