Download Atmospheric Science Across the Stratopause by David E. Siskind, Stephen D. Eckermann, Michael E. Summers PDF

By David E. Siskind, Stephen D. Eckermann, Michael E. Summers

ISBN-10: 0875909817

ISBN-13: 9780875909813

ISBN-10: 1118668391

ISBN-13: 9781118668399

Published by means of the yank Geophysical Union as a part of the Geophysical Monograph Series.

lately, separate geophysical study cultures have constructed within the usa to review the ambience: one in every of area scientists, who specialize in the mesosphere, thermosphere and ionosphere, and the opposite of atmospheric scientists, who specialize in the troposphere and stratosphere. The boundary among those study domain names approximately coincides with the stratopause (50 km). whereas the department ofthe surroundings into layers and limits serves as an invaluable approach to symbolize some of the chemical and dynamical techniques that distinguish those layers, those limitations should not impermeable. to appreciate such severe concerns as worldwide switch, geophysicists needs to examine the ambience as an built-in method. the aim of this monograph is to spotlight these experiences that examine the coupling of those areas and therefore compile medical specialties (atmospheric technology and area technology) which are usually thought of separately.Content:

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Extra info for Atmospheric Science Across the Stratopause

Sample text

For linear gravity waves (neglecting the Coriolis force) is: activity in the vicinity of the critical line. The critical line is (v - uk) = v = N k [m +k + (10) surrounded by a critical layer in which com-plex nonlinear processes dominate, and mean-flow forcing occurs. The Rossby wave-breaking process described above is associated with a westward force on the stratospheric mean where v = v - uk is referred to as the Doppler shifted fre­ flow. The associated mixing is quasi-isentropic, mixing air quency or intrinsic frequency; k is the horizontal waveparcels horizontally over large distance scales in the mid- number; and u is the component of the wind in the latitude "surf zone" Mclntyre and Palmer [1984], but giving direction of wave propagation here referred to as the x direction.

The coldest tempera­ tures occur during northern winter when the upward mass flux is at its maximum, and warmest temperatures occur in northern summer when the upward mass flux is at its minimum. Because the saturation mixing ratio for water is strongly temperature dependent, and air passing through the tropical tropopause tends to be "freeze dried" to its satura­ tion mixing ratio at the temperature of the tropopause, the mixing ratio for water vapor entering the tropical strato­ sphere also undergoes a strong annual cycle.

In order to appreciate the role of the wave-induced global circulation in determining the distribution of longlived tracers in the middle atmosphere, it is useful to consider a hypothetical atmosphere in which there are no wave motions, and hence no wave-induced zonal force. In that case the middle atmosphere would relax to radiative equilibrium, the transport circulation would vanish, and the distribution of the tracer would be determined at each altitude by a balance between slow upward diffusion and photochemical destruction.

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