Bigelow — Radiation in the Earth? s Atmosphere. 265 



From equation (i) we obtain the differential and funda- 

 mental equation connecting pressure, circulation and radiation, 



— dY = gpclz + pqdq + pdQ 



— dP — gdm + pqdq -f pdQ 



When there is no circulation and no radiation the variation of 

 pressure is proportional to the change of mass, and this is the 

 adiabatic state. This is the assumption which E. Gold makes 



Fig. 2. Temperature, Heat and Specific Heat. 



in his paper,* but it excludes the radiation term under discus- 

 sion from the several following dependent formulas. It is 

 desirable to separate the various sources of radiation from the 

 total effect in any layer, but it must be done through a direct 

 study of the observational data in order to be able to construct 

 a system of analytic equations that will classify the series of 

 causes and effects. It is believed that the data in hand have 

 such possioilities and the problems involved will be further 

 studied. 



Figs. 2 and 3 indicate some of the general reactions from the 

 surface to 18,000 meters in height. The isothermal region begins 

 generally in Europe at 12,000 m., but in the tropics at 15,000 m. 

 The specific heat and the heat lost in the stratum have very sim- 

 ilar distributions. The heat (Q 1 — Q ) has two sources of supply 

 in addition to that of the radiating surface, as shown by the 

 curves, the first in the lower cloud region of condensing 

 aqueous vapor, 000 to 2,000 m., and the second at the upper 



* The Isothermal Layer of the Atmosphere and Atmospheric Eadiation, 

 Proc. Royal Soc, A., vol. lxxxii, page 58, Reprint, 1908. 



