Abe, considering that density is proportional to pressure and to the gradient of pressure, 

 obtained 



dp=kpdz, fi^ 



where p is the density, s is the depth of the layer, and k is the coefficient of proportionality. 



P = Caekz, (2) 



Abe determined the constants entering into the formula (2) from his measurements at 7 levels 

 of snow which were about 70 cm and finally obtained 



p = 0.1854e0,O0545z, (3) 



where s is expressed in centimeters. 



According to Shepelevskii, the density of snow remains unchanged to a certain depth, inas- 

 much as the density of the snowflakes is sufficient here to support the light weight of the upper 

 layers. Shepelevskii, like Abe, also considers that below this depth the density of the snow changes 

 with depth according to logarithmic laws. 



Finally after a certain additional assumptions, Shepelevskii arrives at the following formulas 



P = P: 



[/^' 



^0 = o ^1 



(4) 



where p-^ is the density of snow cover at a depth H. . 



For an approximate evaluation of snow density, Kukharskii worked out the following scale 

 which proved to be useful during sled expeditions: 



Point 



1 

 2 

 3 



6,7,8 

 9,10 



Characteristics 



Loose snow not supporting one's weight at all. 



Snow, lightly compressed by the foot . 



Foot sinks up to the ankle and is supported before 

 reaching the ground or the ice. 



The foot sinks into the snow 1 to 2 cm when 

 walking. 



Snow supporting the weight of a man - the foot 

 leaves a slight print. 



Snow is dense and yields to a soft foot gear 

 and to a blow by it. 



Snow yields with difficulty to a blow by a 

 wooden stake. 



LITERATURE: 25, 133, 142. 



174 



