66
'
y
Homogeneous Models of the Ocean Circulation
c
0
0.0
0~----------------------------~~
xFig. 2.12.la--d. Solutions of the wind-driven circulation problem for the case where only bottom
friction balances the wind input of vorticity. Each panel corresponds to an increasing value of the
ratio 6/l>s. a 6/6s = 1. b 6/6s = 2. c 6/6s = 4. d 6/6s = 8. (From Veronis 1966, reprinted from
Pedlosky 1987)
figure, there is only a slight north-south asymmetry produced by the northward
advection of vorticity. As the inertial effects increase in magnitude, the structure of the flow changes significantly over the entire basin. A strong jet along
the northern wall appears for b I/ bs of order 2 (panel b). When the ratio reaches
4 as in panel c, there is a strong boundary jet flowing southward on the eastern
boundary. Note that in the absence of lateral friction Stewart's (1964) argud
'
y
Homogeneous Models of the Ocean Circulation
c
0
0.0
0~----------------------------~~
xFig. 2.12.la--d. Solutions of the wind-driven circulation problem for the case where only bottom
friction balances the wind input of vorticity. Each panel corresponds to an increasing value of the
ratio 6/l>s. a 6/6s = 1. b 6/6s = 2. c 6/6s = 4. d 6/6s = 8. (From Veronis 1966, reprinted from
Pedlosky 1987)
figure, there is only a slight north-south asymmetry produced by the northward
advection of vorticity. As the inertial effects increase in magnitude, the structure of the flow changes significantly over the entire basin. A strong jet along
the northern wall appears for b I/ bs of order 2 (panel b). When the ratio reaches
4 as in panel c, there is a strong boundary jet flowing southward on the eastern
boundary. Note that in the absence of lateral friction Stewart's (1964) argud