90 
THERMODYNAMIC METEOROLOGY 
The negative sign applies only to the characteristic 
lo g C 0 =- 5.960 Co = 9.12 X 10~ 5 
log5 = - 2.220 B = 1.66 X 10“ 2 . 
By means of Table 22 we proceed in Section II of Table 
20 to compute log c and a from log C and A. Assume an 
approximate value a x , as 3.82, and compute a x log T w from the 
value in Section I. Subtract from log K x0 for log c, and in 
Table 22 interpolate that value a 0 , which is the pair value of 
log c. If this value a 0 agrees with the assumed a x the check is 
complete. If, on the other hand, these values of log c and a 
do not quite agree, as in the examples under z = 3000, 4000, 5000, 
take the mean value between the assumed a x and computed 
do, and proceed again with a 2 to compute log c and a. The 
second trial is usually successful if a x has been chosen with some 
practice. The corresponding values of (log c . a) are found in 
the examples of Table 21, and it is seen that the irregularities 
of (log C . A) have disappeared. Log c and a usually decrease 
slowly with the elevation and with the increase of latitude from 
the equator. 
These results check by log c + a log T x0 = log K x0 . 
Application of the Thermodynamic Formulas to Various Meteor 
ological Problems 
It has seemed necessary to give an extended example of the 
method of computing the thermodynamic values in the non- 
adiabatic atmosphere, on account of the complexity of the 
computations, and because of the numerous valuable results 
dependent upon them. In Bulletin No. 3 of the Argentine 
Meteorological Office, 1913, will be found the results for many 
types of data in considerable detail. We can here summarize 
them briefly, depending upon diagrams to bring out the general 
ideas, in particular respecting the isothermal region, the diurnal 
convection, the circulation in cyclones and anti-cyclones, and 
the general circulation of the atmosphere.