In the last chapter I described waves on the sea surface. Now we can consider several special and important cases: the transformation of waves as they come ashore and break; the currents and edge waves generated by the interaction of waves with coasts; tsunamis; storm surges; and tides, especially tides along coasts.
17.1 Shoaling Waves and Coastal Processes
Wave phase and group velocities are a function of depth when the depth is less than about one-quarter wavelength in deep water. Wave period and frequency are invariant (don't change as the wave comes ashore); and this is used to compute the properties of shoaling waves. Wave-height increases as wave group velocity slows. Wave-length decreases. Waves change direction due to refraction. Finally, waves break if the water is sufficiently shallow; and broken waves pour water into the surf zone, creating long-shore and rip currents.
and L is wave-length, c is phase velocity, α is the angle of the crest relative to contours of constant depth, and d is water depth. The subscript 0 indicates values in deep water.
The quantity d / L is calculated from the solution of
using an iterative technique, or from Figure 17.1 or from table A1 of Wiegel (1964).
Because wave velocity is a function of depth in shallow water, variations in offshore water depth can focus or defocus wave energy reaching the shore. Consider the simple case of waves with deep-water crests almost parallel to a straight beach with two ridges each extending seaward from a headland (Figure 17.2). Wave group velocity is faster in the deeper water between the ridges, and the wave crests become progressively deformed as the wave propagates toward the beach. Wave energy, which propagates perpendicular to wave crests, is refracted out of the region between the headland. As a result, wave energy is focused into the headlands, and breakers there are much larger than breakers in the bay. The difference in wave-height can be surprisingly large. On a calm day, breakers can be knee high shoreward of a submarine canyon at La Jolla Shores, California, just south of the Scripps Institution of Oceanography. At the same time, waves just north of the canyon can be high enough to attract surfers.
Water dumped inside the breaker zone must return offshore. It does this by first moving parallel to the beach as an along-shore current. Then it turns and flows offshore perpendicular to the beach in a narrow, swift rip current. The rips are usually spaced hundreds of meters apart (Figure 17.5). Usually there is a band of deeper water between the breaker zone and the beach, and the long-shore current runs in this channel. The strength of a rip current depends on the height and frequency of breaking waves and the strength of the onshore wind. Rips are a danger to unwary swimmers, especially poor swimmers bobbing along in the waves inside the breaker zone. They are carried along by the along-shore current until they are suddenly carried out to sea by the rip. Swimming against the rip is futile, but swimmers can escape by swimming parallel to the beach.
Edge waves are produced by the variability of wave energy reaching shore. Waves tend to come in groups, especially when waves come from distant storms. For several minutes breakers may be smaller than average, then a few very large waves will break. The minute-to-minute variation in the height of breakers produces low-frequency variability in the along-shore current. This, in turn, drives a low-frequency wave attached to the beach, an edge wave. The waves have periods of a few minutes, a long-shore wave-length of around a kilometer, and an amplitude that decays exponentially offshore (Figure 17.6).
|Department of Oceanography, Texas A&M University
Robert H. Stewart, email@example.com
All contents copyright © 2005 Robert H. Stewart,
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Updated on November 19, 2008