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of Igaliko, where a vertical breccia zone separates the old gra- 
nite from the sandstone formation. Farther to the west the 
fault for a distance runs under the sea (Tunugdliarfik Fjord), 
but near Agpat the breccia zone reappears in the coast cliffs. 
From this point the fault line (see Fig. 25) extends southwest- 
ward, between the mountain ridge of Kitdlavat, in which the 
Algonkian granite rises to 1260 meters, and Nunasarnausak 
where the sandstone is at sea level. But the area between these 
mountains is occupied by the batholite, and no fault is exposed 
to view. Since the granite rises abruptly and without breccia- 
tion at the southeastern border of the batholite, it is evident 
that the fault cannot intersect it, and since the peculiar stra- 
tification of the batholite proves the absence of any noteworthy 
dislocations in it, it cannot traverse the Plutonic rocks. Even 
along the boundary between the old granite and the batholite 
no fault is observable: but instead the abyssal rocks show an 
ordinary contact facies with apophyses running into the granite. 
Hence the main faulting, though later than the formation 
of the sandstone and the oldest sheets of the volcanic series, 
is prior to the final consolidation of the batholites. It is 
scarcely possible to give any more precise determination of the 
age relations. At first sight it might seem probable that the 
faulting was directly connected with the intrusion of the batho- 
lites, but at this place it is only necessary to call attention to 
the fact that since the place of the Ilimausak batholite coin- 
cides with the area of maximum subsidence, the faulting can- 
not directly have forced the magma of the llimausak batholite 
into its present position. 
Comparison with the Christiania district. — Although the 
connection of a local subsidence of the earth crust with the 
occurrence of large Plutonic bodies is by no means a general 
rule, yet it is possible to cite a great number of analogous 
cases from other plateau regions. It will suffice to quote here 
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