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FENNIA 66, N:o 1
21
Scandia, whereas the earlier shore-lines have been deformed irregularly,
as in Eastern Carelia and Fishers’ Peninsula1.
DISCONTINUOUS NATURE OF UPLIFT.
It would appear, therefore, that the Fennoscandian uplift area is
characterized by two concentric hinge-lines (Fig. 9). The more central
and later one encircles the buckle which developed at the end of the
Ice Age. The peripheral and earlier hinge-line again shows the outer
limit of a zone which tilted at the beginning of the Salpausselkä stages.
The inner limit of this tilted zone runs near and parallel to the ice
border line of that time. Consequently there is a fairly pronounced
relation between the retreating ice margin and the isostatic rise of
After this paper was ready for print, the author received L .von Post’s
(1938) preliminary report concerning the isobase surfaces in the
late-Quaternary Viska fiord in Western Sweden. Assuming that the diagram showing the
relations and the chronology of the shore-lines is in the main correct, the
vertical distances between the earlier late-glacial and, post-glacial shore-lines in
Western Sweden differ greatly from those observed in the Baltic basin and on
the coast of the Arctic ocean. Consequently also the mode of the land upheaval
took place in another manner. In fact, von Post sets forth that the isostatic
land rise has been twice interrupted by a retardation or a real sinking of the
earth’s crust. The intermissions are assumed to have been caused by a
temporary increase of the ice load especially at the end. of the gotiglacial time and
also afterwards.
The old and well-known idea of land sinkings and transgressions during
the late-glacial epoch has not been supported by investigations in the Baltic
basin, at least not in the Finnish part of it. On the contrary the land near the
ice-sheet has always had a tendency to rise also during the Salpausselkä stages,
as clearly seen by the relative position of the successive marine shore-lines G
and YI. Moreover, our fairly rich stratigraphical, phytopalaeontological and
morphological material does not provide any evidence whatever in favour of the
view that the Yoldia Sea of our system might have been transgressive. Only
the Rhabdonema Sea seems to have in some degree submerged the southern
coast of Finland, probably due to the eustatic rise of the sea level at the close
of the Ice Age, as was the case during the Littorina time (Hyyppä 1939).
Yon Post particularly emphasizes the preliminary character of his diagram.
In the opinion of the author especially the datings of the late-glacial shore-lines
may undergo changes and, therefore also the conclusions based upon these must
be somewhat modified in future. At present the author of this paper suggests
that the changes of level followed the same rule in Western Sweden as in other
parts of Fennoscandia so far investigated in detail. This assumption is
supported by the fine observations which von Post with his young colleagues has made
in the picturesque Viska valley and which he showed during and after the above
mentioned excursions last summer. The map of the Baltic Rhabdonema Sea
(Fig. 3) has been drawn in accordance with this view as regaids Western Sweden.
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