The Spectral Ocean Wave Model (SOWM), a Northern Hemisphere Computer Model for Specifying and Forecasting Ocean Wave Spectra

Pierson, Willard J.

doi:10.21236/ada118688

Cited by 22 publications

(14 citation statements)

References 9 publications

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“…A similar observation to that shown in Figure 15a, was described by McCreery [1992], who used acoustic spectral data from the Wake Island deep‐ocean hydrophone array and SOWM wave energy estimates [ Pierson , 1982] to generate the coherence plot shown in Figure 15b. The 2:1 correlation peak in the LL quadrant of Figure 15b is offset to the left from the 2:1 frequency ratio, possibly a result of inaccuracies in the SOWM wave model.…”

Section: Acoustic Signal Generationsupporting

confidence: 62%

“…A few data sets have been obtained with collocated acoustic and atmospheric measurements, but most suffer from sensor locations on land or in shallow water, inadequate instrumentation, short wind fetch, short record length, or consideration of only the frequency band near the energy peak [ Kibblewhite and Wu , 1991; Babcock et al , 1994; Wilcock et al , 1999]. McCreery et al [1993] made multiyear acoustic observations at deep bottom‐mounted hydrophones near Wake Island that were correlated with wind speeds measured at Wake Island and SOWM (Spectral Ocean Wave Model) wave hindcasts [ Pierson , 1982]. McCreery et al [1993] observed saturation of the acoustic spectrum between 1 and 8 Hz, termed the HOLU spectrum, similar to the saturation of the ocean wave energy spectrum described by Phillips [1985].…”

Section: Introductionmentioning

confidence: 99%

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Wind, waves, and acoustic background levels at Station ALOHA

Duennebier¹,

Lukas²,

Nosal³

et al. 2012

J. Geophys. Res.

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[1] Frequency spectra from deep-ocean near-bottom acoustic measurements obtained contemporaneously with wind, wave, and seismic data are described and used to determine the correlations among these data and to discuss possible causal relationships. Microseism energy appears to originate in four distinct regions relative to the hydrophone: wind waves above the sensors contribute microseism energy observed on the ocean floor; a fraction of this local wave energy propagates as seismic waves laterally, and provides a spatially integrated contribution to microseisms observed both in the ocean and on land; waves in storms generate microseism energy in deep water that travels as seismic waves to the sensor; and waves reflected from shorelines provide opposing waves that add to the microseism energy. Correlations of local wind speed with acoustic and seismic spectral time series suggest that the local Longuet-Higgins mechanism is visible in the acoustic spectrum from about 0.4 Hz to 80 Hz. Wind speed and acoustic levels at the hydrophone are poorly correlated below 0.4 Hz, implying that the microseism energy below 0.4 Hz is not typically generated by local winds. Correlation of ocean floor acoustic energy with seismic spectra from Oahu and with wave spectra near Oahu imply that wave reflections from Hawaiian coasts, wave interactions in the deep ocean near Hawaii, and storms far from Hawaii contribute energy to the seismic and acoustic spectra below 0.4 Hz. Wavefield directionality strongly influences the acoustic spectrum at frequencies below about 2 Hz, above which the acoustic levels imply near-isotropic surface wave directionality.

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Section: Acoustic Signal Generationsupporting

confidence: 62%

Section: Introductionmentioning

confidence: 99%

Wind, waves, and acoustic background levels at Station ALOHA

Duennebier¹,

Lukas²,

Nosal³

et al. 2012

J. Geophys. Res.

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“…The same conclusion was reached by Neu [1976] after comparing the METOC charts with long-term measurements from the SEDCO H oil exploration platform near Sable Island. Other researchers, such as Pierson [1982], disagree with this conclusion, particularly for short-term data, but the results analyzed from continuous instrumental recordings at the Hibernia oil field on the Grand Banks and from concurrent METOC data are in close agreement. A comparison of the exceedance distributions for a period of 1.25 years indicates that the average visual wave height H v is within _ 3% of the average instrumental data Hsig.…”

Section: Data Base and Methods Of Analysismentioning

confidence: 99%

Interannual variations and longer‐term changes in the sea state of the North Atlantic from 1970 to 1982

Neu¹

1984

J. Geophys. Res.

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A 13‐year (1970–1982) time series of 12‐hourly wave charts of the North Atlantic has been analyzed for variations in the sea state. Two types of variation were determined: first, strong 3‐ to 7‐year fluctuations; second, a continuous increase in the sea state during the 13 years. It appears that the former is the result of variations in cyclonic activities over the western North Atlantic and that the latter is caused by a steady increase in the strength of the prevailing westerly winds. The existence of such fluctuations and changes in the wave activity will affect long‐term predictions and are expected to have an important impact on the upper‐level physical, chemical, and biological processes of the ocean.

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“…(1966) and is written as In (A-12), E 0 is the spectral energy component travelling against the wind before dissipation, ED is the energy component after dissipation over one time step, Eĩ s the energy summed over all frequencies and those wave directions lying within ±90~of the wind direction, N is a dimensionless power with a value of 7 in the upwind direction decreasing to 3 in the outermost directional band, and K is a coefficient that controls dissipation and depends on the growth and propagation time step. More details on the dissipation term can be found in Pierson (1982).…”

Section: B Energy Partitioning Into Wind Sea and Swell Componentsmentioning

confidence: 99%