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10 Matti Sauramo, The mode of the land upheaval in Fennoscandia.
coast in Fennoscandia (R. Witting 1918). The annual rates of
upheaval in different localities are very unequal, but the mean upheaval
is entirely compensated about every lustrum. According to Witting
this is due to the fact, that the earth’s crust rises not in the form of
a rigid table and at an even velocity, but rather as a broken mosaic.
Every block of the earth’s crust rises in fits and starts, remaining
thereafter for some years in its place. Consequently, after some length
of time most of these differential movements compensate each other.
Apparently this conception helps us to understand also the nature of
the whole Late - Quaternary upheaval of Fennoscandia. Some of the
differential movements have, however, escaped complete
compensation and have preserved their individual character for thousands
of years.
SYSTEM OF THE ANCIENT BEACHES OF THE BALTIC.
An exception to this rule is easily found in the diagram, Plate I.
The lines, or rather curves in this graph represent, with greatly
exaggerated inclination, the slopes of the planes of the shore-lines in the
south-eastern section of Fennoscandia. The section in question
contains not only the whole of Southern Finland, but also
Ångermanland in the central area of land upheaval, and the Leningrad district
in the periphery. The construction is based upon a straight line LI
representing the above-mentioned initial stage of the Litt orina sea
(Fig. 1.). In the centre of Fennoscandia it has an elevation of 120 m;
in the periphery, on the Carelian Isthmus at Terijoki, near to the
eastern frontier of Finland, this shore-line dives beneath the present
sea level. All other shore-lines are placed at heights which
correspond to their real distances above and below the base line.
The first graph of this kind concerning the Baltic region was made
by the author in 1934 (Sauramo 1934). It was based upon
investigations by V. Auer (1924), E. Hyyppä (1932) on the Carelian
Isthmus, A. Hellaakoski (1928) in Central Finland, L. Aario (1932) in
North Satakunta, R. Liden (1913) in Ångermanland, and K. K.
Markow (1931) around Leningrad. The system of the late-glacial
shorelines was studied by the author, but the material concerning these
stages has not yet been published.
In this diagram is seen a feature of particular significance bearing
on the problem in question: The late-glacial beaches northwest, that
is inside, of the great Salpausselkä recessional moraines are parallel
with each other, whereas all other shore-lines have a different degree
of tilting, the oldest invariably rising quickest when traced north-
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