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Tig. 7. — Example of the variation with height of drizzle accompanying sea fog or 

 stratus. From the diagram it will be understood that the rain-producing 

 la5'-er lies at 200-400 m. above the ground and evaporation layer 0-200 m. 

 Fog situation is as follows : 490 m., top ; 490-430 m., density decreasing with 

 height ; 430-140 m., fog ; 140 m., base ;, 140-40 m., hazy ; 40-0 m., no fog. 



(11) The observations at Nemuro show that in many cases the wind 

 gets maximum velocity at a height of from 150 to 500 metres (see Figs. 

 4-6). This would be owing to topographical effects, but, as the height 

 of maximum velocity generally coincides with the height of the top of 

 the inversion, there might be some other causes. 



(12) The vapour tension of the air above a fog or stratus layer is not 

 low, except in some cases (see Fig 3). 



(13) In the case of sea fog it is rare that the foggy air on the sea 

 surface or on the ground is completely saturated, except in the c9.se of 

 very dense fog or at night when air temperature falls enough. Moreover, 

 in the fog or stratus layer portions of unsaturated air are present, 

 especially near the top and the base of the layer, and sometimes in the 

 middle part of the layer. Such unsaturation cannot be explained by the 

 ■depression of vapour pressure due to salinity of fog particles. 



A New Theory on the Formation of Sea Fog 



An outline of the theory which the present author has suggested is 

 «iven below. 



75 



