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FENNIA 66, N:o 1
19
LAND RISE IN NORTHERN FINLAD.
Let us now see whether the two hinge-lines found in the
southeastern section of the glaciated area are traceable also in other parts
of Fennoscandia.
In the Sotkamo area (Kilpi 1937) and in the northern part of the
Baltic basin (Hyyppä 1936), the late-glacial changes of level have
taken place quite in the same manner as in Western Finland, the
uplift of the earth’s crust having been intermittent and equal
everywhere. These areas consequently lie inside the finiglacial hinge-line.
This can, however, not be placed here in detail, because the changes
of level have not been accurately studied east of the water-shed and
the Finnish frontier. We can only state that the eastern limit of the
equally uplifted central area on the whole coincides with the
ice-border line corresponding to the Salpausselkä moraines (Fig. 9). Thus,
its relation to the retreating land-ice is the same as in Western
Finland.
On the coast of the Arctic Ocean Tanner (1930) has studied the
changes of level in great detail. His diagram shows a great similarity
to that of the author as regards the later marine shore-lines counted
from the end of the gotiglacial time. During the earlier stages, from h
to I in Tanner’s system, Southern Finland was not yet uncovered.
Tanner’s water planes e + / correspond in Southern Finland to YI +
Yli + YIII, and the line c to the metachronous highest limit of the
postglacial transgression indicated by the beaches LI, LII, LIII,
LIV, LV, and, LVI in the Baltic basin. According to this connection
the Arctic coast, submerged by the Late-Quaternary Sea, corresponds
to that part of Southern Finland which lies south-east of the
finiglacial hinge-line. The differential tilting is characteristic for both
areas. The limit against the equally uplifted central area must
therefore lie farther south in Lapland. As there are only high supramarine
lands in this territory it is, however, impossible to trace the
hinge-line in detail.
In Tanner’s diagram the oldest raised shore-lines on the ocean
coast show different degrees of inclination. The greater differences
may of course be due either to a rapid temporary tilting or to a slow
differential uplift during a longer time. As, however, the more
accurate time relations are quite unknown there, we cannot answer the
question about the presence or absence of the gotiglacial hinge-line.
Instead, we find that the most peripheral zone is faulted, the Cambrian
sediments of the Fishers’ Peninsula having dropped about 15 m. in
relation to the Archaean continent. This occurred, not at the retreat-
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