VII IX XI I 



Figure 180. Average quantity of floating ice 

 drifting past Iceland. 



Figure 180 shows, according to Brooks and Kennell, the average seasonal variation in ice 

 abundance along the coast of Iceland for the period 1901 to 1924, as indicated by the floating ice 

 drifting south past Iceland along with the East Greenland current. 



Figure 181 shows, according to Meeking, the average seasonal variation of floating ice 

 along the coast of Newfoundland. The main February maximum is caused here by the movement of 

 ice from Davis Strait to this region. The lesser May maximum is caused by floating ice likewise 

 carried here from Davis Strait, but retarded in its southward movement by the slower moving ice- 

 bergs which are imbedded in the floating ice. 



Figure 182 shows the average seasonal variation in the quantity of icebergs carried out of 

 Davis Strait into the Newfoundland region as observed by the International Ice Patrol from 1900 to 

 1928. 



/ // /// IV i/ VI VII VIII /> k xi XII 



XI XII 



Figure 181. Seasonal variations in the quantity Figure 182. 

 of sea ice descending from the 

 north into the region south of New- 

 foundland. 



Average number of icebergs south of 

 Newfoundland (upper curve). Ice- 

 bergs south of Grand Banks, accord- 

 ing to Smith (lower curve). Ice 

 season lasts from middle of March 

 to middle of July. 



From the figures cited we may clearly see the peculiar seasonal variation of quantity of ice 

 carried by the East Greenland and Labrador currents. On all the curves, the maximum quantity 

 of ice falls in the summer months . 



The same sort of picture may be seen along the south coast of Spitzbergen, where the ice 

 which has formed in the northwest part of the Barents Sea drifts around South Cape and then, 



450 



