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3.5.4: Sea versus swell waves

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    From Sect. 3.4 we know that we may think of an irregular wave train as a sum of sine waves with various periods. For not too long periods of time (maybe an hour and distances of tens of kilometres) and for small amplitudes these sine waves have constant amplitudes and random phases. They travel in many different directions, all at their own velocity given by the so-called dispersion relation according to Airy or linear wave theory.

    Wave fields disperse (spread out) since the different harmonic components travel at different speeds that depend on their frequency. In Sect. 3.5.2 we referred to this phenomenon as frequency dispersion. From the dispersion relation it becomes clear that longer waves travel faster than shorter waves. Also, we have seen that the group velocity (the velocity of the front) is larger for longer period waves.

    截屏2021-10-14 下午9.27.55.png
    Figure 3.12: Swell waves arriving at the Atlantic coast of Angola from two distinct directions (southwest and northwest). This swell is generated by trade winds. Courtesy Stefanie Ross

    At some distance from the storm centre one would therefore first experience a long fast travelling swell and later an increasingly shorter wave period. At long distances from the storm centre the shorter waves are filtered out since dissipation processes (due to currents, white-capping) more strongly affect the shorter waves3. As a result only a long, and fairly regular (as the various components travel at different speeds) swell remains. Besides, the swell is uni-directional crested because only waves travelling in a particular direction end up at a certain location away from the storm centre. The spreading due to different directions of propagation is called direction dispersion. Due to frequency and direction dispersion the spectrum of swell is narrow in frequency and direction respectively. As a result of spreading (and energy dissipation) swell is relatively low. Figure 3.12 shows swell waves arriving at the coast of Angola that have been generated in two different storms.

    截屏2021-10-14 下午9.29.55.png
    Figure 3.13: The effect of swell decay on wave period and wave height in the case of a 6.1 m high, 10-second wave according to J. L. Davies and Clayton (1980).

    The characteristics of swell waves at a particular (coastal) location are determined by the characteristics of the storm and the distance to the storm. Swell can travel the oceans for thousands of kilometres. A 10 s swell wave travels at the speed \(c_0 \approx 1.56 T = 1.56 \times 10 = 15.6\ m/s = 56\ km/h\). The group velocity will be about half of that (in deep water). In Fig. 3.13 a graph is shown with wave height and period as a function of propagation distance from the storm centre.

    At first order, no mass transport is associated with short wave propagation such that the path of swell through the oceans is unaffected by the Coriolis effect. Swell therefore travels the globe along great circles, the shortest distance between two locations on a spherical object.

    截屏2021-10-14 下午9.30.21.png
    Figure 3.14: At a location off the Dutch coast, a northerly swell, generated by a storm off the Norwegian coast, meets a southwesterly sea generated by a local breeze (left). The 2D spectrum represents the spectral energy as a function of frequency and direction and is constructed by combining JONSWAP spectral shapes with Gaussian directional distributions. The 1D spectrum is obtained through integration over all directions. Even though in the 2D spectrum the swell peak is higher than the sea peak, the sea peak is the larger peak in the 1D spectrum because of the larger directional spreading for sea as compared to swell.

    Some coasts around the world – for instance Australia – mainly experience swell waves, which have been generated in storms far away. A typical wave spectrum will then be narrow-banded. For other coasts, locally generated storm waves dominate the wave climate, as is the case for the Dutch coast. The sea state then is irregular and short-crested. Most of the times wave records off the Dutch coast show both swell waves as generated in distant storms and storm waves locally generated. Two distinct peaks can then be observed in the spectrum, see Fig. 3.14. The swell can only come from the north and is usually not older than a day or sometimes two days.

    3. In addition to dissipation and dispersion, non-linear wave transfer plays a role; energy is moved from the centre of the spectrum to both the higher and lower frequencies. The higher frequencies get sub- sequently dissipated, whereas the lower frequencies gain energy.

    This page titled 3.5.4: Sea versus swell waves is shared under a CC BY-NC-SA 4.0 license and was authored, remixed, and/or curated by Judith Bosboom & Marcel J.F. Stive (TU Delft Open) via source content that was edited to the style and standards of the LibreTexts platform; a detailed edit history is available upon request.