52S 



F. II. Bigelow — Thermodynamics of the 



The expended heat (Q, — Q ) per 1000 meters in elevation 

 increases in amount by two distinct systems, one in the strata 

 from the surface to the isothermal layer, and another in that 

 layer. Take the differences in the columns for (Q, — Q ) of 

 Table 2, and these are found in Table 3. 



Table 3. 

 The variation in the loss of heat per 1000 meters. 



-r~ -r— = t" • (Qi — Q°) = Constants. 

 dz dz dz 



Height z 



Europe 



Tropics 



Victoria Nyanza 





— 228 



_ 





18000 



— 132 



17 



— 440 



— 442 



— 204 



16 



— 399 —346 



— 672* —378 



— 265 



15000 



— 437 



— 314 



— 190 



14 



— 253 



— 114 



— 141 



13 



— 321 



— 125 



— 118 



12 



— 211 



— 43* 



— 38* 



11 



— 101 



— 52* 



— 90 



10000 



+ 42* 



— 68* 



— 160 —143 



9 



- 97 



— 82 



— 135 



8 



-114 



— 100 —140 



— 120 



7 



— 127 —137 



— 119 



— 165 



6 



— 143 



— 181 



— 131 



5000 



— 120 



— 168 



— 145 



4 



— 150 



— 135 



— 115 



3 



— 139 



— 210 



— 49 



2 



— 164 



- 77 



-163 



— 8 



1 



— 24 



— 



000 



— 



— 



— 



Mean 



Mean 



A(Q, - Qo) 

 1000 



A(Q, - Qo) 

 1000 



= — 362 for the isothermal layer. 



— 140 for the lower layers. 



There are three facts to be noted, (1) that from the surface 

 to about 2000 meters, in the stratum within which the diurnal 

 convection is confined, the loss of heat diminishes less than in 

 the strata above 2000 meters. In the lower levels there is an 

 accession of heat which prevents as rapid cooling as in the 

 higher levels, and this is probably due to the condensation of 

 the aqueous vapor, which is a source of heat in addition to that 



