By Dana Bell
Air strength shades Vol 1: 1926-42
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An analogous connection between temperature and height can be obtained by introducing n-l (~:)-n- = ~: into Eq. (9). »: h _ T2) n - 1 o(l T I or (10) APPLICATION OF THE PRESSURE EQUATION 33 stating that in a polytropic atmosphere the temperature is a linear function of the height. If we again take the surface of the earth as the origin of our height scale by setting hI = 0, and instead of h 2 write the variable height h, Eqs. (9) and (10) become n - 1 h)n:'l P = PI( 1 - - - n ho and T = h) n - 1 TIl ( - -n- h- o .
A rise in temperature at the surface of the earth due to sunshine produces an tOe" unstable distribution; rising currents of FIG. -Surface cooling, air and corresponding down currents are as a result of which a very stable distribution is prothe result (Fig. 26). The inversion of duced. ) out and the heat boundary A lA 2 moves continually higher. Each rising air current goes a little higher than the previous one and then spreads out where it reaches equilibrium. The air between these ascending currents sinks downward to fill up the gaps.
16, of length l, width b, and immersed depth t. Let the height of the center of gravity above the bottom surface be c. The moments of inertia of the water-line cross section are 28 FUNDAMENTALS OF HYDRO- AND AEROMECHANICS [1 = lb 3 j 12 for the longitudinal axis through the center of gravity, and [2 = l3bj12 for the lateral axis through the center of gravity. Equation (10) states that the stability decreases with the moment of inertia, and, since it was assumed that l > band therefore [2 > [1, the measure of the smallest occurring stability is [1 lb3 h = 11 - a = 12V - a.