. Collected reprints / Atlantic Oceanographic and Meteorological Laboratories [and] Pacific Oceanographic Laboratories. Oceanography AUTOCHTHONOUS PATTERNS OF SEDIMENTATION 327. 39°30 - 39-00 38-30' 74-30' 74-00 73-30' 73-00' 72-30' FIGURE 17. Fair-weather hydraulic regime of the Sew Jersey shelf as indicated by Savoniits rotor current meters mounted to m above the seafloor at jour stations on the New Jersey shelf, for periods of 9 to 11 days in late spring. Progressive vector diagrams indicate a general southerly water drift, partly correlatable with wind directions (McC
. Collected reprints / Atlantic Oceanographic and Meteorological Laboratories [and] Pacific Oceanographic Laboratories. Oceanography AUTOCHTHONOUS PATTERNS OF SEDIMENTATION 327. 39°30 - 39-00 38-30' 74-30' 74-00 73-30' 73-00' 72-30' FIGURE 17. Fair-weather hydraulic regime of the Sew Jersey shelf as indicated by Savoniits rotor current meters mounted to m above the seafloor at jour stations on the New Jersey shelf, for periods of 9 to 11 days in late spring. Progressive vector diagrams indicate a general southerly water drift, partly correlatable with wind directions (McC/en- nen, 7973). Loops, spikes, and bulges on progressive vector diagrams are modulation by the semidiurnal tide. In percent exceedence diagrams, current velocities are compared with bottom wave surge calculated from wave climate data. All data from McC/ennen (1973). ever, neither these unidirectional flow components nor the superimposed wave oscillations (McClennen, 1973) and tidal oscillations (Redfield, 1956) are strong enough to result in significant bed load transport over broad areas. During the winter period of frequent storms, the water column is not stratified, and air-water coupling is more efficient (see discussion, pp. 263-264). The geometry of the Middle Atlantic Bight is especially conducive to strong flows during this period. When low-pressure systems pass over the bight, so that the isobars of atmospheric pressure parallel the isobaths of the shelf surface, the resulting winds blow southward down the length of the Middle Atlantic Bio;ht, parallel- ing the curve of the shoreline, and induce a uniform setup of the shelf water mass against the coast of 40 to 60 cm. High-velocity "slablike" flows of remarkable longshore coherence result (Beardslcy and Butman, 1974; Boicourt, personal communication). The coastal boundary of these storm flows appears to initiate ridge topography at the foot of the shorefacc (I)uane et al., 1972); see Chapter 14, Figs. 28 an
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