The rate of change of a parameter governing this force appears in the denominator of the Sverdrup (suh-VARE-drupp) transport. That parameter governing this force is the difference between the absolute and relative vorticity in the barotropic vorticity equation. Regional variation in this force leads to the beta effect. A consequence of this force's vertical component is the increased perception of gravity at the equator, called the (*) Eötvös (YOT-vosh) effect. When this force is balanced against the pressure gradient, 
The rate of change of a parameter governing this force appears in the denominator of the Sverdrup (suh-VARE-drupp) transport. That parameter governing this force is the difference between the absolute and relative vorticity in the barotropic vorticity equation. Regional variation in this force leads to the beta effect. A consequence of this force's vertical component is the increased perception of gravity at the equator, called the (*) Eötvös (YOT-vosh) effect. When this force is balanced against the pressure gradient, geostrophic phenomena occur. The determination of whether this effect is important within a system is denoted by the Rossby number. Its magnitude of acceleration can be calculated by taking the cross product of negative 2 times capital omega and v. For 10 points, identify this "fictitious" force that results from the deflection of objects when reference frames undergo rotational motion.
The rate of change of a parameter governing this force appears in the denominator of the Sverdrup (suh-VARE-drupp) transport.
Coriolis effect [or Coriolis force]