By E. Meszaros
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Additional resources for Atmospheric Chemistry: Fundamental Aspects
1970 Palestine, TEXAS \ \ \* 1 1 J \* i U Average tropopause 2100 / Average orofiley I I . , . 8 10 1 2 1L 16 IS 20 2 2 CH4 mixing ratio [ppm] Fig. ( B y courtesy of Tellus) An interesting feature of the vertical profile of CH, is the concentration decrease above the tropopause, which was qrst demonstrated by the measurements of Bainbridge and Heidt (1966)who made aircraft and balloon flights. This finding was later confirmed by the balloon obsbrvations of Ehhalt (1974) and the rocket measurements of Ehhalt et al.
Concerning this dimension, it is to be noted that mg kg-’ values can also be called ppmm (m: mass), which is widely used in precipitation chemistry studies (see Chapter 5 ) since for water 1 k g i 1 litre. It may be helpful for the reader that an indication is given here of the organization of the remainder ofthis book. In this chapter we will discuss the atmospheric cycle of all trace constituents including the particulate matter formed by transformation of gaseous compounds (organic vapours, gaseous nitrogen and sulfur compounds) by chemical and physical processes in the air.
However, t h s external source does not increase the atmospheric hydrogen level since hydrogen atoms are also continuously leaving the upper atmosphere. It is to be noted that Lovelock and Lodge (1972) speculate that a significant part of the escaping H, comes from CH, since according to the results of recent measurements the methane quantity reaching the stratosphere from the troposphere is about three times greater than that of H,O. Thus, the photolysis of CH, produces six times more hydrogen than the photodissociation of water vapour.
Atmospheric Chemistry: Fundamental Aspects by E. Meszaros