6.8 The Wind-Driven Circulation of the Ocean
137
6.7.6 Additional Exercise for the Reader
Explore whether the ambient fl w fiel shown in Fig. 6.10 is subtle to the barotropic
instability process. Use L = 500 m and U = 0.2 m/s together with a constant Coriolis
parameter.
6.8 The Wind-Driven Circulation of the Ocean
6.8.1 The Dynamical Structure of the Ocean
Frictional effects are only significan in thin frictional boundary layers, called
Ekman layers, establishing near the sea surface and the seafloo of the ocean and
along coastlines. Larger-scale f ow in the ocean interior is essentially void if friction
and is therefore governed by a balance between the horizontal pressure-gradient
force and the Coriolis force – the geostrophic balance. The ocean’s dynamics can
therefore be classifie by two distinct dynamic regimes: frictional boundary layers
and the geostrophic interior (Fig. 6.11).
6.8.2 Steady-State Dynamics and Volume Transport
Steady-state dynamics reflec a state in which the surface pressure fiel that drives
geostrophic f ow has reached an equilibrium. This equilibrium implies that this
fl w, when averaged over the entire water column, is void of lateral divergence/
convergence. This can be expressed by the balance:
∂ Q x
∂ x
+
∂ Q y
∂ y
= 0
(6.40)
Fig. 6.11 The dynamical structure of the ocean
137
6.7.6 Additional Exercise for the Reader
Explore whether the ambient fl w fiel shown in Fig. 6.10 is subtle to the barotropic
instability process. Use L = 500 m and U = 0.2 m/s together with a constant Coriolis
parameter.
6.8 The Wind-Driven Circulation of the Ocean
6.8.1 The Dynamical Structure of the Ocean
Frictional effects are only significan in thin frictional boundary layers, called
Ekman layers, establishing near the sea surface and the seafloo of the ocean and
along coastlines. Larger-scale f ow in the ocean interior is essentially void if friction
and is therefore governed by a balance between the horizontal pressure-gradient
force and the Coriolis force – the geostrophic balance. The ocean’s dynamics can
therefore be classifie by two distinct dynamic regimes: frictional boundary layers
and the geostrophic interior (Fig. 6.11).
6.8.2 Steady-State Dynamics and Volume Transport
Steady-state dynamics reflec a state in which the surface pressure fiel that drives
geostrophic f ow has reached an equilibrium. This equilibrium implies that this
fl w, when averaged over the entire water column, is void of lateral divergence/
convergence. This can be expressed by the balance:
∂ Q x
∂ x
+
∂ Q y
∂ y
= 0
(6.40)
Fig. 6.11 The dynamical structure of the ocean