MOVEMENT OF AIR IN ANTICYCLONES POCKELS 607 



Therefore at iooo kilometers from the center the barometric 

 pressure is 3.1 +6.32= 9.42 mm lower than at the center. 



At the boundary between the inner and outer regions the gradient 

 is discontinuous, since it falls suddenly from 1.72 to 1.38; but that 

 this must be'so is evident from equations (la') since 



dr 



has different values when r = R outward and inward because of 

 the conditions as to continuity. 



In the exterior region and as the distance from the boundary circle 

 increases, the angle of deflection rapidly approximates to the normal 

 value which in our case is 58 19' = tg~ x 3/2. 



In general the winds and pressures computed in our example 

 correspond very well to those that are actually observed in baro- 

 metric maxima especially in those of the warmer season of the year 

 and where the lowest stratum of air does not play too prominent 

 a part. 



Perhaps we should have come still nearer to the actual conditions 

 of nature if we had assumed the intensity of the descending current 

 of air in the interior region of the anticyclone, not constant, but 

 diminishing toward the boundary so that at the boundary between the 

 inner and outer regions a continuous transition exists for the verti- 

 cal velocity component and consequently for the gradient. A 

 simple assumption of this kind for the vertical velocity at the alti- 

 tude unity above the earth's surface is 



rl 1 y R 



where 11 may be any positive number, for in accord with this theorem 

 w attains its greatest value y at the center of the anticyclone but 

 disappears at the boundary circle whose radius is R. 



For this value of w the equation of continuity (Ic') becomes 



d(rV n ) f , / r \» 



dr --r^ l -\RJ 



and by integration 



1 r r n+1 



V n= - 2 rr + n~+2 ~R" 



where again the constant of integration is unnecessary. 5 

 * It is zero as in equation CO. — C. A. 



