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R. M. Samelson

diabatic velocity W is taken here to be proportional to the difference of the square of the layer thickness h and an imposed function h * 2 ( x , y ), which can be chosen to represent heating at midlatitudes and cooling near the poles: where α w is a given constant of proportionality, and h * 2 is a given function of x and y . Although numerical solutions are possible for general dependencies of W on h and diabatic forcing, this particular choice allows a convenient analytical solution

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Baylor Fox-Kemper and Raffaele Ferrari

localized diabatic upwelling near the equator ( S s in Fig. 2 ). These authors impose heating or cooling in particular locations and infer the layer transport based on the loss or gain of fluid. Nurser and Williams (1990) consider all of the diabatic forcings in Fig. 2 . The essential balance they propose is that the northward transport of light water east of the outcrop is T north = T e + T i + T w , composed of the Ekman, interior geostrophic, and western boundary transport. These flows are

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