about the restoration of equilibrium, which, is being constantly disturbed from below. The principal periodical winds—such as the trade-winds, the monsoons, the land and sea breezes—are found to be essentially dependent on periodical variations of atmospheric pressure, accompanying variations of temperature due to geographical position or surface conditions. The proximate causes of the more characteristic winds have also been well made out. These, too, are due to atmospheric disturbances producing areas of high or low pressure; the rapidity and intensity of the development of which, with the direction of their paths and their position, determine the force of the wind, the direction in which it blows, and the manner in which it veers or backs, that is, changes its direction. But how the changes of pressure are determined, and what causes the transfer of the disturbed area, commonly under the form of an atmospheric eddy or vortex, in a definite direction, usually from west to east, is still to be ascertained; though here, too, it is obvious that the distribution of the land and sea areas, and of the ocean-currents, on which the temperature of the superincumbent air so immediately depends, combined with the rotatory motion of the earth, are among the principal agencies at work.
Among the most intricate problems of meteorology are those relating to the evaporation of water, the formation of vapor and its diffusion and suspension in the air, and its condensation as cloud, rain, or snow. The low specific gravity of aqueous vapor, and the consequent evaporation that releases it at the earth's surface, tend to diffuse it in accordance with the mechanical laws which govern elastic fluids. But the reduction of the temperature of the air in ascending above the surface renders this diffusion impossible beyond a certain point; and observation shows that the quantity of vapor actually existing in the upper parts of the atmosphere is mainly dependent on temperature, and amounts to not more than one fourth part of what would be present if it were diffused freely and simply obeyed the law of hydrostatic pressure. It follows that a height in the atmosphere is at length necessarily reached where condensation must take place and clouds or rains be formed, and that, speaking generally, the vapor in the upper strata of the air is constantly tending to a condition of unstable equilibrium, from which it may readily be once more restored to the earth in the shape of water. This sufficiently accounts for the rarity of a perfectly cloudless sky, which indeed can hardly exist excepting where such a movement of the air is going on as will carry off the aqueous vapor, as fast as it is formed by evaporation, to a region where the temperature is high enough to prevent its condensation.
The great activity of the air in discharging the functions of
