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Publisher: Co-Action Publishing
Journal: Tellus A
Languages: English
Types: Article
Shallow, surface plumes of buoyant water are frequently discharged into coastal waters by rivers, bays, power plants, and other sources. The most readily observed portion of these plumes is the near field where the initial expansion of plume water occurs, and where there is large contrast between plume and ambient water. In contrast to existing turbulent jet models of such plumes, the present model divides the plume near field into two domains, a frontal domain where turbulent exchange between plume and ambient water is intense, and the remainder of the flow where the dynamics of inviscid, nonlinear gravitational spreading of a shallow buoyant layer dominates. Using this approach, the steady state flow produced by the supercritical outflow of buoyant water from a channel at a coast into ambient water with a uniform alongshore current is modelled. Earth rotation is neglected. Frontal jump conditions developed in an earlier paper are applied to match the flow at the frontal boundary with the remainder of the plume. Numerical solutions for the entire flow are found by the method of characteristics, but much of the flow can be determined by simpler analytic computation. The computed flow fields show that a frontal boundary forms on the upstream or offshore side of the plume where the oncoming ambient current contains the gravitational spreading of the buoyant water. No front forms on the corresponding downstream, inshore side. In the body of the plume the flow simultaneously expands and turns downstream toward alignment with the ambient current. Relatively little change in plume water speed occurs, but the pressure field required for turning the flow downstream results in deepening of the plume interface offshore near the front. This, in turn, concentrates plume volume flux along its offshore side near the front. The maximum angle through which the flow may be turned initially is less than 66°. Outlet channel angles greater than this produce plumes which are separated from the shoreline by ambient water. The model results explain many of the observed features of the Connecticut River plume in Long Island Sound.DOI: 10.1111/j.2153-3490.1982.tb01818.x
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    • Abbott, M. B. 1961. On the spreading of one fluid over Garvine, R. W. 1981. Frontal jump conditions for another. L a Houille Blanche 622-628 and 827-846. models of shallow, buoyant surface layer dynamics.
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    • Ferri, A. 1954. The method of characteristics. Section G. Jirka, G. 1980. Two-dimensional density current from In General Theory of High Speed Aerodynamics (ed.) continuous source in stratified crossflow. Proc. 2nd W . R. Sears. Vol. VI, High Speed Aerodynamics and Int. Symp. on StratiJed Flows 2,860-870. Jet Propulsion. Princeton: Princeton Univ. Press, Kao, T. W., Park, C. and Pao, H.-P. 1977. Buoyant 583-669. surface discharge and small-scale oceanic fronts: a
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    • Garvine, R. W. 1977. Observations of the motion field of Stoker, J. J. 1957. Water Waves. New York: Inthe Connecticut River plume. J. Geophys. Res. 82, terscience Publishers, Inc. 4 4 1 4 5 4 . Stronach, J. A. 1981. The Fraser River plume, Strait of Georgia. Ocean Management. 6,201-22 1.
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