46 V. Ferrel on motions of Fluids and Solids 
Man, pp. 189,190.) The torsive or deflecting force which causes . ; 
the westward motion of the atmosphere and the ocean in the 
equatorial regions, and the eastward motion in the higher lati- 
tudes, has been shown to be as the velocity of the interchanging 
motion between the equatorial and the polar regions; and hence 
if this motion in both were similar, the relative amount of this 
force in each must be as the whole mass multiplied into the velo- 
city of this motion between the equator and the poles. I 
suppose the ocean to be 3 miles in depth, its mass is about 500 
times that of the atmosphere, and hence if the motion between 
the equator and the poles were only ;}, of that of the atmos- 
phere, the part of the force which gives it a westward motion 
near the equator, and an eastward motion towards the poles, 
arising from this cause, must be greater than that of the action 
of the atmosphere upon it, since the‘whole amount of this force 
in the atmosphere is not spent upon the ocean, but only that part 
which overcomes the resistances to its motions. Although the 
effect of temperature in producing a difference of density, and 
consequently of disturbing the equilibrium, is very much less in 
the ocean than in the atmosphere, yet since the amount of motion 
which a given disturbing force will produce where time is not — 
considered, depends as has been stated, upon the amount of the 
resistances, and not upon the amount of inertia to be overcome; 
and since the resistances diminish as the square of the velocity, 
a very small amount of disturbing force arising from a difference 
of density must be adequate to cause an interchanging motion in — 
the ocean between the equatorial and the polar regions equal to — 
sta Of that of the atmosphere; and hence we have reason to 
think that a greater part of the motions of the ocean is due to — 
this cause than to the action of the atmosphere upon it. 
_ 41. The motions of the ocean being similar to those of the at- 
they must cause a slight elevation of the surface about — 
mosphere, 
the parallels of 30°, and a depression at the equator and the poles, 
just as in the case of the atmosphere, except that it will be less 
in the ratio of the relative velocities of the motions of the ocean 
and of the atmosphere. If we suppose the east and west motions 
bottom of the ocean as at the surface, there would be no tenden- 
cy of the water to flow out at the bottom from beneath this 
accumulation; but since the motions there must be much less, it — 
must flow dut both towards the equator and the pole, especially - 
