geostrophic mass transport is very small, the assumption may be 

 justified that p ~ for the purpose of estimating r. Then, from 

 (30) and table 1 for <p = 55° 



r - Hm m = 3-3* x ID" 6 [sec' 1 ] . 



In the lower layers of the atmosphere, r is on the average 

 approximately 100 times larger. H.U. Sverdrup and J. Holtsmark 

 (1917) derived for 10 North American stations average values from 

 50-100 individual observations. They found r between 7 x 10 J and 

 2.7 x 10~ 4 sec" 1 , and p between -12° and +48°. 



The height of the anemometer above the ground is of great in- 

 fluence. Both r and p decrease with height, as shown by Sverdrup 

 and Holtsmark: 



height (meters) 25 25-49 50 



r x 10 4 2.20 1.99 1.56 sec" 1 

 p 25° 20° 17° 



With increasing height, p and r decrease in the lower layer of 

 the atmosphere, but it seems that no fairly well established in- 

 formation about these friction coefficients is available for the 

 higher troposphere, which is comparable with the layer of wind 

 driven ocean circulation beneath the layer of frictional influence. 

 It may well be, that in the higher troposphere p— *- 0, magn. a ~ 2°, 

 and magn. r ~ 10 ' - 10 . 



According to equation (30) etna should vary approximately 

 proportionally to sincp, if r is considered to be constant. Since 

 a is given in table 1 by previous results, r in different lati- 

 tudes is shown in the following table: 



35 



