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b 0 =0

Sverdrup interior.  2 p + [(2*H* b 0 )/(d *|f 0 |)] ∂ x p + [2/d ] f 0 /|f 0 | ∂ y t (x) = 0. Stommel boundary. Vorticity:. b 0 =0. b 0 >0. -p ( x,y ). t (x). f -plane:. b -plane:. f const x const. f + x -. f const x const. f - x +. f + x = const. f + x = const.

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b 0 =0

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  1. Sverdrup interior 2p + [(2*H*b0)/(d*|f0|)] ∂xp + [2/d] f0/|f0| ∂yt(x)= 0 Stommel boundary Vorticity: b0=0 b0>0 -p(x,y) t(x) f-plane: b-plane: fconst xconst f+ x- fconst xconst f- x+ f+ x = const. f+ x = const.

  2. Stommel, H., 1951: An elementary explanation of why ocean currents are strongest in the West, BAMS, 32, 21-23. West East Vorticity tendencies due to 1. Planetary b-effect: Vorticity tendencies due to 2. Wind-stress Curl: Vorticity tendencies due to 3. Friction: Total vorticity tendencies: -1.0 (-9.0) +1.0 (+0.9) -1.0 (-1.0) -1.0 (-1.0) +0.1 (+10) +0.1 (+0.1) -1.9 (0.0) +0.1 (0.0) f+ x- f- x+ f+ x = const.

  3. Modeled Sea Surface Temperature Gulfstream

  4. http://science.hq.nasa.gov/oceans/physical/OSC.html

  5. Barotropic Instability of a Shear Flow (Gaussian Strip of Vorticity): y x http://www.atmos.washington.edu/~hakim/542/barotropic.html

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