Reserves and fluxes of methane in the atmosphere-ocean-land system

Participating OH radicals form in the atmosphere during water vapor photolysis. As a result, the simplest diagram of methane oxidation in the atmosphere is the following  

Let the marsh surface temperature vary cyclically with frequency w and amplitude A, decreasing with depth 7V(0, t) = A(z) cos(ujt), where 

The solution to Equation (4.32) enables us to trace temperature variations Tw(z, t) and suggests the conclusion that in this case these variations weakly depend on TW(Q, t). Even if 7V(0, /) increases by 2°C, then according to (4.32), the amplitude of temperature changes with depth will rapidly decrease to 0.97°C, 0.33°C, and 0.01°C at depths 40cm, 2m, and 3m, respectively. Hence, with a 2°C increase in the average global atmospheric temperature, flux FlCH4 will increase by no more than 1.4%. 

The western Siberian region of Russia is characterized by numerous intensive natural and anthropogenic sources of methane formation. These are marshes, tundra, permafrost, oil and gas deposits. In this region, flux FlCH4 varies widely both during the year and shorter time periods. From measurements carried out by Jagovkina et al. (2000) on the Yamal coastline in June 1996, the CH4 concentration in the atmosphere 

The main mechanism for the formation of methane in a marsh is connected with the functioning of special groups of micro-organisms. Some methane due to diffusion is emitted to the atmosphere, but most remains in the peat layer and is gradually emitted to the atmosphere. 

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Figure 4.16. Reserves and fluxes of methane in the atmosphere-ocean-land system. From Fung et al. (1991). Notation Tg= 1012 g.

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