STEJNEGER] ANIMALS AND PLANTS OF NORWAY 509 
eastern coasts of Norway] (the ra period, Baltic ice period) the 
land cannot have been lower than now, but sank afterwards during 
their formation continually deeper, possibly to a depth about 90 to 
100 meters lower than now (at Moss).” The idea that the Scandi- 
navian inland ice in western Norway did not extend beyond the 
heads of the fjords during any time of the second glaciation seems 
to be gaining ground among the Norwegian geologists,! and if I am 
correct in connecting the ice-free border land with Geikie’s Forestian 
Scotland, we have a satisfactory explanation of the milder climate 
and the survival of the Scoto-Atlantic biota from the previous period. 
The depression lasted a very long time in eastern Norway, but 
finally the land began slowly to rise there as the ice cap of the 
second glaciation melted away. As a concomitant event Scotland 
and the Scoto-Norwegian land bridge was submerged, Geikie’s 
Lower Turbarian stage, Scotland sinking to 45 to 50 feet (14 to 15 
meters) below present level, and the climate became cold and wet. 
In the farther southern and eastern portion of the Scandinavian 
peninsula another depression then took place, the so-called Ancylus 
depression, followed by another considerable rise, the Ancylus rise, 
during which the Baltic became a lake, the Ancylus lake. The 
climate there became warmer. 
In eastern Norway, as we have seen, there is no clear indication 
of this depression and rise to the east, but the reciprocal movement 
may well have been manifest in west Norway without having been 
demonstrated there as yet, for in Scotland there are signs of the 
reciprocity stages of rise and depression, the Upper Forestian stage 
_ with its dry and congenial climate representing the rise more or 
less synchronous with the Ancylus depression, and the Upper Tur- 
barian stage, somewhat cold and wet, representing the depression 
(25 to 30 feet, 8 to 9 meters) synchronous with the Ancylus lake 
elevation. 
The subsequent rise in Scotland must then have begun during the 
Baltic Littorina depression. By this time the gradually decreasing 
movements resulting from the original pressure of the megaglacial 
ice-cap had become so feeble that they may have left no trace at 
the extreme periphery of the area affected. 
1Even Brogger (Norges Geol. Unders., No. 31, 1900, p. 104) admits that 
“it is therefore probable that during the last great glaciation at least 
portions of the west coast [of Norway, particularly mouth of the Sognefjord] 
may have been ice-free.” 
