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LATE WEICHSELIAN END MORA<strong>IN</strong>ES <strong>AND</strong><br />
<strong>DEGLACIATION</strong> <strong>IN</strong> <strong>EASTERN</strong> <strong>AND</strong><br />
<strong>CENTRAL</strong> F<strong>IN</strong>LANI)<br />
Synopsis<br />
Heikki Rainio<br />
Geological Survey of Finland<br />
Espoo 1996
LATE I"ATE WEICHSELIAN WEICIISELHN END MORA<strong>IN</strong>ES MORA<strong>IN</strong>ES <strong>AND</strong> <strong>DEGLACIATION</strong><br />
DEGI"ACHTION<br />
<strong>IN</strong> <strong>EASTERN</strong> <strong>AND</strong> <strong>AND</strong> <strong>CENTRAL</strong> F<strong>IN</strong>L<strong>AND</strong> F<strong>IN</strong>II\ND<br />
Synopsis<br />
by<br />
HEIKKI HEIKKI RA<strong>IN</strong>IO RAIMO<br />
with 4 <strong>fi</strong>gures <strong>fi</strong>gures in in the text<br />
ACADEMIC DISSERTATION<br />
DISSERTATION<br />
To To be presented with the permission permission of the Faculty Faculty of Science (Geology) of<br />
the University of Helsinki, for public public critisism in in the lecture lecture room 1049,<br />
Unioninkatu 37 on June June 19th, 1996, at 12 noon<br />
Geological Survey Sunrey of Finland<br />
Espoo 1996
Rainio, Heikki 1996. Late Weichselian end moraines and deglaciation deglaciation in eastern eastern<br />
and central Finland. Geological Suruey Survey of Finlnnd, Finland, Espoo. 73 pages and 4 frgures. <strong>fi</strong>gures.<br />
At the beginning of the the Salpausselkä I I phase, phase, the the front of the ice ice sheet sheet run from<br />
Värtsilä along the Finnish-Russian border northeast to Möhkö, Möhkö, where where it crossed crossed over over<br />
into Russian Karelia. During the the Salpausselkä Salpausselkä I I phase, the ice sheet sheet front, instead<br />
of remaining stationary in North Karelia as it did farther west, withdrew. The The<br />
Tuupouaara Tuupovaara end morainc moraine deposited during the the late late Salpausselkä Salpausselkä I I phase.<br />
Salpausselkäll Salpausselkä 11 and andthe the Koitere end maraine rrwraine are largely largely contemporaneous. However, However,<br />
the relationship between the end end moraines of ofTuupovaara Tuupovaara and Koitere Koitere suggests suggests that<br />
the part part of the Koitere end moraine east of Lake Koitere may have begun to to form<br />
during the last Salpausselkä I phase, phase, at the same time as that of the the T\rupovaara<br />
Tuupovaara<br />
end moraine, and that it represents the end of Salpausselkä I phase and the the<br />
Salpausselkä 11 II phase. phase. The Koitere end end moraine moraine is is physically correlative correlative with the the<br />
Rugozero @ukajärui) (RukajärvO end end moraine in Russian Karelia. Karelia.<br />
The Pielisjtirui Pielisjärvi end end moraine constitutes constitutes the the third chain chain of ice-marginal ice-marginal deposits. deposits. Its<br />
position, position, esker analysis and and the the base level of of erosion erosion during its formation all<br />
demonstrate it to be younger younger than than Salpausselkä 11 II and the Koitere Koitere end end moraine. moraine. It<br />
may be correlative in time time with with Salpausselkä 111; III; physically physically it is is correlative correlative with the<br />
KaLeualn Kalevala moraine m.oraine in in Russian Karelia. Karelia.<br />
The The ice ice sheet sheet readvanced twice for tens ofkilometres of kilometres in late-glacial late-glacial time, time, <strong>fi</strong>rst frrst before<br />
the deposition of Salpausselkä I, and and then then again before before the deposition of ofthe the Central<br />
Finland Finland end end moraine. moraine. These extensive extensive oscillations are called the Heinola<br />
deglaciation-Salpausselkä d,eglaciation-Salpausselkä readvance readuance and the Keuruu deglaciation-Jyväskylä<br />
deglaciation-Jyuäskyla<br />
readvance, r eadu ance, respectively.<br />
Key words (GeoRef Thesaurus, AG!): AGI): glacial glacial geology, geology, glacial glacial features, features, ice-marginal<br />
ice-marginal<br />
features, Salpausselkä, Central Central Finland Finland end moraine, moraine, stratigraphy, stratigraphy, deglaciation,<br />
deglaciation,<br />
readvance, readvance, Quaternary, Pleistocene, Pleistocene, Weichselian, Weichselian, historical geology, Finland,<br />
Central Finland, Finland, Eastern Eastern Finland, Finland, Russian Federation, Federation, Republic Republic of of Karelia.<br />
Heikki Rainio Rainia<br />
Geological Geol.ogical Survey of Finland Finland<br />
F<strong>IN</strong>-02150 Espoo<br />
Finland<br />
ISBN 951-690-628-1
... realitt, reality con can sta,nd' stand eaen even thz the rrlost most inprobable improbable thaoretica,I theoretical structures structures... ... (Hermann (Hermann<br />
Broch, Sleepwalkers III)<br />
TO TO I(ARELIA KARELIA AT{D <strong>AND</strong> TO ITS IT'S PEOPLE
CONTENTS<br />
CON"IENTS<br />
Preface . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . 8<br />
Joint publications . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . 9<br />
<strong>IN</strong>TRODUCTION II{IRODUCTION . . . . ...... . ...... .......... .. . ........ .... ..... . . 9<br />
General .. ........ . .. ... . ........ ........... .... ...... . 9 I<br />
Concepts and nomenclature nomenclature ... .. .... ......... ..... ..... . .. 11<br />
HOW THE GLACIAL GIÄCIAL THEORY THEORY WAS ACCEPTED <strong>IN</strong> F<strong>IN</strong>L<strong>AND</strong> F<strong>IN</strong>IÄND .. ... ...... . 13<br />
Observations Observations calling for explanation . . . . . . . . . . . . . . . . . . . . . . . .. 13<br />
Glacial theory theory . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . .. 14 L4<br />
STUDIES STUDTES ON THE SALPAUSSELKÄS SALPAUSSELKAS .. . .. .. .. .. . . . . .... . ... . ... .. . . . 16<br />
The Salpausselkäs Salpausselkäs and eskers are understood as entities . . . . . . . . . 16<br />
The name na-e Salpausselkä Salpausselkä . ... .... ... .... . ... ....... .... . .. . 17 L7<br />
Early stages stages of systematic systematic research into into the Salpausselkäs . ...... 19<br />
Continuation of of the continental ice sheet front<br />
in North Karelia and Russian Karelia Karelia at the time<br />
the Salpausselkäs were formed forned ................... .... ..... 21 2L<br />
Interpretation of shoreline displacement displacement as<br />
a dominant factor . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . .. 22<br />
CONT<strong>IN</strong>UATION COI{I<strong>IN</strong>UATION OF THE TIIE SALPAUSSELKÄS SALPAUSSELKAS <strong>IN</strong> NORTH<br />
KARELIA <strong>IN</strong> <strong>IN</strong> THE TIIE LIGHT OF RECENT CONCEPTS . . . . . . . . . . . . . . . . . . . .. 25<br />
Biostratigraphical and morphological<br />
morphological<br />
interpretations rehabilitated ....... . ...................... 25<br />
Position Position of of the ice sheet front du during ring<br />
the the deposition deposition of Salpausselka Salpausselkä I I . . . . . . . . . . . . . . . . . . . . . . . . . . .. 25<br />
Position Position of the ice sheet front in in North Karelia<br />
during the deposition deposition of Salpausselkä Salpausselkä II II . . . . . . . . . . . . . . . . . . . . . . 28<br />
Position Position of the Pielisjäirvi Pielisjärvi end moraine chain . .. ... .. .. . ..... .. 29<br />
SALPAUSSELKA SALPAUSSELKÄ I <strong>AND</strong> <strong>AND</strong> THE CEI{ITRAL <strong>CENTRAL</strong> F<strong>IN</strong>IÄND F<strong>IN</strong>L<strong>AND</strong> END MORA<strong>IN</strong>E,<br />
RECESSIONAL OR TERM<strong>IN</strong>AL?<br />
TERM<strong>IN</strong>AL? ............................... . .... 32<br />
MATERIAL <strong>AND</strong> METTIODS METHODS OF THIS STUDY ......................... 34<br />
Mapping Mapping of deposits in North Karelia Karelia (I, IV, VI) . . . . . . . . . . . . . . .. 34<br />
Results Results from from North Karelia and the no-ing naming of<br />
geomorphological units (I, IV, VI) . . . . . . . . . . . . . . . . . . . . . . . . . .. 35<br />
Studies Studies elsewhere in southern Finland (II, III, V, VI) . . . . . . . . . . .. 35<br />
RESULTS RESULTS<br />
I.<br />
I .. . ....... ............... .. .. ........ .. . .. ........ . .<br />
11 ........ . .. . . ...... .... .. .............. . ..... .... . .<br />
111 ..... ..... ... . . . . . . . . ... ............... . ..... . ... .<br />
IV ........... .......... . . ............. . ... . .. ...... .<br />
V ....... ................. ... ....................... .<br />
VI . ...... .... . ... . ... . .... ................. .. ...... .<br />
II<br />
III<br />
Iv<br />
v<br />
VI<br />
I<br />
I<br />
11<br />
32<br />
37<br />
37<br />
38<br />
39<br />
4L 41<br />
42<br />
43
DISCUSSION<br />
DISCUSSION ... .. . .. . ....... . . . . . . ...................... . .. . 45<br />
The front of the Scandinavian Seandinavian ice iee sheet at the time<br />
Salpausselkä I was formed . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . 45<br />
The relationship between Salpausselkä Salpausselkä II 11 and<br />
the Pielisjän'i Pielisjärvi end moraine moraine ............... . ...... . .... . 47<br />
The relationship between the Central Finland and<br />
Pielisjärvi end moraines moraines . . . . . . . . . . . . . . . . . . . . . . . . . . . . . .. 48<br />
Shoreline displacement displaeement in North Karelia .. . .... . .. . ....... 48<br />
Final phases of the Alleröd chron ehron at Ilomantsi . . . . . . . . . . . . .. 50<br />
Interpretation of bottom deposits . . . . . . . . . . . . . . . . . . . . . . .. 51<br />
The Salpausselkä readvance readvanee . . . . . . . . . . . . . . . . . . . . . . . . . . .. 52<br />
The Keumu Keuruu deglaciation deglaeiation and Jyväskylä Jyväskylä readvance readvanee . . ........ 53<br />
CONCLUSIONS ..... . .. . . . ...... . . . .......... .. .............. 54 54<br />
Closing words . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . .. 57 57<br />
CONCLUSIONS .<br />
Closing words .<br />
ACKNOWLEDGEMENTS . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . .. Dt 57<br />
REFERENCES ............. ..<br />
. .............. . . . ......... . ...... 59
The thesis is based on the following following papers p"p; referred referred to by the Roman numerals:<br />
I<br />
11 II<br />
111 III<br />
IV<br />
v v<br />
VI<br />
7<br />
Rainio, H. II. 1983. 198:1. The Tuupovaara Tuupovaara end moraine in North Karelia,<br />
Eastern Finland - an ice marginal marginal formation formation of the same age as the<br />
Salpausselkä Salpausselkä ridges. Bulletin Bulletin of the Geological Society of Finland 55, b5,<br />
67-76.<br />
Rainio, H. 1985. Första Första Salpausselkä utgör rand rendzonen zonen for für en landis<br />
som avancerat avancerat pä nytt. Summary: S 'mmary: The The First Salpausselkä is a marginal<br />
formation of the the outermost outermost margin margin of a readvanced ice sheet. Geologi<br />
37 (4-5 (4-5),70-77. ), 70-77.<br />
Rainio, H., Kejonen, A., Kielosto, Kielosto, S. & Lahermo, Lahermo, P. 1986. 1g8G.<br />
Avancerade inlandsisen pä nytt nytt ocksä till till Mellan<strong>fi</strong>nska<br />
randformationen? Summary: Summary: Is the the Central Finland Finland ice-marginal<br />
formation terminal? terminal? Geologi Geologi 38, (4-5), 95-109.<br />
Rainio, H. 1991. 1991. The The Younger Younger Dryas Dryas ice-marginal ice-marginal formations formations of<br />
Southern Finland. Eastern Eastern Fennoscandian Fennoscandian Younger Dryas end<br />
moraines. moraines. In: Field conference, North Karelia, Karelia, Finland, Finland, and Karelian<br />
ASSR, ASSR, June 26 - July 4,1991. 4, 1991. Excursion guide. Rainio, H. & Saarnisto,<br />
M. (eds). Geological Survey Survey of Finland, Finland, Guide 32. 1991. Pp. Pp.25-72. 25-72.<br />
Rainio, H. 1993. The Heinola deglaciation and Salpausselkä readvance<br />
as recorded in the lithostratigraphy of the the distal area of Salpausselka<br />
Salpausselkä<br />
I at Ihalainen, Lappeenranta, Finland. In: Geological Survey of<br />
Finland, Current Research 1991-1992. Autio, S. (ed.). (ed.). Geological Survey<br />
ofFinland, of Finland, Special Paper 18, 18,53-62, 53-62, 1993.<br />
Rainio, H., Saarnisto, M. & Ekman, I. 1995. Younger Younger Dryas end<br />
moraines in in Finland and NW NW Russia. In: IGCP 253 - Termination of<br />
the Pleistocene - frnal <strong>fi</strong>nal report. Lundqvist, J., J ., Saarnisto, M. M. & Rutter, N.<br />
(eds. ). Quaternary International, 28, 179-192.<br />
179 -192.
Preface Preface<br />
Thirty or so years years aga ago it was was still still widely widely believed, believed, mainly mainly in the the light light of of<br />
interpretations of shoreline shoreline displaeement, displacement, that that the the front front of the the Seandinavian Scandinavian lee Ice<br />
Sheet ran ran from from Joensuu northwards northwards or or north-northwestwards north-northwestwards during the deposition<br />
of the Salpausselkäs. There were, were, however, no iee-marginal ice-marginal depösits to support support this this<br />
view, advoeated advocated mainly mainly by Hyyppä (1936) and Sauramo Sauro-o (1958). Hyvärinen (1966b)<br />
raised doubts about about the the tenability tenability of of the the eoneept. concept. In his master's master's thesis thesis on on the the<br />
Uimaharju end moraine, morai.e, Rainio (1965) had already already suggested that that at the the time time the the<br />
Jaamankangas and Uimaharju moraines moraines deposited deposited the the iee ice front front eontinued continued<br />
eastnortheastwards to to the the north north of Suomujärvi. Suomujärwi. The The old old general general map of Quaternary<br />
deposits (Frosterus, (Frosterus, 1920; Frosterus & Wilkman, Wilkman, 1915) also showed showed landforms landforns that<br />
might serve as extensions of of the the Salpausselkäs. The The original original aim aim of of the the present present<br />
study, study, whieh which is is a direet direct eonsequenee consequence of of the the above thesis, thesis, was was to establish establish the the<br />
position position of the the iee ice sheet sheet front front in in eastern eastern North North Karelia Karelia at at the the time time the<br />
Salpausselkäs were forming. forming.<br />
Later, Later, however, the the seope scope of of the study study enlarged to to include include the the strueture structure of the<br />
Salpausselkäs and the the Central Central Finland Finland end moraine moraine and the the stratigraphy of their<br />
proximal zones. As As data data on on euttings, cuttings, glaeial glacial striae striae and and stratigraphy aeeumulated<br />
accumulated<br />
from these these zones, it became beeame inereasingly increasingly obvious obvious that that events events during the the <strong>fi</strong>nal frnal phase phase<br />
of of glaeiation glaciation in in southern Finland were more eomplieated complicated than than had eommonly commonly been<br />
believed believed a eouple couple of of deeades decades earlier, earlier, and that the the ideas ideas of of "non-uniformity" of<br />
deglaeiation deglaciation suggested suggested many many years earlier earlier should should in in fact fact be given serious<br />
reeonsideration. reconsideration. Henee, Hence, the the last last deglaeiation deglaciation in southern southern and eentral central Finland Finland and<br />
the the position of the the large end end moraines - the the Salpausselkäs and and the the Central Finland<br />
end end moraine - were included included in in the study (Fig. 1).<br />
Thus this this study study embraees embraces two two related related major major topies: topics:<br />
1)<br />
1)<br />
2)<br />
8<br />
The Younger Dryas Dryas end moraines in in eastern North N orth Karelia Karelia and their<br />
relation relation to to the the Salpausselkäs and and large large iee-marginal ice-marginal eomplexes complexes in<br />
Russian Russian Karelia, i.e. the loeation location of the eontinental continental iee ice sheet margin margin in<br />
North Karelia at the time time of formation formation of the Salpausselkäs (I, IV, VI)<br />
and<br />
the last deglaeiation deglaciation and and the eontemporaneous contemporaneous large oseillations oscillations of the<br />
Seandinavian Scandinavian lee Ice Sheet Sheet in in southern Finland (Il, (II, IIl, III, V V and partly partly IV, [V,<br />
VI).
Joint publications<br />
9 I<br />
Publications III and and VI are arejoint joint publications. publications. The contribution of ofthe the authors are as<br />
follows: follows:<br />
The material for paper III was collected collected by the the authors authors in the course of various<br />
assignments, mainly the mapping of Quaternary deposits and the assessment of<br />
gravel resources. The contributions of of Rainio Rainio and Lahermo were made speci<strong>fi</strong>cally specifrcally<br />
with this study study in mind in connection with with the investigation investigation of the Central Finland<br />
ice-marginal formation. The observations observations of Kejonen Kejonen and Kielosto derive mainly<br />
from the western western part and and those of of Rainio and and Lahermo from the eastern part of the<br />
area. The The bulk of the the paper was compiled and written by Rainio.<br />
The authors authors ofpaper of paper VI participated participated in in studies on the Younger Dryas end moraines<br />
between Hanko and Kem in Russian Russian Karelia, Karelia, and the overall overall picture is a<br />
combination combination of of their views. Rainio Rainio dealt dealt mainly mainly with the ice-marginal deposits in<br />
Finnish North Karelia and and their their relation relation to the other parts parts of the ice-marginal<br />
landform landform chains. Saarnisto Saarnisto alone is responsible for for the discussion of late-glacial<br />
hydrology. hydrology.<br />
<strong>IN</strong>TRODUCTION<br />
General<br />
The The bedrock bedrock of of southern southern Finland is is composed of crystalline palaeo-Proterozoic rocks.<br />
The The easternmost easternmost part of the bedrock, east east of the the Pielinen-Värtsilä area, is of older,<br />
Archaean Archaean origin.<br />
In the southernmost southernmost part of of southern Finland the local local variation in elevation is<br />
slight, usually no no more than than a few tens of metres. In In central and eastern Finland,<br />
the variation is greater but still seldom over 100 m. Movements Movements of the continental<br />
ice sheet were probably affected most by the ridges in the Koli-Värtsilä area, where<br />
the maximum variation in elevation elevation is 200-250 m.<br />
Southern Finland was largely largely subaquatic at the the end of glaciation. That there were<br />
large supra-aquatic areas in central and eastern eastern Finland is revealed by the<br />
distribution of glacial and postglacial postglacial deposits (Kujansuu & Niemelä, 1984), which<br />
clearly clearly depends on whether the area was supra- supra- or subaquatic. The occurrence and<br />
structure of the Salpausselkäs and and the Central Finland Finland end moraine moraine were also<br />
affected by the position of the front of the ice sheet at which which they deposited, i.e.<br />
whether it was on land or in water (Ramsay, 1921; Rainio & Lahermo, 1985; Eronen<br />
& Vesajoki, 1988).
11<br />
Efforts to unravel unravel the his history tory of of the Salpausselkäs constitute an important chapter<br />
in the the his history tory of ofresearch research into Quaternary geology geology in Finland. Finland. Therefore, Therefore, the course<br />
taken taken by by Quaternary geological research, research, studies of the Salpausselkäs Salpausselkeis and the use<br />
of of the the Salpausselkä concept are treated treated at some length length in in what what follows. follows.<br />
Concepts an and d nomenclature<br />
Salpausselkä I, as as an entity entity of of that that name, is here here considered to to terminate at a<br />
marginal plain at the the village village of Patsola, Patsola, Värtsilä. Värtsilä. Salpausselkä Salpausselkä 11 II terminates<br />
immediately south south of the village village of Kiihtelysvaara. Kiihtelysvaara. Its Its northernmost northernmost plains plains on the<br />
basic maps (4241 04 Viesimo Viesimo and 4241 424L 05 Kiihtelysvaara) Kühtelysvaara) are Puustellinkangas,<br />
Metsälänsalo and Kirkkokangas. South ofKiihtelysvaara, of Kiihtelysvaara, Salpausselkä 11 II continues<br />
in the east up up to Sykönvaara Sykönvaara and and Kannusvaara, Kannusvaara, as agreed unanimously by<br />
researchers.<br />
The large interlobate zone zone of of Tervasuo Tervasuo (Rainio, 1990) l-990) and and the large large esker of<br />
YhdyshaIju Yhdysharju (Connection esker) esker) (Frosterus & Wilkman, 1915) 1915) continue from<br />
Salpausselkä 11 II towards Jaamankangas Jaemankangas (Fig. 2). 2). These These interlobate formations fomations were<br />
once included in in Salpausselkä 11 II (e.g. Repo, 1957). 1957).<br />
Because Because general agreement is is stilllacking still lacking as to the relation of the North Karelian<br />
end end moraines to to the Salpausselkäs, individual individual names nrmes have been proposed for each<br />
apparently synchronous marginal deposit (Rainio, 1985b). 1985b). In North Karelia the icemarginal<br />
systems corresponding to to the Salpausselkäs constitute three prominent prominent<br />
rows (Rainio et al., al., 1995, Fig. 6 6 [VI)): IVIJ): the Tuupovaara, Koitere and Pielisjärvi end<br />
moraines (Rainio, 1985b). These "continuations" of the Salpausselkäs are not,<br />
however, parallel parallelover over their entire length, length, and so so the corresponding positions ofthe<br />
ice ice front are not indisputable.<br />
The above names are are used here, as are the names <strong>fi</strong>rst <strong>fi</strong>rst used by by researchers when<br />
possible. possible. Otherwise the names are those given on basic map sheets.<br />
It is not always easy to distinguish between between an ice-marginal formation and its its<br />
proximal part. pa..--t. Here, then, the ice-marginal formation is considered to include those<br />
components that have counterparts over a fairly long distance throughout the<br />
ice-marginal formation entity; it it does not include parts that were clearly formed<br />
later than the main chain, even though they may appear to join the latter. Such<br />
parts are the Tervasuo complex and the complex of ice-marginal and and interlobate interlobate<br />
deposits between Kiihtelysvaara and Pyhäselkä.<br />
The Heinola deglaciation and the the Salpausselkä readvance refer refer to the deglaciation<br />
and readvance stage of the continental ice sheet before the deposition of<br />
Salpausselkä I as de<strong>fi</strong>ned by Okko (1962, p. 150) (see Rainio, 1985a [II], 1991, 1993).<br />
Salpausselkä I as de<strong>fi</strong>.ned by Okko ( 1962, p. 150) (see Rainio, 1985a [II], 1991, 1993).
20 km<br />
:l .,,I End Fnd moraines<br />
* /2<br />
Connection Conneclion esker eske(<br />
(i The Tmvasuo<br />
@ rne Tervasuo complex<br />
lieksa<br />
12<br />
Fig. 2. Major end end moraines moroines in in Finnish Finnish North Karelia: the the Tuupovaara,<br />
Tuupouaara,<br />
Koitere and and. Piclisjärui Pielisjärvi end end. tnoroines, moraines, as utell weil as as the the Tervasuo Teruosuo interlobate interlobote<br />
complex cornpbr ond and the the Connection Connection esker esker (Yhdysharju) (Yhd.ysharju) (modi<strong>fi</strong>ed (modiftcd (rom from Rainio<br />
et et al, al, 1995).<br />
In this this context, the zones zones of the Salpausselkäs and the Central Finland end end moraine<br />
refer to the the glaciogeologically glaciogeologically exceptionally exceptionally complex complex proximal areas areas of these<br />
landforms. landforms.<br />
The term term deglaciation phase phase is used here for for those events of the total deglaciation<br />
during which which the ice sheet did not readvance signi<strong>fi</strong>cantly. signi<strong>fi</strong>cantly. Such a term term is necessary<br />
when the the mutual relations of glacial glacial deposits - ice-marginal ice-marginal deposits and eskers in in<br />
particular - - are considered within the framework of large entities. The The Heinola<br />
deglaciation, deglaciation, for for example, is a deglaciation deglaciation phase phase that ended with the Salpausselkä<br />
readvance event.<br />
The tenn term of ofbase base level is used used as de<strong>fi</strong>ned by by Flint & Skinner (1977, p. 146-147, 146-147, G2).<br />
The geomorphological geomorphological names are conventional and and were were often often coined by by chance.<br />
They do not usually refer to strictly confrned con<strong>fi</strong>ned entities that would not permit a single<br />
piece piece to be removed or added. To avoid confusion, however, these nnmes names should be<br />
used consistently consistently and with a reasonable amount of accuracy.
13<br />
HOW THE GLACIAL GI.,ACIAL THEORY THEORYWAS WAS ACCEPTED ACCEPTED <strong>IN</strong> F<strong>IN</strong>L<strong>AND</strong> F<strong>IN</strong>I.<strong>AND</strong><br />
(according to Rainio 1994, pp. 20-23)<br />
Observations calling for explanation<br />
explanation<br />
In 1740, the Swedish prospector Daniel Daniel Tilas (1712-1772) showed that the source of<br />
erratic boulders resting on a 'wrong' rock in Finland Finland should be searched for in the<br />
north or northwest (Nathorst, 1894, p. 50). In 1821 and 1822, the tLLe Englishman<br />
Strangways Strangways listed localities localities in Finland where the bedrock was a source of boulders<br />
that had migrated to Russia Russia (Strangways, 1821, L82L, pp. 39-30; 1822, p. 10).<br />
Networks of eskers eskers and sandy ice marginal marginal deposits were described from Finland in<br />
the 18th century (Heinricius, 1895; 1895; Argillander, Argillander, 1784). 1784). The landforms landforms were<br />
considered as entities and the the <strong>fi</strong>rst frrst explanations of of their genesis were made in the<br />
early 19th century. In 1819, for 1o" example, elample, Henrik Henrik Deutsch Deutsch concluded that some<br />
eskers were were'products 'products of water' watef (Deutsch, 1819, p. 369) (Rainio & Kukkonen, 1985, 198b,<br />
p. 11).<br />
Striae were known back at the the time time of Tilas; rilas; what what was not not known known was that they<br />
showed parallel orientation within large areas (Sefström, 1837, 1837, p. p. 1). Encouraged by<br />
the example of the Swedish chemist chemist N.G. N.G. Sefström (1787-1845), Finnish Finnish scholars<br />
began began to collect collect information on striae striae in in the the late late 1830s.<br />
Potholes Potholes were studied at around the the same seme time (Nordenskiöld, 1842), and the<br />
contribution of flowing water to their their genesis genesis was was acknowledged. In the late 1830s,<br />
Hofmann Hofmann and Boehtlingk Boehtlingk made observations on the transport of ofboulders boulders in Finland,<br />
and on uplift and ancient shores (Hofmann, 1841, 1841, pp. 119-120 and 124-125; 124-L25;<br />
Boehtlingk, 1839, 1839, 1840a). 1840a).<br />
The frrst <strong>fi</strong>rst universally applicable explanation proposed was was a adeluge. deluge. Next came<br />
rapid, large-scale large-scale movements of the the Earth's Earth's crust, floods floods and parallel movements of<br />
great earth masses masses (Boehtlingk, 1939, p. 4).<br />
Among the the foreign scholars who studied Finland was Strangways (1821, (1821, p. 42). He<br />
deduced the direction ofthe of the flooding waters from the transport directions of erratics<br />
or from the trend of striae striae and eskers. Another was Sefström, a Swede whose rolling<br />
stone, or petridelaunian, flood theory theory had enormous influence in Finland (Sefström, (Sefström,<br />
1837). 1837). According to him, a colossal stream stream had had loosened and transported rolling<br />
stones and sand, erratics erratics and gravel gravel from north north to south. Stones and sand had<br />
polished the the roche moutonn6es. moutonnees. As the the force ofthe of the stream abated, gravel gravel and sand<br />
deposited as long eskers parallel to its flow. (Sefström, 1837; Rainio, 1994, Fig. 4)
L4 14<br />
Obsen'ations Observations of icebergs in polar regions in the late la te 19th century led to the idea<br />
that alien boulders had been transported transported by icebergs (Murchison et al., 1848, 1848, p. 508; 508;<br />
Flint, 1971, pp. 11-12). 11-12). Several students of Finnish geology accepted this<br />
explanation to to lend weight weight to to their their own hypotheses or then then they based their own<br />
ideas on on it (Nordenskiöld, 1863).<br />
Wilhelm Boehtlingk Boehtlingk (1809-1841) studied studied the diluvium of ofFinland Finland in detail in the late<br />
1830s. He made the the important observation that the striae striae are are oriented oriented radially from<br />
the head of the the Gulf of Bothnia and not merely merely from from north to south, as suggested by<br />
Sefström (Boehtlingk, 1840b; 1840b; Rainio & Kukkonen, Kukkonen, 1985, 1985, Fig. 2).<br />
The The absence of sedimentary sedimentary rocks in in Finland and and the the Kola Peninsula and their<br />
occurrence on on the other other side side of of the the Gulf Gulf of of Finland, the signatures signatures of of abrasion<br />
visible on on hard hard granitic rocks and striae striae trending in different directions directions in different<br />
parts of the the country led Boehtlingk to reject the theory theory of adeluge a deluge of short short duration<br />
as inadequate inadequate and propose instead a a long diluvial stage stage with with varying varying flows flows<br />
(Boehtlingk, (Boehtlingk, 1839, p.20 p. 20 and and 1840a, p. 108; 1840b, p. p. 208).<br />
According According to to him, him, the the stage stage began with with the the sudden uplift uplift of Scandinavia, Finland<br />
and the the Kola Kola Peninsula Peninsula followed by by the withdrawal of the huge water water mass that had<br />
inundated these areas. The The latter had caused the the transportation of ofloose loose soil and and old<br />
sedimentary sedimentary rocks rocks to to the the boundary of of the the present crystalline crystalline bedrock area<br />
(Boehtlingk, 1840b, p.207-208). p. 207-208). Mudflows Mudflows streaming streaming in different directions directions from the the<br />
centre centre of of uplift uplift scoured scoured the the roche moutonnees moutonndes and and carved striae on on their their surface<br />
(Boehtlingk, (Boehtlingk, 1839, p. 25 and and 1840a, p. 127; I27; Rainio, Rainio, 1994, Fig. Fig.5). 5).<br />
Glacial Glacial theory<br />
From From its its very very earliest earliest days, the the glacial theory theory as de<strong>fi</strong>ned by Agassiz (1840) in his<br />
"Etudes "Etudes sur sur glaciers" glaciers" was known known in Finland. Finland. Boehtlingk had started to polemize<br />
against against it (Boehtlingk, 1841), but but his untimely death put an end to his his resistance.<br />
At <strong>fi</strong>rst, frrst, other other dissidents either either referred to Sefström and Boehtlingk or elaborated elaborated<br />
their their own concepts while while arguing arguing against the the glacial theory.<br />
The theory theory was still still incomplete incomplete at that that time time and and could could not not explain explain all that that is now<br />
known known about about the the behaviour behaviour of a glacier. The The objections objections to the theory theory thus often<br />
arose from from the the need to point out out these inadequacies.<br />
Scholars just could not understand understand how apparently apparently rigid and brittle ice could have<br />
circumflexed circumflexed rock knobs knobs and carved carved striae striae on their their sides, let alone under under ledges<br />
(Boehtlingk, 1841). 1841). Flowing water had undoubtedly undoubtedly assisted assisted the formation formation of<br />
potholes.
15<br />
Eskers and the ice marginal moraines of Alpine glaciers, alike in appearance but<br />
different in internal structure, were compared with each other as if the glacial<br />
theory had maintained that they had been formed in a similar manner (Rainio,<br />
1994).<br />
It was also diflicult to und understand erstand how an Alpine glacier could have spread to cover<br />
half of Europe and to rise uphill (Rainio, 1994).<br />
Up to the early 1860s, only one student student of Finland clearly defended the glacial<br />
theory; that was Eichwald, Eichwald, an adherent adherent from the very beginning (Söderbaum, 1927;<br />
Eichwald, 1843). At that time, scholars were willing willing enough to accept the theory,<br />
according it equal validity with many others, but they lacked the courage to make<br />
a clear break with the past (Holmberg, 1858; Thoreld, Thoreld, 1863). 1868). Some opinions were<br />
expressed so vaguely that no one could could be quite sure what was actually meant<br />
(Moberg, 1857; Mäklin, 1863). 1863). On on his <strong>fi</strong>eld maps, maps, now held in archives, Thoreld<br />
(1862) was the <strong>fi</strong>rst frrst to refer to till as 'glacierbildning'.<br />
'glacierbildning,.<br />
Adolf Moberg, a professor of physics at the University of Helsinki, studied diluvial<br />
phenomena for a good 15 years and, and and from from 1849, gave several lectures on the<br />
subject to the Finnish Society Society of Sciences and Letters. Letters. At <strong>fi</strong>rst frrst he favoured deluges<br />
as an explanation for his observations, but but he gradually changed his mind.<br />
At a lecture he gave to to the the Society in 1865, Moberg Moberg de<strong>fi</strong>nitely defrnitely came out in favour of<br />
the glacial theory. He stated that the theory was capable of explaining'the explaining 'the northera northern<br />
diluvial and and post-Pliocene formations'most formations' most logically and most naturallyon naturally on the basis<br />
of physical conditions still prevailing (Moberg, 1865). 186b).<br />
Although not often discussed in the Finnish literature, the glacial theory had<br />
obviously sparked considerable considerable debate. The ground ground had been prepared prepared for it, and the<br />
generation which had had staked its honour on the old ideas was passing. After Mobergrs Moberg's<br />
lecture, the old old theories theories were consigned to the past in Finland. (Rainio, 1994, pp. 20-<br />
23)
16<br />
STI'DIES STUDIES ON ON THE SALPAUSSELKAS SALPAUSSELKÄS (IV, S. s. 33-38)<br />
Ttre The Salpausselkäs and and eskers eskers are are understood understood as entities<br />
Long Long before the Salpausselkäs became a subject of geological study they would would<br />
appear to to have aroused people's people's interest interest as formations formations of of an an exceptional exceptional nature. nature. For<br />
gxqrnple example the uppermost Viipuri road seems to have followed followed Salpausselkäs I and 11 II<br />
way back in in the 15th 15th and and 16th 16th centuries centuries (Wallin, 1893, 1893, pp. 59 - 91).<br />
Geographical descriptions started started to talk ofthe of the Salpausselkäs as eskers in the late<br />
18th century. In In his description of the the parish of of Lohja in 1766, 1766, Heinricius showed<br />
that the network ofthe of the western western parts parts of Salpausselkäs I land and 11 II and the associated<br />
eskers were known known all the way to southern southern Ostrobothnia Ostrobothnia (Heinricius, 1895; 1895; Rainio, Rainio,<br />
1985c).<br />
Writing Writing in 1784 in the the Abo Tidningar tidttingar news newspaper paper about about Tuneld's T\:,neld's Geography of<br />
Sweden published published in in 1773, L773, Abraham Abraham ArgiHander Argillander elaborated elaborated on T\rneld's Tuneld's brief<br />
reference to an esker. His His fuH full description of the esker network in southern Finland<br />
includes long long stretches stretches of the the two Salpausselkäs (IV, Fig. Fig. 5) (Rainio, 1985c).<br />
The information given given by Argillander Argiilander and Heinricius Heinricius reveals that the course of the the<br />
Salpausselkäs between Joensuu and Tammisaari Tnmmisaari had already already been been weH well established<br />
established<br />
by the the end end ofthe of the 18th century, century, considering the facilities facilities ofthe of the time. A more detailed<br />
description was to to wait wait for for almost a century. century.<br />
In In the early 19th century, century, the the origin origin of sur<strong>fi</strong>cia:l surfrcidl deposits deposits - eskers eskers and the<br />
Salpausselkäs included included - was explained in terms terms of the the diluvial theories (Rainio &<br />
Kukkonen, Kukkonen, 1985). The The <strong>fi</strong>rst frrst attempt attempt to to assign the the Salpausselkäs Salpausselkäs to their their proper proper<br />
position position in in geology was made made by Wilhelm Wilhelm Boehtlingk Boehtlingk in 1839.<br />
Although Although N N.G. .G. Nordenskiöld Nordenskiöld did did not believe in in the the new glacial theory theory he applied applied it<br />
to Salpausselkä I while while studying studying the the cutting cutting for the the Saimaa Saimaa canal canal in 1846. He<br />
thought thought that the Salpausselkä Salpausselkä "would be a huge ice-marginal ice-marginal moraine moraine provided provided that<br />
the the theory theory of Agassiz holds". holds". However, according to Nordenskiöld, the degree of<br />
sorting sorting of the the sediments in the section section demonstrated demonstrated that this could not be the case. case.<br />
These ideas he expressed in a letter to J.J. J.J. Berzelius Berzelius (Arppe, 1867, 1867, p. p. 34). However,<br />
it was not not until until a quarter of a century century later that that they they were further elaborated elaborated by<br />
Wiik. wiik.<br />
The <strong>fi</strong>rst comprehensive comprehensive description of of the the extensive extensive ice-marginal formation formation of of the<br />
Salpausselkäs Salpausselk,is was was published by Anders Anders Thoreld Thoreld in 1863. He described described a great great<br />
cutting cutting formed when when the waters of Höytiäinen discharged discharged through through the the large large<br />
glaciofluvial delta delta of Jaamankangas Jaa-ankangas in 1859. He considered Jaamankangas Jaamankangas part of<br />
an extensive esker esker network, but was unable unable to decide decide whether whether or not not the ice age had<br />
anything anything to do with it (Thoreld, 1863; Rainio Rainio & & Kukkonen, Kukkonen, 1985, p. 74 and and Fig. 10).
The name Salpausselkä<br />
17 L7<br />
The name Salpausselkä Salpausselkä was introduced introduced at ab about out the same time as the glacial theory<br />
was gaining ground in Finland in the late 1850s. Origina11y, originally, however, it referred to<br />
a certain part ofthe of the water water divide network, network, not to a conspicuous geological geological formation.<br />
Detailed descriptions descriptions of Finland's Finland's water divide ridges and their network are to be<br />
found in geographical papers papers written over two two centuries ago. Until until the mid-19th<br />
century century Maanselkä Maanselkä was the only only name used for long long stretches of these water divides<br />
(in Swedish Swedish Landtryggen, landtryggen, Land-Ryggen, Landrygg, Landrygg, Landtryggen (TuneId, (T\rneld, 1795». 1Zg5)).<br />
Part of the geological Salpausselkäs were included included in that network, albeit still as<br />
nameless units, in the 18th century century (TuneId, (Ttneld, 1795, pp. 260-261; 2G0-26L;Rein, Rein, 1839, 1889, pp. 7-9). Z-g).<br />
By the 1850s it had had become become necessary to distinguish distinguish between the different parts of<br />
the network, a task that was undertaken undertaken by Mr Mr Gylden, Gyld6n, director general general of the<br />
National Board of Survey. Survev.<br />
According to Ramsay Ramsay (1921), the name nnme Salpausselkä salpausselkä <strong>fi</strong>rst appeared in notes for<br />
geography lectures given by Z. Topelius Topelius in 1854-1858. 1854-18b8. As shown by these notes, in<br />
March 1857 Topelius used used the the nomenclature nomenclature of water water divides compiled by Gylden; Gyld6n;<br />
in autumn 1857 he included included the the name nnme Salpausselkä.<br />
Gylden, Gyld6n, then, then, coined both both the name Salpausselkä and the names nrmes of the other parts<br />
of of the water divide network (Ramsay, 1921). The The archive of names kept by the<br />
Research Institute for the Languages of of Finland Finland does not contain a vemacular vernacular<br />
Salpausselkä; Salpausselkä; it is is in fact a scientifrc scienti<strong>fi</strong>c makeshift makeshift (Saara (Saara Welin, oral comm. 15.1.1996).<br />
Thus, Thus, there there was was no no small sm all ridge going going by the the name of salpausselkä, Salpausselkä, which could later<br />
have been been extended extended to cover cover a larger entity. entity.<br />
The The neme name Salpausselkä Salpausselkä <strong>fi</strong>rst appeared in print in the Hallst6n Hallsten geography of 1858 in<br />
the form salpausselänne. Salpausselänne. on On a historical and geographical geographical map published published for<br />
schools schools in the same same year the the name was in in the the form form Salpanselkä (Lillja, (Lillja, 18b8), 1858), by<br />
which was was meant a "southern water water divide, divide, separating separating central Finland Finland from the<br />
south south coast" (den södra skiljovägg, skiljovägg, som afsöndrar afsöndrar det mellersta mellersta landet ifrän ifran den<br />
södra kusten, kusten, Salpan- (rättare Salpa-) selkä) (G.R., 1859) (Saarnisto (Saarnisto et al., 1994,<br />
Fig. 8). It seemed appropriate enough as a name for a water divide because the<br />
ridge ridge was was thought thought to impound the waters of the Finnish lake district. In describing<br />
the Vuoksi watercourse, Ignatius Ignatius (1891), expressed it thus: "The "The water mass, which<br />
<strong>fi</strong>lls <strong>fi</strong>lls all a11 the depressions in in an almost almost horizontal horizontal tenain, terrain, .. meets in the south at<br />
Salpausselkä Salpausselkä a wall that prevents prevents it from from flowing flowing to the Gulf of Finland."<br />
The meaning of Salpausselkä is clear enough on the map of Lillja. In present-day<br />
terms, Salpausselkä Salpausselkä marked the southern boundary of the Eurajoki, Kokemäenjoki,<br />
Kymijoki and and Vuoksi Vuoksi watercourses. In the the west, west, it started south of Rauma, ran<br />
south of Lake Pyhäjärvi in Säkylä, to the areas of Somerniemi and Loppi, and from
18<br />
there via Riihim<strong>fi</strong>, Riihimäki, Oitti and and Järvelä Järvelä to Salpausselkä I I at Sairakkala, Hollola.<br />
From there it followed followed Salpausselkä I to south of Lake Pyhäjärvi in Uukuniemi, and<br />
then continued west of the the village village of Kitee Kitee to Salpausselkä 11 II at about Tolosenmäki,<br />
Tolosenmäki,<br />
Kitee. It It followed followed Salpausselkä 11 II to the church at Kühtelysvaara Kiihtelysvaara and then<br />
meandered to west of the village of Ilomantsi, turning there southwards southwards to<br />
Tolvajärvi and from there there north- northeastwards northeastwards to tojoin join the the Maanselkä Maanselkä water water divide divide<br />
in Russian Karelia. Karelia.<br />
As the name of a a water divide, Salpausselkä was used for the the next frfteen <strong>fi</strong>fteen years,<br />
though spelled in in a variety of ways - Salpanselänne, Salpaselkämä Salpaselkämä and Salpaselkä Salpaselkä<br />
all being seen (G.R. 1859). The form form Salpausselkä was eventually thought up by<br />
Rein (1864, p. 55), who used it to to refer refer to to the water divide divide at Ilomantsi, which which is<br />
outside the present present ice-marginal ice-marginal formation formation of Salpausselkä.<br />
In the early 1840s, the the still anonymous Salpausselkäs were considered to be be<br />
geological formations, formations, as shown by the the studies undertaken undertaken by Boehtlingk (1839) in in<br />
Tartu or or by thoughts expressed expressed by N.G. Nordenskiöld (Arppe, 1867), neither neither of of<br />
whom accepted the the explanation based on the the glacial glacial theory.<br />
Before long, long, geological research needed names for the the "sand eskers" which which had<br />
turned turned out out to to be be ice-marginal ice-marginal features. features. In 1874, Wiik, for the <strong>fi</strong>rst frrst time, time, clearly<br />
linked the the name Salpausselkä to to a geologicallandform geological landform complex. This was a ridge ridge<br />
that was part of a water water divide divide of the the same name. nnme. He also discussed the subject of<br />
eskers, and and from from the the longitudinal longitudinal eskers eskers distinguished distinguished a transversal transversal esker, esker,<br />
Salpausselkä, which which he explained as an ice-marginal ice-marginal deposit. According to him, him, "it<br />
extends as an an arcuate arcuate landform landform from from Lahti Lahti via via Lappeenranta Lappeenranta to Joensuu" (Wiik,<br />
1874, pp. pp. 290-291). He He was was referring referring partly to the the central central arc of the the present present<br />
Salpausselkä I, which which begins at Sairakkala, Sairakkala, Hollola, Hollola, in in the the west, and partly to to the<br />
eastern end of Salpausselkä Salpausselkä 11. II. Wiik Wiik probably probably based his generalization on Hallsten's Hallst6n's<br />
map, on on which which the the water water divide from from Kitee Kitee to Kiihtelysvaara in the Joensuu Joensuu area area is<br />
Salpausselkä Salpausselkä 11. II.<br />
Over the the next 15-20 years there there was no clear clear distinction between the the water divide divide<br />
Salpausselkä and and the end moraine moraine Salpausselkä. Salpausselkä. At the turn of the century, century, the the<br />
geological Salpausselkä emerged emerged as victor with with the the decline decline in importance importance of water water<br />
divides in in geographical geographical and geological descriptions.<br />
To begin begin with, with, the ice-marginal ice-marginal ridge running from Sairakkala, Sairakkala, Hollola, Hollola, via<br />
Hyvinkää, Hyvinkää, Lohja Lohja and Tammisaari Tammisaari to Hanko Hanko was not included included in Salpausselkä Salpausselkä (I),<br />
although, at at least least from 1875, it was considered contemporaneous with it (Wiik 1875, 1875,<br />
p. 233). It went by several several names names in the early years: Lohja-Hanko Iohja-Hanko moraine,<br />
Hankoniemi Hankoniemi ridge or Hankoniemi- Hankoniemi- Hyvinkää esker. esker. Gradually, Gradually, Lohjanselkä Lohjanselkä or<br />
LohjanhaIju Lohjanharju became the accepted "of<strong>fi</strong>cial" "offrcial" names, and the landform landform was variously variously<br />
known known as either an extension extension or part of of Salpausselkä.
19<br />
Before long the concept Salpausselkä was extended to cover the landform complex<br />
all the way to Hankoniemi. By the early 1900s, Salpausselkä salpausselkä was the prevailing<br />
term, although as late as 1921 Ramsay suggested that the name Lohjanselkä should<br />
be revived. Strangely Strangely enough, Lohjanselkä Lohjanselkä was still used in an article in the Otava<br />
encyclopaedia published in 1960.<br />
No speci<strong>fi</strong>c specifrc name has ever ever been proposed proposed for Salpausselkä II. Until the turn of the<br />
century it was known alm almost ost exclusively exclusively as the "parallel ridge". In the early 1890s, 1g90s,<br />
it was sometimes sometimes referred to as the Minor Minor Salpausselkä as if it were somehow<br />
smaller in size. Terms Tems such as "Both parallel parallel ridges of Salpausselkä", salpausselkä", the "Inner "Inner<br />
Salpausselkä" salpausselkä" and, in the early years of this this century, the "Second "second Salpausselkä"<br />
salpausselkä"<br />
came ce-e and went went in the literature. The terms Second and Third Salpausselkäs do not<br />
seem to have gained currency currency until used by Sauramo in 1915. 191b.<br />
Berghell (1904) and Leiviskä (1920) used the term Salpausselkä collectively for<br />
Salpausselkäs I and 11. II.<br />
As late as 1921, Ramsay Ramsay tried to to bring order order to the the nomenclature of the different<br />
parts of ofthe the Salpausselkäs and and to return partly to the old practice, but it was all too<br />
late. The <strong>fi</strong>rst, second and third third Salpausselkäs, initially written in lower case, had<br />
already already found favour with younger younger geologists in in the 1920s. Alongside these, terms<br />
emphasizing geological aspects, aspects, such such as "outer "outer and inner Salpausselkäs" are still in<br />
common use today. The names northern and and southern Salpausselkäs make the odd<br />
appearance but the the Minor Salpausselkä has has practically died out altogether.<br />
As a geological term, the nnme name Salpausselkä Salpausselkä was was a gteat great success from from the very<br />
start. Iftopotkin Kropotkin imported it into Russia in the mid-1870s, mid-1870s, and in 1880,<br />
Salpau-Selkä Salpau-Selkä was was mentioned mentioned in a French French geography geography with a reference to Kropotkin<br />
(Reclus 1880). 1880). The The Swede De Geer used it in his his study of 1885. 188b.<br />
Early stages stages of systematic research into the the Salpausselkäs (IV)<br />
Systematic Systematic studies studies on the the Salpausselkäs started started in in the 1870s, by which time they<br />
could could be based based on on sound sound principles, principles, as the the ice age theory theory had been accepted as a<br />
research research tool. It was was realized how important it was for Finnish geological studies as<br />
a whole whole that the geology of these ice-marginal ice-marginal deposits be established (Sederholm,<br />
(Sederholm,<br />
1889, 1889, p. 29 29 and 40 - 41). 4L). By the end of the century basic information that is still<br />
valid today had been been obtained about their their course.<br />
F.J. Wiik discussed discussed several several basic issues related to the Salpausselkäs in a number of<br />
papers (1871, 1874, 1874, L875,1876, 1875, 1876, 1879). Initially (1871), in accordance with earlier<br />
concepts, concepts, he described described the Salpausselkäs Salpausselkäs as beach ridges. Three years later, after<br />
studying studying the striae, he distinguished Salpausselkä I from other eskers and advanced
20<br />
the the notion, rejected rejected by by Nordenskiöld Nordenskiöld 30 years years earlier, earlier, that that both both Salpausselkä I I<br />
(Wiik, 1874, L874, p. 290) and its its northern northern parallel ridge ridge (Ss II) were were ice-marginal<br />
moraines (op. cit. p. 293 and and Wiik, Wiik, 1875, p. 234). He He state"d stated that that Salpausselkä I I<br />
extended from Lahti Lahti to the Joensuu area (Wiik, 1874, L874,p.291), p. 291), and, and, soon afterwards afterwards<br />
(1875, p. 233), that the Salpausselkä extended from Hankoniemi Hankoniemi to Joensuu. In his his<br />
doctoral thesis, Wiik Wük declared that that Salpausselkä I I was was a distinct distinct ice-marginal<br />
ice-marginal<br />
moraine in in both external extemal and and internal intemal structure stmcture and and in relation to the the striation striation<br />
(Wiik, (Wiik, 1876, p. 89). Wiik's Wiik s other principal theses were that that the the front front of the the ice had<br />
retreated to Salpausselkä I I from from its its earlier, more extensive position (1874, (L874, p. p. 293<br />
and 1876, p. 89), that Salpausselkä I marked the the maximum maximum level of the the Diluvial, Diluvial, or<br />
Late-glacial, Sea (1874, (1874, p. 293 and 1876, 1876, pp. 95 - 96) and that, calculated calculated from land land<br />
uplift, no more than 25 000 years had had elapsed since that that time time (1874, (1874, p. 293).<br />
Around the same time, Solitander (1875) (1875) and Jernström (1876) (1876) were were collecting more<br />
detailed material on Salpausselkä Salpausselkä to support the broad general general delineation delineation ofWiik. of Wiik.<br />
Information Inforrnation ab about out the the course, shape and structure structure of Salpausselkä Salpausselkä and its parallel<br />
ridge accumulated rapidly with with the the start start of geological mapping mapping in in Finland in in 1876.<br />
In 1885, the the Swede De De Geer Geer concluded that the ice-marginal ice-marginal moraines in the Vänern Vänern<br />
and and Vättern Vättern areas areas of of central central Sweden Sweden and and the the Ra Ra moraines moraines in in Norway Norway were<br />
contemporaneous with with Salpausselkä Salpausselkä and and its its parallel ridge, ridge, Salpausselkä II II (De (De<br />
Geer, 1884 - 1885, pp. pp. 436, 438). 438). According According to him, him, they they all mark the position position ofthe of the<br />
front front of the readvanced continental continental glacier glacier (pp. 443, 456). Between them, however,<br />
there there had been the the Baltic Ice Stream, Stream, which which had flowed along the the basin of the Baltic Baltic<br />
Sea far to to the the south. Consequently, the the ice front front could not not have extended over the<br />
Baltic Baltic Sea (pp. 442 - 443). He He also postulated postulated that that the the ice ice front front could not not have<br />
passed passed Maanselkä, the the water water divide divide on the the Finland's Finland's eastern border, but but that the<br />
margin margin of the the continental continental ice ice sheet in in Finland Finland had had trended trended northwards northwards from the<br />
Joensuu area (op. cit. cit. pp. pp. 438,457 and Plate Plate 13).<br />
In 1889, 1889, Sederholm Sederholm proposed that that Salpausselkä Salpausselkä and its its parallel ridges ridges mark<br />
synchronous positions of of the the ice ice front front during during the the retreat retreat of the ice and that in<br />
southwestern southwestem Finland there there are three ofthese of these positions. Unlike De Geer, he thought<br />
it it very very likely likely that that the the end end moraines moraines continued continued on on the the other other side of the the eastern<br />
border. border. He He also also rejected rejected De De Geer's idea idea that that the the Baltic Baltic Ice Ice Stream Stream had been<br />
contemporaneous with with the the deposition deposition of the the ice-marginal ice-marginal moraines moraines of the<br />
Salpausselkäs or Vänern (Sederholm, 1889 and Appendix 1).<br />
Salpausselktis or Vänern (Sederholm, 1889 and Appendix 1).<br />
In 1890, Ramsay studied studied the the course of the the eastern parts of the Salpausselkäs and<br />
their continuations continuations the the ice-marginal ice-marginal moraines ofKoitere of Koitere and Pielisjärvi. He pointed<br />
out that that as the the course of of the the big big ice-marginal ice-marginal moraines in in Norway, Sweden and<br />
Finland had now been established, it was time time to to continue continue the studies in Russian<br />
Karelia. Karelia. (Ramsay, 1891, Appendix Appendix 1)
21 2l<br />
Financed by the Geographical Geographical Society of Finland, Finland, Rosberg followed up Sederholm's<br />
sederholm's<br />
ideas and began to study the continuation continuation of the moraines in Russian Karelia in<br />
1891. He elaborated elaborated on the fmdings frndings of Ramsay concerning the Koitere Koitere and<br />
Pielisjärvi segments, and in 1895 set off on a new expedition to Russian Karelia<br />
(Rosberg, 1892, 1892, 1899XIV Appendix Appendix 1 and the cover).<br />
At the same time the staff stalf of the Geological Geological Commission, the forerunner of the<br />
Geological Survey Suney of Finland, were mapping mapping the course of the moraines in North<br />
Karelia (Frosterus & & Wilkman, Wilkman, 1915). 1915).<br />
Thus, Thus, by by the end of of the the last century, century, Finnish Finnish researchers had had largely established the<br />
course course of the large end moraines, moraines, partly in Russian Karelia, IGrelia, too, mainly mainly by<br />
interpreting landforms, landfoms, i.e. by means means of geomorphology. geomorphology. With Ramsay's and<br />
Rosberg's Rosbergis expedition into Russia, Russia, Finns Finns became the experts in matters related to<br />
deglaciation deglaciation in Russian Karelia.<br />
Continuation of the continental ice ice sheet front front<br />
in North Karelia and Russian Karelia at at the the time time<br />
the Salpausselkäs were formed formed<br />
Opinions opinions differed as to the the relationship between between the Salpausselkäs Salpausselkis and and the<br />
ice-marginal ice-marginal formations formations ofNorth of North Karelia Karelia and Russian Karelia. Karelia. Initially, the Koitere<br />
end moraine moraine was considered contemporaneous with with Salpausselkä I (Ramsay, 1891;<br />
Rosberg, 1892, 1892, 1899, 1899, pp. 44, 44,46). 46).<br />
According According to Rosberg Rosberg (1899, pp. 47,69), 47, 69), the the chain of moraines contemporaneous<br />
with with Salpausselkä Salpausselkä I I continued continued north of Lake Lake Segozero Se go zero (Seesjärvi) (Seesjärvi) via Shalgovaara<br />
to east of Lake Lake Vig (Uikuj:irvi) (Uikujärvi) and from there to the coast of the White Sea (Fig. 3).<br />
Jaamankangas might be a apart part of the "second ice-marginal deposit" i.e. of<br />
Salpausselkä 11. II. Its extensions would then be the ice-marginal ice-marginal formations in<br />
Russian Karelia, which, discontinuously, extend to north of Lake Topozero<br />
(T\roppajärvi) (Tuoppajärvi) (op. cit. pp. 46, 69).<br />
Ramsay Ramsay (1906) suggested that the position of the the ice sheet contemporaneous with<br />
Salpausselkä Salpausselkä I I might be indicated by ice-marginal ice-marginal formations formations that, to modern<br />
thinking, are are rather far south and east. According to him, this zone ran east of Lake<br />
Vig (Uikujarvi) (Uikujärvi) through through Vohtozero (Vuohtselkä), Rigasel'ga (Riihiselkä), Tivdiya<br />
(Tiutia) and and Povenets Povenets to Sumskiy Sumskiy Posad (Suma) (Ramsay, 1906, p. p. 4) (Fig. (Fig. 3). In<br />
that case, the the ice front would would have continued from from Värtsilä directly eastwards.<br />
Sederholm (1911c, p. p. 41; see Atlas Atlas of Finland Finland 1910, Folio Folio 5 III) contended that the<br />
Salpausselkäs "continue "continue over Lake Segozero (Seesjärvi) (Seesjärvi) to Onega Bay (Atinislahti)"<br />
(Äänislahti)"<br />
(Fig. 3). The end moraines found by Rosberg farther west he considered<br />
contemporaneous with the Central Central Finland Finland end moraine, moraine, or or then of of an entirely<br />
different age.
22<br />
In 1920, Leiviskä Leiviska published published comprehensive documentation on on the the Salpausselkäs<br />
that he had had collected in in the the 1910s. His His emphasis was on a geographical geographical description description<br />
and classi<strong>fi</strong>cation.<br />
classilication.<br />
Before long, however, all the the leading scholars had come to to the the conclusion that that the the<br />
Koitere end moraine was indeed contemporaneous with Salpausselkä 11 II and that the the<br />
Pielisjärvi end moraine was was younger younger than than either either (Sederholm, 1899a, b; b; Frosterus Frosterus &<br />
Wilkman, Wilkmarr, 1915; Ramsay, Remsay, 1921; L92L; Sauramo, 1928, p. p. 16). Evidently Rosberg, too, had had<br />
been converted (Suomenmaa VIII, VIII, 1927, pp. 228,326). 228, 326). To begin with Sauramo Sauram o went went<br />
along with this this idea idea (Sauramo, 1929, Fig. Fig. 18, p. 53 53 and and Fig. Fig. 23, 23, p. 65). Leiviskä Leiviskä<br />
(1920), (1920), the geographer, was was the the only one left to maintain that the the eskers eskers extending extenöng<br />
from from Kiihtelysvaara Kühtelysvaara towards Jaamankangas Janmankangas were were extensions of Salpausselkä Salpausselkä 11 II<br />
(Leiviskä 1920, p. 217; 2L7; 1928, L928, p. 59).<br />
As far as Finland was concerned, then, then, the the position position of the continental ice ice sheet sheet front front<br />
during the formation formation of of the the Salpausselkäs seemed to have have been more more or less<br />
established. Salpausselkä Salpausselkä I was the the only only one for which which no no "extensions" had had been been<br />
found northeast of Värtsilä. Once the the Koitere Koitere end moraine was rras no longer longer thought thought to<br />
be the same sarne age age as as Salpausselkä I, clear clear opinions opinions on the the continuation continuation of of the the<br />
continental ice sheet front front from from the the eastern end of Salpausselkä I I ceased to to exist.<br />
Frosterus & Wilkman (1915, (1915, p. 51) and and Leiviskä Leiviskä (1920, pp. 110 110 and and 228) 228) a11 all claimed<br />
that the then known known southern southern part of of the the Tuupovaara Tuupovaara end end moraine moraine was was an<br />
extension of ofSalpausselkä Salpausselkä I, I, but this this was not not very very helpful. helpful.<br />
In the 1930s, new new <strong>fi</strong>ndings <strong>fi</strong>ndings (Hyyppä, 1936; 1936; Sauramo, 1937; Kilpi Kilpi 1937) based on<br />
shoreline displacement studies changed opinions on deglaciation, deglaciation, in in North Karelia<br />
in in particular, to to such an extent that that a conclusive answer still evades scholars.<br />
Interpretation of shoreline shoreline displacement as a dominant dominant factor factor<br />
Contact Contact with with Russian Russian or or Soviet Soviet Karelia Karelia was was severed severed when when Finland Finland became beceme<br />
independent, independent, and and the the USSR USSR was was established. established. From From the the 1920s 1920s Finnish Finnish efforts<br />
concentrated on shoreline shoreline displacement displacement studies and the the application application of of the results results<br />
under the the supervision supervision of of Sauramo and and Hyyppä. Hyyppä. The The position of of the the ice ice front front in in<br />
North Karelia at at the the time time of the the Salpausselkäs were deposited was re-interpreted.<br />
The The ice-marginal ice-marginal deposits deposits in easternmost easternmost Finland Finland and and Soviet Soviet Karelia Karelia were<br />
overlooked, presumably presumably because they they were incompatible with with the the interpreted shore<br />
line line displacements; they they were were not not referred referred to in in the the literature literature or or mentioned mentioned at<br />
university lectures.
23<br />
Hyyppä Hyyppä (1936, p. p.437, 437, app. 7) was the <strong>fi</strong>rst to suggest that the Baltie Baltic lee Ice Lake (B 11) II)<br />
had extended through eastern Finland Finland to Kuusamo. Kuusamo. Thus, at the time the<br />
Salpausselkäs were were formed the iee ice front would have trended northwards from North<br />
Karelia.<br />
His ideas ideas were baeked backed up by the eonclusions conclusions reaehed reached by Sauramo Saura-o (1937, (1gBZ, pp. 17 L7 - 22)<br />
and Kilpi (1937, pp. 111 - 113) from shoreline displaeements displacements studies eondueted conducted in<br />
North Karelia and Kainuu. Sauramo (1937, p. 9) summarized the old and new<br />
eoneepts concepts by stating that: " .. ...in .in eontrast contrast to what what has been eonsidered considered thus far,<br />
Salpausselkä Salpausselkä I does not trend to NE NE towards towards East East Karelia Karelia and Lake Se Segozero go zero<br />
(Seesjärvi) but direetly directly northwards northwards towards Lake Pielinen". Further, "at "at the time of<br />
the Baltie Baltic lee Ice Lake, the iee ice had disappeared from the east of ofthe the Pielinen basin and<br />
during the Yoldia stage from almost almost the the whole basin. basin. Henee, Hence, it was possible that<br />
already during the Salpausselkä stage the Baltie Baltic Sea sea extended from the south<br />
between the eastern water water divide divide and and the iee ice sheet sheet as far far as Maanselkä" and further<br />
still, as pointed out by Kilpi Kilpi (op. eit. cit. p. 17 - 18). 18).<br />
On the basis of of the the interpretation of of shoreline displaeement, displacement, Sauramo Saurams (1937, (1987, p. 9,<br />
1958, pp. 100, 396) 396) maintained "that the the front front of the eontinental continental iee ice in North<br />
Karelia had already already lain lain at at the the morphologieal morphological Seeond Second Salpausselkä at the time of<br />
the First First Salpausselkä. The great great end moraines of southern Finland are united in<br />
North Karelia ". The eontinuous continuous Salpausselkä would would aeeordingly accordingly start in the area of<br />
Kitee-Kesälahti (Sauramo, 1937, 1937, p. 9) 9) or or in in the area of Tohmajärvi-Onkamo<br />
Tohmajärvi-Onka-o<br />
(Sauramo, 1958, 1958, p. 100). 100).<br />
In the following decades deeades Sauramo and Hyyppä and their students refrned re<strong>fi</strong>ned their coneoncepts.eepts. Brenner was was probably the only one who did not respect the the frndings <strong>fi</strong>ndings of Hyyppä and<br />
Sauremo. Sauramo. In his study in which whieh he analysed the the lobate behaviour of the continental eontinental<br />
ice iee sheet, Brenner claimed elaimed that the ice-marginal iee-marginal deposits deposits in Russian Karelia<br />
described deseribed by Rosberg most probably represented these these lobes and and were slightly<br />
younger than than Salpausselkäs I and II. 11. According Aeeording to him, him, the the ice iee front front frrst <strong>fi</strong>rst ran from<br />
Jaamankangas Jaamankangas via Selkäkangas to north ofLake Segozero (Seesjärvi), but later from<br />
Jaamankangas Jaamankangas via Uimaharju UimahaIju to Lake Lake Yushkozero (Jyskyjärvi) and Tuoppajärvi<br />
Lake Topozero (Tuoppajärvi) (Brenner, 1944, pp. 23-25 and Fig. 4, p. 17).<br />
Lake Topozero (Tuoppajärvi) (Brenner, L944, pp. 23-25 and Fig. 4, p. 1-7).<br />
Leiviskä continued eontinued to contend eontend that that at least the the northernmost northernmost fork of Yhdysharju<br />
YhdyshaIju<br />
esker (Connection esker) was part of Salpausselkä II. 11. Jaamankangas was formed<br />
later than the the forks ofYhdysharju ofYhdyshaIju (Connection (Conneetion esker) buried in it (Leiviskä 1951,<br />
pp. pp. 67, 69), but Salpausselkä Salpausselkä II 11 and Jaamankangas had had formed during during the same<br />
marine stage. The difference differenee in elevation was attributed attributed to uplift uplift and disparity of<br />
age (op. cit., eit., pp. pp. 69-70).
24 24<br />
According According to the interpretation interpretation of of Leiviskä, Leiviskä, the the ice front withdrew from<br />
Salpausselkä 11 II earlier in the the west than than in the the east: "At the the time the the great arc arc ofthe of the<br />
Inner Salpausselkä was was forming, forming, ice <strong>fi</strong>lled frlled the the Finnish interior like an enormous<br />
giant cake whose western western margin, margin, from from the the position of of the the end end formations and<br />
judging by the distribution distribution of of clay clay deposits, deposits, had withdrawn to the the line<br />
Hämeenkangas - Pohjankangas, Pohjankangas, while while the the outer margin margin was stationary stationary at the the flank flank<br />
ofthe 6f t[s Inner Tnnsr Salpausselkä" (Leiviskä, 1951, p. 66), 66), that is, to the the level ofthe of the western<br />
part part of the Central Central Finland end moraine.<br />
Repo investigated the cross-striations and dispers dispersal al of ofpebbles pebbles in glacial deposits in in<br />
North Karelia, Karelia, in the the Joensuu area in particular. He suggested suggested that Jaamankangas<br />
was contemporaneous with with the Salpausselkä Salpausselkä 11 II formations at Kiihtelysvaara (Repo,<br />
1957, p. 149; 149; 1960, pp. 11-16), having been deposited deposited as an interlobate interlobate complex in in<br />
a a crevice between between two two glacial lobes. However, However, neither neither then then nor nor later later (Repo 1960;<br />
1969, 1969, see however however pp. 70-71) 70-71) did did he he take take into into account account the the fact, as shown shown by by the the<br />
elevation of Jaamankangas Jaamankangas and and the the associated associated esker plains, that that they they were were formed formed<br />
when the base base level level of erosion was about 30 30 m lower than the the plains of Salpausselkä<br />
Salpausselkä<br />
11.<br />
II.<br />
In In Repo's opinion, opinion, Pöllönvaara, the the northernmost ridge ridge of Yhdysharju Yhdysharju (Connection<br />
esker) esker) between between Kiihtelysvaara Kiihtelysvaara and and Jaamankangas, Jaamankangas, was was the the northern northern end end of<br />
Salpausselkä 11, II, even if precisely at Pöllönvaara it it was was "a perfectly longitudinal<br />
ridge" ridge" (Repo, 1957, L957, pp. 110, 110, 148, 156-158; Rainio Rainio et et al., aI., 1995 [VI], [VIJ, Fig. Fig. 6, VI). His<br />
explanation was that that there had had been dead ice ice on the the distal distal side of the the ice-marginal<br />
formation formation and that that water water had had streamed streamed in in a longitudinal crevasse.<br />
Repo Repo (1957) considered Jaamankangas Jaamankangas and and Uimaharju coeval but but did not discuss the<br />
continuation continuation of the the Salpausselkäs SalpausselkEis from from North Karelia Karelia in in any any direction.
25<br />
CONTlNUATION CONT<strong>IN</strong>UATION OF THE SALPAUSSELKÄS SALPAUSSELI(AS <strong>IN</strong> NORTH<br />
KARELIA I(ARELIA <strong>IN</strong> THE LIGHT LIGIIT OF RECENT RECENT CONCEPTS<br />
CONCEPIS<br />
Biostratigraphieal Biostratigraphical and and morphologie morphological al<br />
interpretations rehabilitated<br />
As a consequence, consequence, the ice-marginal ice-marginal deposits in easternmost Finland and in Soviet<br />
Karelia were were largely ignored ignored until until the the 1960s, when a fresh look was taken at the<br />
concepts of shoreline shoreline displacement displacement (Hyvärinen 1966a, 1966a, b), and studies on the course<br />
of the ice-marginal landforms were reopened reopened using using a geomorphological approach<br />
(Rainio, 1972). 1972). Pollen and and radiocarbon radiocarbon evidence was used to demonstrate presence<br />
of organic organic deposits ofYounger of Younger Dryas Dryas age in the southem southern foreland ofNorth of North Karelian<br />
end end moraines moraines (Selkäkangas) (Selkakangas) whereas whereas at sites farther north north the pollen re record cord opens<br />
with Early Holocene assemblages; assemblages; hence hence the end moraines moraines could be<br />
biostratigraphically correlated correlated with the the Younger Younger Dryas Dryas (Hyvärinen 1971a, Lg7ra, 1972, Lg72,<br />
1973).<br />
In the early 1970s, 1970s, the the Geological Survey of Finland Finland and the geologists of Soviet<br />
Karelia joined forces in studying studying the the deglaciation of the Salpausselkä phases<br />
(Lukashov et al., 1981). As As a result, result, the the work ofRosberg of Rosberg on Russian Karelia becnme became<br />
topical topical on once ce more (see Hyvärinen, 1973).<br />
Position of the iee ice sheet front front during during<br />
the deposition of Salpausselkä Salpausselkä I I<br />
The The chain chain of of ice-marginal ice-marginal ridges included included in Salpausselkä Salpausselkä I comes to an end at the<br />
Patsola Patsola marginal plain plain in Värtsilä, North North Karelia (Berghell, 1904; Ramsay, 1921; Ig2L;<br />
Repo & Tynni, 1967, p. 136; Rainio, 1983 tll). [I]). The terrain to the east and northeast<br />
ofthe plain rises rises and is supra-aquatic. supra-aquatic. As can be inferred from from the orientation ofthe<br />
easternmost eastemmost plains of Salpausselkä I, the front of the continental continental ice sheet could<br />
well weIl have continued continued north-northeastwards north-northeastwards in this area (cf. Rainio 1983 tll, [I], p. G8). 68).<br />
Various ideas ideas about the position of the ice front northeast of Patsola have been put put<br />
forward since the late 1970s without, however, any distinct, continuous end<br />
moraines moraines being found to support support them. them. In the following following these studies are reviewed.<br />
In 1978 1978 and 1980, Rainio suggested that at the time the Salpausselkä I was forming<br />
the front of the continental continental ice sheet continued continued from Patsola Patsola northeastwards northeastwards to<br />
Möhkö and from from there there to Russia. He maintained maintained that the position position of the ice front,<br />
which which he called the Ilomantsi zone, was indicated indicated by the discontinuous chain of<br />
esker deltas, ice-marginal formations and areas of ofhummocky hummocky moraines and that the<br />
Iandforms landforms of ofthe the ice front corresponding to Salpausselkä I were within a lO-km-wide 10-km-wide<br />
zone. In other words, the ice front had had withdrawn withdrawn about 10 km here, whereas<br />
farther west it had remained approximately stationary stationary at Salpausselkä I.
26<br />
In this zone, whieh which is elose close to to the the Russian border, bord er, there there are valleys valleys of the the aneient ancient<br />
Baltie Baltic Sea over a distanee distance of of 10 km kn from from Patsola. Glaeiofluvial Glaciofluvial plains developed in in<br />
them indieating indicating a base level level of of erosion at at 106-112.5 m, m, whieh which is is more or or less the the<br />
same sarne as the 110 m m of the the Patsola plain (Rainio 1991 [IV], [rVj, p. 46). They represent, represent,<br />
then, then, the ineipient incipient Baltie Baltic lee Ice Lake Lake (BI). The The farthest farthest plains are are north north of of Lake Lake<br />
Kaustajärvi, Kaustqjäind, elose close to the the village village of Saarivaara. There, between the the ponds Mellitsan<br />
lampi, Varpalampi Varpalampi and Aittolampi Aittoln-pi at 106-107 m a.s.l., a.s.l., a group of glaeiofluvial glaciofluvial plains plains<br />
has developed at the the 110-112.5-m level.<br />
On the basis of of shoreline shoreline displaeement, displacement, Hyvärinen Hyvärinen (1966b) fIrst frrst eonsidered considered it it<br />
possible that Selkäkangas, one of of the the marginal marginal terraees teraces of of the the Koitere Koiters ehain, shein, was was<br />
eontemporaneous contemporaneous with with Salpausselkä I. I.<br />
Aario Aario & Forsström (1979, (1979, p. 44) dedueed deduced from from glaeiallobe glacial lobe analysis analysis "that "that the train<br />
of marginal marginal deposits, deposits, ineluding including the the Selkäkangas Selkäkangas moraine, moraine, for example, slre*ple, eould could<br />
possibly belong to to the the First Salpausselkä".<br />
Punkari seems to have have started started off offwith with the the idea (1979, p. 25; 1980) that the Koitere<br />
iee-marginal ice-marginal formation formation with with its its Russian eontinuations continuations was eontemporaneous contemporaneous with<br />
Salpausselkä Salpausselkä I. Later (1982, Fig. Fig. 8; 8; 1984, Fig. 4) he apparently apparently ehanged changed his mind,<br />
eonsidering considering it more more likely that the Koitere Koitere end end moraine was was approximately the same<br />
age as as Salpausselkä 11 II and and that that the the iee ice front front probably ran ran from from Tohmajärvi Tohmqjärvi to<br />
Himolanjärvi Himolanjän'i during the the formation formation of Salpausselkä Salpausselkä I. In 1995, Punkari Punkari & Boulton<br />
(1995, Fig. Fig. 6) 6) eventually eventually eoneluded concluded that the Rugozero (Rukajärvi) (Rukajäirvi) iee-marginal<br />
ice-marginal<br />
eomplex complex represents both both Salpausselkä I I and Salpausselkä 11. II.<br />
By By grouping iee-marginal ice-marginal moraines moraines and and esker esker deltas deltas on on small-seale small-scale maps,<br />
Lyytikäinen and Kontturi demonstrated that from Patsola the front front of the iee ice sheet<br />
had run run 10 10 km northeastwards northeastwards before be fore ehanging changing direetion direction at at Korpijärvi Korpijärvi and erossing crossing<br />
the Russian border border (Lyytikäinen, (Lyytiktünen, 1980, 1980, p. 2, Fig. Fig. 1; 1982, p. 80, 80, Fig. 60; Lyytikäinen<br />
& Kontturi, Kontturi, 1980, p. 8, Fig. 6). However, in Fig. 58 59 (p. 1p. 78) Lyytikäinen Lyytikiünen plaeed placed the iee ice<br />
front front somewhat somewhat farther north. north.<br />
Hirvas Hirvas (1980) and Ignatius Ignatius et et al. al. (1980), again on a very very small-seale small-scale map, showed<br />
that the the iee ice front front had had eurved curved gently gently northwards northwards from from Patsola, joining the Koitere<br />
ehain chain somewhat northeast northeast ofKiihtelysvaara. of Kiihtelysvaara. Nenonen eame came to the same eonclusion conclusion<br />
in 1984. Till-stratigraphie Tlll-stratigraphic studies later eonvineed convinced Kujansuu Kujansuu and Nenonen (1987, (1987, pp. pp.<br />
62,63, 62, 63, Fig. Fig. 2, p. 65) that that the the First Salpausselkä and the the Tuupovaara T\rupovaara end moraine<br />
were were eontemporaneous. contemporaneous. Aeeording According to Nenonen (oral eommunieation, communication, 13.12.1995 ), the<br />
Koitere Koitere end moraine moraine is also eontemporaneous contemporaneous with with the the above, as ean can be seen from<br />
his his work work (Nenonen, 1995b, Fig. Fig. 26, p. 58) if interpreted interpreted eorreetly. correctly.<br />
Russian workers workers interpreted the the Rugozero Rugozero iee-marginal ice-marginal formation, a direet direct<br />
eontinuation continuation of the the Koitere Koitere end moraine in in Russian Karelia, Karelia, as a eontemporary contemporary of<br />
Salpausselkä I (Lukashov & Ekman, Ekman, 1982; Ekman Ekman et al., 1981; Ekman & Ilyin,<br />
1991).<br />
1991).
27<br />
According According to the interpretation of Kurimo Kurimo (1982, Fig. Fig. 6), the ice front front ran ran from<br />
Patsola Patsola for about 20 20 km km in the Finnish side before before crossing over into Russia, where<br />
it continued continued to the Segozero (Seesjärvi) area and from from there to south of Lake Vig<br />
(Uikujärvi).<br />
(Uikujänd).<br />
Rainio Rainio (1983, I) contended that that the Tuupovaara Tuupovaara end moraine moraine was slightly younger<br />
than Salpausselkä Salpausselkä 1. I. His concept was was based on on the relationship relationship between the<br />
Tuupovaara T\rupovaara end end moraine and the Patsola marginal marginal plain at the northeastern end of<br />
Salpausselkä 1. I.<br />
Salminen & Hartikainen maintained maintained that the Tuupovaara Tuupovaara end end moraine was<br />
contemporaneous with Salpausselkä I, I, and that that " the sm small all end moraines south of<br />
Selkäkangas Selkäikangas evidently belong belong to to the the Salpausselkä Salpausselkä I stage". stage". (Salminen &<br />
Hartikainen 1985, s. 10) 10)<br />
In In the opinion opinion ofEronen and Vesajoki (1988, p. 321): 321): "It is thus apparent that the<br />
Heinola Heinola deglaciation deglaciation and the following following readvance were were limited to the region occupied<br />
by the the Lake Lake District lobe. lobe. Very Very probaly probaly the the margin margin of the North Karelian lobe was<br />
continuing its retreat at the the same time being being interrupted intermpted only temporarily by short<br />
standstill periods. This This explains explains partly why why there there is no massive end-moraine<br />
complex corresponding to Ss I in the the region of the the North N orth Karelian lobe, lobe, but instead<br />
aseries a series of discontinuous, discontinuous, relatively sm small all end moraines." moraines."<br />
Rainio et al. suggested in 1995 that, that, in in North Karelia, Karelia, the front front of the continental<br />
ice sheet sheet withdrew from from east of ofKitee Kitee during the the Salpausselkä Salpausselkä I I stage:<br />
"On maps (Berghell, 1903; Frosterus, Frosterus, 1920; Leiviskä, Leiviskä, 1920) Salpausselkä Salpausselkä I in North<br />
Karelia is marked marked as a fairly wide ice-marginal ice-marginal formation formation composed of two parallel<br />
arms. They They demonstrate demonstrate that the ice front withdrew in in North North Karelia during the<br />
Salpausselkä Salpausselkä I stage but remained remained stationary farther west. The The Tuupovaara icemarginal<br />
fomation formation ... represents the youngest frontal position position correlative correlative with<br />
Salpausselkä Salpausselkä 1. L ... The orientation of the the T\rupovaara Tuupovaara end moraine suggests that, at<br />
the end of the Salpausselkä I stage, stage, the ice margin margin east of Lake Koitere was was located<br />
at the same level as during the the Salpausselkä 11 II Stage. Stage. Thus the eastern part of the<br />
Koitere Koitere ice-marginal ice-marginal formation and its its extension extension in Russia may represent represent both the<br />
late Salpausselkä land the Salpausselkä 11 stage." (Rainio et al. 1995, VI, s. 185)<br />
late Salpausselkä I and the Salpausselkä II stage." (Rainio et al. 1995, VI, s. 185)<br />
The only reference to end moraines in Finnish territory northeast of Patsola comes<br />
from Rosberg (1899, p. 32, p. 45), who placed an end moraine between Ilomantsi and<br />
Möhkö. He probably meant the the expansion of the Petkeljärvi-Putkela esker south of<br />
Muokonjärvi, Muokonjärvi, which which does indeed display some features typical of an ice-marginal<br />
deposit. deposit. From Liusvaara, now in Russia, Russia, Rosberg mentioned mentioned "two small sm all end<br />
moraines" (op. cit. p. 32).
28 28<br />
According to Berghell (1916), (1916), there there is is a small small "transversal esker" at Kuolismaa (p.<br />
75) and Alasulkulampi (pp. 79-80) and and a "marginal "marginal esker" at Ylimmäisenjärvi (p.<br />
87-88), all now on the Russian side side of of the the border. These are are consistent consistent with with a<br />
discontinuous chain of ice-marginal moraines. According to to Ekman, Ekman, Lukashov Lukashov and<br />
Iljin (personal communication), no ice-marginal ice-marginal deposits deposits that that might serve serve as<br />
extensions of Salpausselkä Salpausselka I are are known known on on the the distal distal side side of the the Rugozero Rugozero<br />
(Rukajärvi) end mo moraine raine in in Russian Karelia. Karelia.<br />
Position of the ice ice sheet front front in North Karelia<br />
during the the deposition deposition of Salpausselkä Salpausselkä 11 II<br />
Current ideas about the position of ofthe the ice front front northeast, northeast, north north and northwest northwest of of<br />
the Kiihtelysvaara-Heinävaara area during during the the formation formation of Salpausselkä Salpausselkä H II are are<br />
very much much the same as those prevailing at at the the turn turn of the century. century. The intervening intenening<br />
years have embraced two two main main interpretations and their their elaborations.<br />
elaborations.<br />
According According to the <strong>fi</strong>rst <strong>fi</strong>rst one, the the Koitere Koitere chain chain of of end end moraines moraines is is approximately<br />
contemporaneous with with Salpausselkä H. II. This This idea idea has has recently recently been seconded by<br />
Hyvärinen Hyvärinen (197la; (1971a; 1973, p. 87-88), Rainio Rainio (1972, (L972, 1985b, 1985b, 1991 1991 [IV] tIVl and and 1995),<br />
Kurimo (1982, p. 66, 66, Fig. Fig. 6, p. 67), 67), Punkari Punkari (1982, 1985) 1985) and and Salminen Salminen & &<br />
Hartikainen Hartikainen (1985, (1985, p. 10-11).<br />
In In the opinion opinion of of Saarnisto Saarnisto (1970, p. 22), 22), shoreline shoreline dis displacement placement shows shows that<br />
Salpausselkä H II started started to to deposit in in the the east during during the the BH BII stage and and that the<br />
continental continental ice sheet sheet withdrew from from Salpausselkä H II earlier earlier in in the the east east than than in in the<br />
west.<br />
Lyytikäinen (1980, (1980, p. 2, Fig. Fig. 2; 2;1982, 1982, pp. 78-79, Fig. 2) and Lyytikäinen & Kontturi<br />
(1980, p. 9) considered that that the the front of ofthe the North Karelia glaciallobe glacial lobe had already<br />
reached reached the the Koitere Koitere chain chain slightly slightly before before the the Salpausselkä Salpausselkä II II stage and had<br />
withdrawn to to the the proximal side ofthe of the chain chain when the the front ofthe of the Lake-District lobe Iobe<br />
was at Salpausselkä Salpausselkä H. II.<br />
On the the basis of of flow flow analysis of of the the ice sheet, Forsström (1984, p. p. 307) suggested<br />
that the the eastern eastern curve of Salpausselkä H-Koitere Il-Koitere end end moraine in in North Karelia "is<br />
slightly slightly younger than than the western part".<br />
Eronen Eronen & Vesajoki Vesajoki (1988, pp. pp.322-323) 322-323) were were of of the the opinion opinion that that the the front front of the<br />
North Karelia Karelia lobe withdrew withdrew to the the Koitere Koitere ice-marginal ice-marginal moraine moraine be before fore the<br />
Lake-District lobe had retreated to the Salpausselkä II zone (see Forsström, 1989).
29<br />
According According to the proponents proponents of the second main interpretation, Salpausselkä Salpausselka II is<br />
contemporaneous contemporaneous with the Pielisjärvi Pielisjärvi chain, chain, and the glaciofluvial deposits and<br />
moraines moraines between Kiihtelysvaara and Paihola, Paihola, the deposits of the Tervasuo complex<br />
and Yhdysharju (Connection esker) esker) all belong to it. A similar idea had been<br />
proposed by Rosberg in 1899. Backed Backed up by more arguments it was also presented<br />
by Repo Repo (1957, (L957, and 1960; Repo & Tynni, T)rnni, 1967, 1967, p. 136), whose opinions were shared<br />
(to start starü with) by Punkari (1979 on the basis of his his ambiguous map) and Hirvas<br />
(1980, Fig. 1), Ignatius et al. (1980, Fig. 11), 11), Nenonen (1984, (1984, 1995b, Fig. Fig.26, 26, p. 58)<br />
and Kujansuu & Nenonen (1987).<br />
Position of the Pielisjärvi end moraine moraine chain<br />
According According to Rainio Rainio (1978, 1985b), the Pielisjärvi Pielisjtirvi ice-marginal formation is a chain<br />
of contemporaneous contemporaneous deposits that that begins at YlämyHy-Honkavaara Ylämylly-Honkavaara at the western westem<br />
end of Jaamankangas, where where a glaciofluvial complex changes into a distinct<br />
ice-marginal formation, and conti continues nu es via via Uimaharju to the Russian border.<br />
Divers opinions opinions have been expressed expressed on the the relation relation of the Pielisjärvi ice-marginal<br />
formation, or or more often its its southwestern southwestern end, end, Jaamankangas, Jaemankangas, to Salpausselkä salpausselkä 11. II.<br />
The key issue has been been how to to interpret interpret the Tervasuo complex (Rainio, 1990, pp.<br />
35-38), Yhdysharju (Connection esker) esker) between Heinävaara Heinävaara and Jaamankangas<br />
(Frosterus & Wilkman, 1915, p. 55) 55) and and the the associated deposits, as well weH as the<br />
movements of the continental continental ice sheet.<br />
In Saurnmo's Sauramo's clay elay chronology (1928, p. 16, Table VIII), the front of the continental<br />
ice sheet sheet was at the Jaamankangas- Jaamankangas- Uimaharju line line in years 100-200 (Fig. (Fig. 6, p. 26<br />
and and Table VII). South South of Jaamankangas, Jaamankangas, the the ice front lay west of ofPyhäselkä Pyhäselkä in year<br />
100 100 and west of Orivesi Orivesi in year 200.<br />
Sauramo Sauramo (1928, p. p. 16), among others, considered Jaamankangas contemporaneous<br />
with Salpausselkä Salpausselkä III, in southwestern southwestern Finland. According to him (19b8, (1958, p. 894), 394), the<br />
Jaamankangas end moraine is part of Salpausselkä Salpausselkä III 111 (".. (" .. die Endmoräine Endmoräne<br />
Jaamankangas Jaamankangas zu dem 3. Salpausselkä Salpausselkä gehört"). gehört"). He also suggested (on (on the basis of<br />
a super<strong>fi</strong>cial super<strong>fi</strong>cial striation interpretation) that Janmankangas Jaamankangas had formed at the front of<br />
a readvanced ice sheet ("Dabei war sicherlich ein Vorrücken des Eisrandes<br />
eingetreten.") eingetreten.") (op. cit. p. 397).<br />
According According to Saarnisto Saarnisto ( (1970, 1970, pp. pp. 24, 77), the elevation of the Jaamankangas J aamankangas plains<br />
is close elose to that ofthe of the Yoldia Yoldia Sea and so they they are younger than than Salpausselkä II. 11.
30<br />
Rainio (1972) (L972) proposed that Jaamankangas Jaamankangas and the the chain chain of ice-marginal ice-marginal deposits<br />
extending from from Uimaharju to the Russian border border were were of the same age and younger younger<br />
than than Salpausselkä Salpausselkä II. In his licentiate thesis, Rainio Rainio (1973) demonstrated that there there<br />
is a discontinuous chain chain of of end moraines between Jaamankangas Jaamankangas and and Uimaharju,<br />
and and that that Jaamankangas Jasmankangas and and the the contemporaneous marginal plains plains were were formed<br />
elose close to to the the level level of the the Y Yoldia oldia Sea.<br />
Initially, Initially, Aario Aario & Forsström (1978, (1978, p. p.521, 52; 1979, L979, p. 43) 43) supported supported the the interpretation<br />
ofRepo. of Repo. But they also proposed (Aario & Forsström, Forsström , 1979, L9'79 , p. 44) that the the Pielisjärvi<br />
end moraine "together "together with the Jaamankangas Jaamankangas complex would be be the the one one correlative<br />
with with the Second Salpausselkä". Salpausselkä". Later, Later, on on the the basis basis of of esker analysis, analysis, Forsström Forsström<br />
(1984, (1984, p. 307) suggested suggested that Jaamankangas Jaamankangas was younger than than Salpausselkä II ("it<br />
would seem more more probable that the the eastern parts of Ss II formed diachronously and<br />
gained gained their <strong>fi</strong>nal <strong>fi</strong>nal shape only only at the the stage when ice movement in in the the Lake-Finland<br />
Lake-Finland<br />
lobe in in the the direction direction indicated by the striae had already come to an end and the the ice<br />
margin margin had begun to retreat northwestwards towards towards Jaamankangas.")<br />
After After analysing the the movements of the the continental continental ice sheet, sheet, Hirvas Hirvas (1980) came to<br />
the the same same conelusion conclusion as Repo. Repo. As mentioned mentioned above in in the the discussion discussion on on the the<br />
continuation of the the ice ice front during during the formation formation of Salpausselkä II, Hirvas' Hirvas'opinion opinion<br />
was was shared by by Punkari Punkari (1979, 1980), Ignatius Ignatius et et al. al. (1980), Nenonen (1984) and<br />
Kujansuu Kujansuu & Nenonen (1987).<br />
Lyytikäinen & Kontturi (1980, (1980, pp. 9-10) 9-10) and Lyytikäinen (1982, (1982, pp. pp.78-79, 78-79, Fig. Fig. 59)<br />
contended that that Jaamankangas Jaamankangas started to form form at at the the same time time as Salpausselkä Salpausselkä II II<br />
and and continued continued to to deposit deposit after after it. As As they they put it: "Through gradual deposition,<br />
Jaamankangas Jaamankangas is thus thus connected connected to to the the northern northern part of of Salpausselkä Salpausselkä II."<br />
EIsewhere Elsewhere the the Pielisjärvi end end moraine had already deposited when Jaamankangas<br />
was still still building up up (Lyytikäinen, (Lyytikänen, 1982, pp. pp.78-79, 78-79, Fig. Fig. 59).<br />
According According to to the the lobe analysis analysis of of Salminen Salminen & Hartikainen Hartikainen (1985, pp. 11-12), L1-12), the<br />
North North Karelia glaciallobe glacial lobe <strong>fi</strong>rst frrst withdrew withdrew in in such a manner manner that that the Lake Lake District<br />
lobe could occupy the the Höytiäinen Höytiäinen basin for for some time. time. With With the the departure departure of that<br />
lobe, the the North North Karelia lobe readvanced to to the the Pielisjärvi Pielisj:irvi ice-marginal ice-marginal formation,<br />
generating a chain of ice-marginallandforms ice-marginal landforms with with different components. Eronen &<br />
Vesajoki Vesajoki (1988, p. p. 324) supported supported the the concept of Salminen and Hartikainen.<br />
In the opinion opinion ofEronen and and Vesajoki (1988, (1988, p. p. 320): "The slope ofthe delta surface<br />
(of (ofJaamankangas) Jaamankangas) in a distal distal direction direction from from about 120 120 m to 105 m above sea level,<br />
along with the relatively rough topography, indicates that that a lowering lowering in water level<br />
took place during deposition of the the glaciofluvial sediments."
31<br />
Over over the years it has been deduced that the Pielisjärvi Pielisjärvi chain, or parts of it, was<br />
either contemporaneous with Salpausselkä II (Ramsay (at <strong>fi</strong>rst), frrst), 1891, p. 7; Z; Rosberg,<br />
1892, p. 123, 1899, pp. 46, 68; Repo, 1957; Ignatius Ignatius et al. al., , 1980; Hirvas, 1980; 19g0;<br />
Kujansuu Kujaneuu & Nenonen, 1987; Nenonen, 1984, 1995b) 1gg5b) or younger than it (Ramsay,<br />
1921; Sederholm 1899a, b, 1911a, p. 11; Frosterus Frosterus & Wilkman 1915; l91b; Sauramo Saurnmo<br />
1928a, p. 16; Rainio 1972, L972,1985b, 1985b, 1991 [IV], 1995; Hyvärinen Hyvärinen 1973; 1978; Punkari 1982,<br />
1985; Kurimo 1982, 1982, p. 66, <strong>fi</strong>g. frg. 6, p. 67; Salminen Salminen & Hartikainen Harüikainen 1985, 1g85, p. 10-11;<br />
Eronen & Vesajoki 1988). 1988). Opinions Opinions have been based on the position position of ofparts parts of ofthe the<br />
ice-marginal formation in relation to other other ice-marginal ice-marginal formations, fomations, on shoreline<br />
displacement displacement and on the interpretation interaretation of elast clast transport, striation and other fabric<br />
elements.<br />
Nenonen (1993, pp. 49-50, 1995b, pp. 79-80) considered it possible possible that the<br />
Pielisjärvi end moraine and and Salpausselkä Salpausselka III in southwestem southwestern Finland might be<br />
approximately contemporaneous with with the the Central Central Finland Finland end moraine.<br />
Eronen and Vesajoki (1988, p. 318, 318, Fig. Fig. 1) have have published published aseries a series of maps<br />
illustrating different concepts of the the position position of of the the front front of the ice sheet in in North<br />
Karelia during the formation of the Salpausselkäs.<br />
If Ifthe the action action of ofglacial glaciallobes lobes is taken taken into into account the interpretation of ofdeglaciation<br />
deglaciation<br />
by by many many researchers (e.g. Salminen Salminen & Hartikainen, 1985; Eronen & Vesajoki, 1988) 1g88)<br />
becomes too complicated complicated to be reviewed here.
s2 32<br />
SALPAUSSEI.J(A SALPAUSSELKÄ I AI{D <strong>AND</strong> TIIE THE CENTRÄL <strong>CENTRAL</strong> F<strong>IN</strong>I.<strong>AND</strong> F<strong>IN</strong>L<strong>AND</strong> END END MORA<strong>IN</strong>E,<br />
RECESSIONAL OR TERM<strong>IN</strong>AL? (modifred (modi<strong>fi</strong>ed from Rainio Rainio 1991, 1991, IV, IV, pp. 30-33) 30-33)<br />
The discussion about ab out whether whether Ss I was recessional or had had formed in front front of the the<br />
readvancing continental ice sheet was opened by De De Geer (1885). Sederholm (1911b)<br />
approached the Central Finland end end moraine moraine from the same angle. For many many years<br />
the view that the formations were recessional was favoured. More More recently, recently, however, however,<br />
evidence has accumulated to show that they are are end end moraines moraines fomed formed in front of ofthe the<br />
readvancing ice sheet and that that glaciation glaciation in southern southern Finland and the the stratigraphy<br />
of ofthe the glacigenic deposits are are more complicated than had had earlier earlier been been suspected suspected (e.g.<br />
Okko, 1962; Hyyppä, Hyyppä, 1966; Fogelberg, 1970, pp. pp.25,62, 25, 62, 65-66; Aartolahti, Aartolahti, 1972, L972,pp. pp.<br />
11,77; LL,77; Hirvas & Nenonen, 1980, 1985, 1987; Nenonen, 1984; Rainio, Rainio, 1984a; Rainio, Rainio,<br />
1985a, 11; II; Rainio et al., al., 1986, III; Nenonen, 1995b).<br />
Okko (1962) proposed that that the period during during which which the ice sheet retreated retreated from<br />
Finlands Finland's southern coastal area to somewhere north north of Ss I I should should be called the<br />
Heinola deglaciation. The following following advance advance to Ss I I should accordingly accordingly be referred referred<br />
to as the Salpausselkä readvance. Rainio Rainio (1984a, 1985a, 11) II) suggested that during<br />
the Heinola Heinola deglaciation deglaciation the the ice sheet sheet had had receded for at least 80 km on the the<br />
proximal side of the the present present Ss I. I. (cf. Hirvas Hirvas & & Nenonen, 1987, pp. 53, 53,62; 62; Eronen<br />
& Vesajoki, 1988, p. 321; 321; Nenonen 1995b, s. 79) 79)<br />
Mainly in in the light light of his his interpretations of striations, striations, Sauramo (1958, pp. 99-100,<br />
396) suggested suggested that that the the ice sheet sheet in North Karelia had withdrawn to the<br />
Outokumpu area at at the the end end of the Alleröd Alleröd interval. From From there it had had readvanced<br />
in the early early Younger Younger Dryas Dryas stage to the the Salpausselkä zone, i.e. to the present present<br />
Salpausselkä 11, II, which, which, according according to Sauramo Sauramo (1937, 1958), represents both<br />
Salpausselkä land I and Salpausselkä Salpausselkä 11. II.<br />
The following following facts support the the concept of a readvance of the the ice in the the zone of the<br />
Salpausselkäs and the the Central Central Finland end moraine:<br />
1. Till-covered <strong>fi</strong>ll-covered glacigenic deposits deposits occur all over over Finland. In the south south ofthe of the country, country,<br />
a considerable proportion proportion ofthem are concentrated in certain certain zones. One such zone,<br />
50 - 80 km wide, is on the the proximal side of of Ss I and another, another, at least least 50 km wide,<br />
is on the the proximal side of the Central Central Finland ice-marginal ice-marginal formation. formation. There There are<br />
sites where clays and and glaciofluvial deposits deposits are overlain overlain by till or where there there are<br />
several superimposed discordant discordant till beds. The chain chain of ofglaciofluvial glaciofluvial deposits deposits is discontinuouscontinuous<br />
in both both ice-marginal ice-marginal formation formation areas areas and the eskers eskers do not extend extend<br />
through through them. them. The base level of erosion at the time the till-covered till-covered glaciofluvial<br />
deposits deposits formed formed was was higher than that at the end of deglaciation. This is clearly clearly<br />
visible visible in the zone of of the Central Central Finland end moraine, where the difference difference in base<br />
levels levels is up to 50 m. The till-covered till-covered deposits deposits are often deformed.
33<br />
2. The striae on either side of the ice-marginal ice-marginal formations differ in direction. Some<br />
striae terminate abruptly at the marginal marginal formation. fomation.<br />
3. The uppermost uppemost till in the Salpausselkä Salpausselkä zone is often immature, immature, making it easy to<br />
identify the parent sediments. sediments.<br />
From the position of the eskers at Ilomantsi, llomantsi, Eronen Eronen and Vesajoki Vesqjoki (1988, p. 321)<br />
argued "that the Heinola Heinola deglaciation deglaciation and the following following readvance were limited to<br />
the region region occupied occupied by the Lake Lake District District lobe". Punkari Punkari & Boulton (1995) disagreed<br />
with the whole idea of a major major oscillation. oscillation.<br />
Kujansuu & Nenonen (1987, Fig. 4, p. 64), Hirvas Hirvas & Nenonen (1987, (1982, p. 62) and<br />
Nenonen Nenonen (1995a, Fig. 15, p. p.24,p.27)have 24, p. 27) have all published published observations oftill-covered<br />
of till-covered<br />
glacial deposits that they have interpreted interpreted as representing representing the Salpausselkä<br />
readvance. Referring to the the work of ofEronen Eronen and Vesajoki vesajoki (1988), (1988), Nenonen (1995b, (lgg5b,<br />
p. 60) wrote that: "The till stratigraphy and the relations relations of o<strong>fi</strong>ce ice flow stages show and<br />
directions directions to the ice-marginal ice-margindl formations formations imply that that the ice sheet readvanced a fair<br />
distance distance m rn North Karelia, Karelia. too".<br />
The Central Finland end moraine has has been been considered as either either recessional<br />
(Sauramo, 1929; Repo, 1964) or or as having having formed formed in front of a glacier glacier that had<br />
oscillated less than 10 km (Sederholm, 1911b, p. 69; Virkkala, 1959, pp. 52-53; b2-b3;<br />
Aartolahti, 1972, pp. pp.59-66, 59-66, 78; Kujansuu, 1995). 19g5). The conceptions of "oscillation"<br />
"oscillation"<br />
were based based mainly on observations, made in in the proximal part part of the end moraine,<br />
of of some some submorainic submorainic glacial deposits. It has also been been suggested that the formation<br />
was formed diachronologically diachronologically (Saurn- (Sauramo o 1924, p. 65), or was deposited partly in a<br />
crevasse crevasse of of the ice ice sheet (Repo 1964, p. 150), in in a fairly large glacial bay (Saur"-o (Sauramo<br />
1928, p. 26,29;Ristaniemi 26, 29; Ristaniemi 1985, p.8 p. 8 andAppendixll, and Appendix H, 1982, 1987, <strong>fi</strong>g. 81, 31, p.43, p. 43, enclosure<br />
map II) or between glacier lobes (PunkaÄ, (Punkari, 1982, p. 75; 75; see Kujansuu, Kujansuu, 199b). 1995).<br />
According According to Ristaniemi Ristaniemi (1987, p. 88): "observations "Observations of the highest shoreline do not<br />
attest to the Keuruu deglaciation." This opinion he arrived at by analysing<br />
movements of the ice sheet and the late-glacial base level of erosion, and<br />
interpreting varved clays on the the distal distal side of the the ice-marginal ice-marginal formation.<br />
Further Further information information on till-covered till-covered sediments, sediments, striations and the orientation of<br />
eskers eskers was obtained from gravel assessments, mapping mapping of Quaternary Quatemary deposits;<br />
geological mapping and special investigations investigations undertaken by the Geological Sun'ey Survey<br />
of Finland. These These showed that glacial features in the Central Finland end moraine<br />
and its proximal zone were similar to those in Salpausselkä I and its proximal proximal area,<br />
that is, those mentioned on pages 32 -33.<br />
that is, those mentioned on pages 32 -33.
34 34<br />
In the the light light of the above, Rainio Rainio & Lahermo Lahermo (1985) and Rainio et al. aL (1986, III)<br />
concluded conc1uded that the ice sheet receded from Ss I I to at least least 50 km km north north of what is<br />
now the Central Finland end moraine moraine without any signifrcant signi<strong>fi</strong>cant advances advances interrupting<br />
deglaciation. The The ice then readvanced to to where the formation formation now stands. Rainio et<br />
al. (III) proposed that the stages be termed the Keuruu deglaciation and the<br />
Jyväskyla Jyväskylä readvance (Rainio, 1991, IV, Fig. 4). (cf. Hirvas & Nenonen, Nenonen, 1987, pp. 53,<br />
62)<br />
Nenonen has published published a agraphie graphic diagram of ofthe the relationship relationship between end end moraines moraines<br />
and the stratigraphy caused by readvances ofthe ice ice in southern southern Finland (Nenonen,<br />
1992, L992, Fig. Fig. 2). 2).<br />
MATERIAL <strong>AND</strong> AT.ID METHODS METHODS OF OF TIDS THIS STUDY<br />
Mapping of deposits deposits in in North Karelia (I, IV, fV, VI)<br />
Owing to the lack lack of of accurate maps and aerial aerial photos, photos, the the investigations investigations in in North<br />
Karelia were conducted on foot to to begin with. Routes Routes were planned planned by studying old<br />
maps and picking out out points that that seemed to to have relevance for the the investigation.<br />
investigation.<br />
Later, use was made of aerial photo interpretations, interpretations, which were then then checked in the<br />
<strong>fi</strong>eld. <strong>fi</strong>eld.<br />
The basic basic maps at at 1:20 000 scale introduced introduced in in the mid-1970s made interpretation<br />
more accurate. Most Most of the the elevation elevation values were obtained from these these maps.<br />
It was was not not long long before the the <strong>fi</strong>eld freld observations demonstrated the existence of two<br />
continuous chains of ice-marginal ice-marginal ridges in North North Karelia. The <strong>fi</strong>rst extends from<br />
Kiihtelysvaara, Kiihtelysvaara, from the the known known - albeit albeit not gene generally rally accepted - eastern eastern end end of<br />
Salpausselkä, Salpausselkä, and the the second from Uimaharju into Russia. Moreover, Moreover, there there is also<br />
a fairly fairly continuous continuous chain chain of ice-marginal ice-marginal deposits deposits between Jaamankangas Jaamankangas and<br />
Uimaharju. Uimaharju. As it turned turned out, these landforms landforms had had already been largely largely described by<br />
Sederholm (1899a, b; Ramsay Ramsay (1891) and and Rosberg (1892, 1899) a hundred hundred or so<br />
years ago.<br />
Later, Later, two more more important ice-marginal ice-marginal chains were found between the two longest longest<br />
chains, chains, of which the Tuupovaara T\upovaara end end moraine moraine deposited towards towards the end end of of the<br />
Salpausselkä I stage.
35 s5<br />
Results frorn from North Karelia and the narning naming of<br />
geornorphological geomorphological units (I, IV, fV, VI)<br />
Rainio published preliminary <strong>fi</strong>ndings frndings on the position oftwo of two continuous end moraine<br />
chains in 1972. L972. His licentiate thesis thesis in 1973 19?B dealt with the area between<br />
Jaamankangas and and Uimaharju. uimaharju. In 1978 19?8 and 1980, 1g80, he published published his observations on<br />
deglaciation and and end moraines in North Karelia Karelia in excursion guides, and in 1983 l98B the<br />
results of a detailed detailed investigation of the Tuupovaara T\rupovaara end moraine, which is part I of<br />
this doctoral thesis. Two T\vo years later he collected the names he had proposed for the<br />
ice-marginal formations foruations in 1978, 1980 and 1983 1g8B :ind and published them together with<br />
a map depicting their position (Rainio, 1985b). 1g8bb). In 1991, 19g1, he wrote a general<br />
description of deglaciation deglaciation and the position position of of end moraine moraine ridges in North Karelia<br />
for the excursion guide of the IGCP-253 IGCP-25B programme. programme. The description, which<br />
incorporates his earlier suppositions, suppositions, examples examples of various various landforms and new<br />
<strong>fi</strong>ndings frndings and conclusions, constitutes constitutes part IV of this thesis. Part VI is also closely<br />
related to the investigations investigations in North Karelia; Karelia; more about it on page 00.<br />
Stu Studies dies elsewhere in southern southern Finland Finland (11, (II, 111, III, V, VI) VI)<br />
Aß As a result of ofthe the sand and and gravel assessments assessments undertaken by the GSF in 1969-72 Lg6g-72<br />
and the subsequent subsequent mapping of of Quaternary deposits, the research area beca-e became<br />
larger than originally intended, eventually including including the structure structure of the<br />
Salpausselkäs Salpausselkäs and Central Finland Finland end end moraine moraine and the stratigraphy of their<br />
proximal zones. Observations made made on cuttings and striations in these zones<br />
suggested that the the late-glacial late-glacial stratigraphy of southern Finland wEß was more complex<br />
than had generally been been believed a couple ofdecades of decades earlier. It turned out that the<br />
ideas about the "non-uniformity" of deglaciation put forward decades ago aga might be<br />
worth reconsidering. reconsidering. Thus it was that the last deglaciation in southern and central<br />
Finland and and the the position of the major major end moraines - - the salpausselkäs Salpausselkäs and the<br />
Central Finland end end moraine - were included in in the research.<br />
In the light of material mainly collected in the course of the assessment of sand and<br />
gravel resources in Mikkeli province province and and mapping mapping of Quaternary deposits in the<br />
Mikkeli, Vuohijärvi, Vuohijärvi, Lappeenranta, Savitaipale, Savitaipale, Kouvola, Kouvola, Heinola, Sysmä and<br />
Luumäki map-sheet map-sheet areas, a paper was was published published vindicating M. M. Okko, who, in<br />
1962, 1962, had suggested suggested that a substantial substantial oscillation of the Weichselian ice sheet had<br />
preceded the formation of Salpausselkä Salpausselkä I. 1. That paper forms part part II of the present<br />
thesis.
36<br />
Rainio and Lahemo Lahermo together studied studied the Central Finland end moraine moraine and and its<br />
proximal proximal zone. Additional observations were made during the assessment assessment of sand<br />
and gravel gravel resources resourees in Central Finland Finland province provinee and mapping in the Jyvtiskyla, Jyväskylä,<br />
Jämsä and Korpilahti map-sheet areas . They published published their frndings <strong>fi</strong>ndings in 1976, 1976, 1985 1985<br />
and 1986. In partnership partnership with with A. Kejonen Kejonen and S. Kielosto Kielosto they published a paper on<br />
deglaciation deglaeiation and oscillation oseillation in the proximal proximal area of the Central Finland end end noraine moraine<br />
in 1986; it is part III ofthe of the present thesis.<br />
In conjunction eonjunetion with mapping of ofQuaternary Quaternary deposits of ofthe tJre Lappeenranta Lappeenranta map-sheet map-sheet<br />
area, the lithostratigraphy of bottom deposits was studied studied in an open open pit belonging belonging<br />
to Partek Oy at Ihalainen to see whether the signature of the Heinola<br />
deglaciation-salpausselkä deglaeiation-Salpausselkä readvance readvanee was recorded reeorded in them. The The results results of ofthis this study<br />
constitute eonstitute part V of the thesis.<br />
Part VI, VI, compiled eompiled together with Matti Saarnisto Saarnisto and Ilpo Ekman, Ekman, is is the frnal <strong>fi</strong>nal report<br />
of the IGCP 253 project projeet dealing with Finland, Russian Karelia and Kola. It looks looks<br />
briefly at at the mutual mutual relations, relations, size, location loeation and and position position of the Younger Dryas Dryas<br />
iee-marginal ice-marginal formations formations and discusses diseusses their their relation to the Baltie Baltic Ice lee Lake Lake and and the the<br />
Yoldia Y oldia Sea. Diserepaneies Discrepancies in the opinions opinions of Finnish and Russian Russian geologists<br />
concerrring eoneerning the age and relations relations of the end end moraines in North N orth Karelia and Russian<br />
Karelia are highlighted (Rainio et al., al., 1995, VI).
RESULTS<br />
37<br />
I<br />
Rainio, H. 1983. The Tuupovaara Tuupovaara end mOrlune moraine 10 in North Karelia,<br />
Eastern Eastem Finland - an ice marginal marginal formation fomation of the same age as the<br />
Salpausselkä Salpausselkä ridges. Bulletin of the Geological Society of Finland 55,<br />
67-76.<br />
This report describes describes a previously previously largely unknown unknown end moraine in the province of<br />
North Karelia. The landform, which extends extends from Värtsilä värtsilä to Ilomantsi via<br />
Tohmajärvi and and Tuupovaara, r\rupovaara, is given the name Tuupovaara T\upovaara End Moraine. Including<br />
a few short short gaps, it is 50 km long, trends N-S and SSW-NNE ssw-NNE and runs at distances<br />
of 12 to 22 22fu' km from the distal distal flank of Salpausselkä 11. II. Striae indicate that the last<br />
movement ofthe of the ice ice was perpendicular to the end moraine. To the southeast ofLake of Lake<br />
Loitimo the striae extend for some 4 km to the the western western margin margin of the esker of<br />
Otmen. otmen. The parts formed in the Baltic Baltic lce Ice Lake Lake and the Loitimo, a glacial lake,<br />
consist mainly of glaciofluvial material, whereas whereas the supra-aquatic parts are<br />
composed composed largely of till till and are much smaller smaller than the glaciofluvial glaciofluvial parts.<br />
The Tuupovaara End Moraine Moraine begins begins at Pykälävaara, PykäLlävaara,4 4 km north ofthe of the easternmost<br />
part parü of Salpausselkä Salpausselkä I, - the the Patsola marginal marginal delta. Pykälävaara lies 4-6 km Lm behind<br />
the line of of the glacier margin represented by the plateaus of Salpausselkä I. The<br />
trends of of the striae also indicate that that the delta delta plain of Pykälävaara is is slightly<br />
younger than that at Patsola. Patsola.<br />
The Tuupovaara Moraine is thus slightly younger than salpausselkä Salpausselkä I, but<br />
distinctly older older than Salpausselkä 11, II, indicating that the margin of the Weichselian<br />
ice sheet did not extend extend from Värtsilä to the ice-marginal deposition zone between<br />
Kiihtelysvaara and selkäkangas, Selkäkangas, and that the ice ice receded more rapidly in the<br />
Ilomantsi area than farther west during the the deposition deposition of Salpausselka Salpausselkä I.<br />
The esker complex complex of _otmen, Otmen, which which is located about 2-b 2-5 km to the east of the<br />
Tuupovaara Tuupovaara End Moraine, Moraine, lies at the boundary boundary between two different sets of<br />
striations. From the evidence presented presented by by the the location location and structural features of<br />
the complex, complex, it must be identifred identi<strong>fi</strong>ed as an interlobate interlobate complex.<br />
TVenty-seven Twenty-seven stone stone counts indicate that the material was transported from between<br />
the west and and northwest. Local rocks become predominant after a transport distance<br />
of a few kilometres. kilometres.
38<br />
11 II Rainio, H. H. 1985. 1985. Första Salpausselkä Salpausselkä utgör utgör randzonen randzonen for für en landis landis<br />
som avancerat pä nytt. Summary: The The First Salpausselkä is is a marginal marginal<br />
formation of the outermost margin margin of a readvanced readvanced ice sheet. sheet. Geologi<br />
37 (4-5), 70-77.<br />
Most of the material for for this paper was was coHected collected in the the course course of of a special<br />
investigation of end end moraines moraines in in North Karelia, Karelia, the the assessment of gravel resources resources<br />
in in the the western part of of Mikkeli Mikkeli province and and Quaternary mapping of of Quaternary<br />
deposits in the map sheet areas of Lappeenranta (3134), Mikkeli Mikkeli (3142), Luumäki<br />
(3131), Savitaipale (3132), (3132), Vuohijärvi (3114) and Sysmä (3121).<br />
The The debate over whether whether Salpausselkä Salpausselkä I formed during during a a temporary temporar5r halt of of a<br />
withdrawing ice front or at the front front of readvanced ice was was opened in in Finland and and<br />
Sweden a century ago. Salpausselkä Salpausselkä I I has has usually usually been been considered considered a recessional<br />
recessional<br />
deposit, although although several several researchers researchers have have not excluded excluded the the possibility of a<br />
readvance. Marjatta Marjatta Okko Okko became the the chief chief advocate advocate of readvance readvance when, in 1962,<br />
she introduced the concepts Heinola Heinola deglaciation deglnciation and Salpausselkä readvance.<br />
readuance.<br />
In this paper paper new evidence is is presented that that the the deposition deposition of Salpausselkä Salpausselkä I was<br />
preceded preceded by deglaciation, during which which the the margin margin of ofthe the ice ice sheet sheet receded tens tens of of<br />
kilometres north of the the line line of Salpausselkä Salpausselkä I. The observations are mainly from the the<br />
part of Finland lying lying east of Lake Lake Päijänne. Päjänne.<br />
Sections where till overlies overlies glaciofluvial deposits deposits are a common common occurrence in in a 40km-widekm-wide<br />
zone zone on the the proximal side of of Salpausselkä Salpausselkä I. Some of these these deposits deposits are are<br />
longitudinal longitudinal eskers; eskers; others others are are more more dif<strong>fi</strong>cult diffrcult to de<strong>fi</strong>ne. defrne. They They frequently frequently display<br />
deformation structures structures and, and, in the the Lappeenranta-Savitaipale-Mäntyharju Lappeenranta-Savitaipale-Mäntyharju area, area, a<br />
base level level of oferosion erosion 10-20 m higher higher than than that that of ofyounger younger deposits. deposits.<br />
The network of ofglaciofluvial glaciofluvial deposits does not continue continue through Salpausselkä I. I. Only<br />
at at four four sites sites does an an esker esker that that started started some kilometres kilometres outside outside Salpausselkä I<br />
continue continue into into Salpausselkä Salpausselkä I, I, its extent extent demonstrated demonstrated by kettles kettles in in the the marginal marginal<br />
plateaus.<br />
Three new new observations observations of till-covered till-covered varved varved clays, clays, one of of them them 55 55 km km on on the<br />
proximal side of Salpausselkä Salpausselkä I, are are described. described. Balls Balls and lumps lumps of clay have been<br />
found found in glaciofluvial deposits, deposits, end end moraines moraines and and till. till. The The most most recent till there<br />
frequently frequently contains contains remnants of other sediments sediments as weH well as clay.<br />
The differences between the the sets of ofstriae striae on on either either side of ofSalpausselkä Salpausselkä I, especiaHy especially<br />
in the vicinity of Joensuu Joensuu and Päijänne, Päüjänne, lend fuel to to the the idea idea of a readvancing ice<br />
sheet.
39<br />
Thus Salpausselkä Salpausselkä I marks marks the limit of a number number of glacigenic phenomena. phenomena. The<br />
sequence of glacigenic glacigenic deposits is much more complex on the proximal proximal than on the<br />
distal side of ofthe the formation. formation. The till separates separates two sequences of ofdeglaciation deglaciation deposits<br />
of different age. The network network of glacial streams does not clearly continue through<br />
Salpausselkä Salpausselkä I, and the set of of striae striae on its proximal proximal side frequently frequently differs from that<br />
on its distal side. The uppermost uppermost till is rather immature, immature, and thus the original<br />
sediments can still be identi<strong>fi</strong>ed. identifred. These phenomena are most most obvious in an area<br />
extending extending from Salpausselkä Salpausselkä I to about 20 km on the proximal proximal side of Salpausselkä<br />
11, II, i.e. for 40-45 km. Farther away away they they are less less numerous, numerous, but till-covered<br />
sediments are still found 70-80 km km or more from from Salpausselkä I. During the Heinola<br />
deglaciation the ice sheet sheet seems seems to have receded receded to at least least 80 km north of<br />
Salpausselkä Salpausselkä I, to a line extending extending from from Koli Koli to to Turku T\rrku via via Viinijärvi, Heinävesi,<br />
Rantasalmi, Rantasalmi, Mikkeli, Kuhmoinen, Kuhmoinen, Toijala Toijala and Loimaa. Loimaa.<br />
Certain factors, however, argue against against the idea idea presented above. There is nothing<br />
in the varve chronology chronolory to corroborate the Heinola deglaciation (Niemelä (Niemelä 1971). The<br />
base level of erosion shown by the the till-covered glaciofluvial deposits is incompatible<br />
with what is known known of late-glacial late-glacial development on the distal side of Salpausselkä I.<br />
Many Many phenomena could also be be explained explained by several short oscillations of the ice<br />
margin. margin.<br />
It is pointed out that that neither neither the the clay clay chronology of Niemelä Niemelä nor the earlier<br />
chronology chronology of ofSauramo Sauramo support support the concept concept of ofsubstantial substantial oscillation. The high base<br />
level of of erosion indicated indicated by the till-covered till-covered glaciofluvial deposits was found to be<br />
incompatible incompatible with the fact that the g level, which is is markedly markedly lower than the B level<br />
and is interpreted as the base level level of of erosion in the distal area of Salpausselkä I,<br />
should also have existed existed in the north of Salpausselkä Salpausselkä I I during the Heinola<br />
deglaciation.<br />
deglaciation.<br />
III<br />
Rainio, H., Kejonen, .&, Kielosto, S. & Lahermo, P. 1986.<br />
Avancerade inlandsisen pä pa nytt ocksä ocksa till till Mellanlinska<br />
Mellan<strong>fi</strong>nska<br />
III Rainio, H., Kejonen, A., Kielosto, S. & Lahermo, P. 1986.<br />
randformationen? Summary: Is the Central Finland ice-marginal<br />
formation formation terminal? terminal? Geologi 38 (4-5), 95-109.<br />
Although generally considered a recessional formation, the Central Finland icemarginal<br />
formation - the fourth fourth large chain of ice-marginal ice-marginal formations in southern southem<br />
Finland - has has also been regarded as a a formation deposited in front front of an ice sheet<br />
that had readvanced readvanced for a few kilometres. This latter concept is based on the<br />
presence of a few till-covered glacial glacial deposits on the proximal proximal side of the formation.<br />
It has also been suggested that that the Central Central Finland Finland ice-marginal ice-marginal formation is a<br />
diachronous diachronous formation or that it deposited in a wide crevasse in the ice or in a large<br />
glacial bay or even even that it is an interlobate interlobate deposit.
40<br />
This This article presents new observations of of submorainie submorainic glaeial glacial deposits from from a zone<br />
about about 50 km wide on the the proximal side side of the the Central Central Finland Finland iee-marginal<br />
ice-marginal<br />
formation. formation. In 60 deposits the the till-covered till-covered material material is glaeiofluvial, glaciofluvial, and in 10 stillwaterwater<br />
sediments, that is, is, varved varved silt or clay. Information is also given on striae, the<br />
continuity of ofeskers, eskers, and and variations variations in the the late-glacial late-glacial base level level of of erosion. erosion.<br />
The strueture structure of the the Central Central Finland iee-marginal ice-marginal eomplex complex is that that of of a typicallarge<br />
typical large<br />
end end moraine, even even in parts parts earlier thought thought to have formed in in a crevasse or or between<br />
glaeiallobes.<br />
glacial lobes.<br />
Observations Observations show that that the the surroundings surroundings of of the the Central Central Finland end moraine moraine are<br />
similar to those those of Salpauselkä I. Most Most observations, old and and new, new, were were made made on on the<br />
proximal side of the formation. formation. The till till cover is generally generally 1-3 m, most frequently frequently 1-<br />
1.5 m, m, thiek. thick.<br />
The eskers eskers do not not eontinue continue across the end moraine. On the the proximal side, side, the the base<br />
level level of of erosion shown by by the the submorainie submorainic glaeiofluvial glaciofluvial sediments is is eonsiderably<br />
considerably<br />
higher, higher, 20-60 m, than than that that indieated indicated by by the the sediments without without a till cover. The<br />
directions directions of striae striae differ differ on the the two two sides sides of of the the marginal marginal formation. formation. Distal<br />
striations seem to oeeur occur as older older striations striations on the proximal side of the the iee-marginal<br />
ice-marginal<br />
formation. formation. A A particular partieular group group of striae striae on the the proximal side suddenly disappears at<br />
the end end moraine. moraine.<br />
These frndings <strong>fi</strong>ndings support the the views of of earlier researehers researchers that that the ice sheet<br />
readvaneed readvanced before deposition of the the Central Central Finland iee-marginal ice-marginal eomplex. complex. It now<br />
seems, however, that the iee ice margin retreated retreated farther than than was previously previously believed,<br />
that is, at at least least 50 km from from the the zone of the end end moraine. moraine.<br />
In short, the Central Finland end end moraine marks a limit separating areas of<br />
different striae directions, direetions, different erosion base levels, and different different groups of<br />
eskers. eskers. The area of submorainic submorainie sediments extends for at least 50 km km from from the end<br />
moraine. moraine.<br />
A cursory study of of the continuity eontinuity of of the eskers outside outside the Central Finland icemarginal<br />
formation seems to to imply that the margin margin of ofthe the ice sheet receded reeeded from the<br />
Salpausselkä Salpausselkä zone to the vicinity vieinity of the the Central Central Finland end moraine without any<br />
major readvances. readvanees. Thus the Salpausselkä readvance readvanee and the deposition of<br />
Salpausselkä Salpausselkä I were probably probably followed by by recession reeession ofthe of the ice iee to to a location loeation at at least<br />
50 km behind the zone of the Central Central Finland end moraine. The recession turned<br />
into into readvance, readvanee, and the margin of the ice sheet advanced to the zone of the the end<br />
moraine. To facilitate faeilitate discussion of the above events, events, it it is suggested that the<br />
deglaciation deglaciation following the readvance readvanee of the ice-sheet iee-sheet to Salpausselkä I should be<br />
known known as the the Keuruu Keuruu deglnciation deglaciation and the the subsequent readvance readvanee as the Jyuäskyki Jyuäskylä<br />
readuance.
41 4L<br />
IV ry Rainio, H. II. 1991. 1991. The Younger Younger Dryas f)ryas ice-marginal ice-marginal formations fomations of<br />
Southern Southern Finland. Finland. Eastern Eastern Fennoscandian Fennoscandian Younger Dryas end<br />
moraines. moraines. In: Field conference, North North Karelia, Karelia, Finland, Finland, and Karelian<br />
ASSR, ASSR, June June 26 -- July 4, 1991. 1991. Excursion Excursion guide. Rainio, H. & Saarnisto,<br />
M. (eds). Geological Survey Suney of Finland, Finland, Guide 32. 1991. pp. Pp. 25-72.<br />
The paper paper reviews reviews the the genesis, loeation location and and structure structure of the Younger Dryas end<br />
moraines in southern southem Finland and and the the Central Central Finland Finland end moraine and their<br />
relation to the the highest highest shore shore line. line.<br />
The structure of the the glaciofluvial glaciofluvial end moraines and their relation relation to glacial glacial rivers<br />
are described with reference to data data on a 170-km-Iong l70-km-long strip mapped between Lahti T.ahti<br />
and Joutseno. It is concluded that that the the moraines are are not not glaciofluvial deltas in the<br />
true meaning meaning of the the word. The structure structure of ice-marginal deposits shows that these<br />
landforms landfoms received similar similar amounts of of material along the the entire entire margin margin of the ice<br />
sheet. sheet. The ice never ceased ceased to flow while while the the end end moraine moraine was was depositing, and local<br />
melting and flow were approximately approximately in in equilibrium. As shown by the structure of<br />
Salpausselkä II in North Karelia, I(arelia, the the ice ice may may still have been been very active right up to<br />
the the end of deposition of the the moraine. moraine.<br />
Clearly Clearly different different in structure structure and also less less common common are are the the glaciofluvial deltas sensu<br />
stricto that that deposited at at the the mouth mouth of glacial glacial rivers, rivers, in in their their discharge bay.<br />
It is discussed whether whether Salpausselkä Salpausselkä I I is is a recessional or or terminal sedimentary<br />
event and demonstrated demonstrated that that it is most likely terminal, having deposited in front of<br />
a continental ice ice sheet that withdrew tens of of kilometres kilometres north north of the the place pI ace now<br />
occupied by the Salpausselkä and then readvanced.<br />
The The history of ofresearch research into the Salpausselkäs is is reviewed, with special emphasis on<br />
information gleaned from investigations investigations and concepts of the the 18th and 19th centuries<br />
put forward by by Rainio Rainio elsewhere.<br />
The problematic problematic area of North Karelia is discussed in the light of results presented<br />
earlier by Rainio. It is pointed out out that the scope of the Salpausselkä concept has<br />
not been de<strong>fi</strong>ned de<strong>fi</strong>ned with suf<strong>fi</strong>cient accuracv. accuracy.<br />
f,lamples Examples of Salpausselkäs I and and II, the Tuupovaara, Koitere Koitere and Pielisjärvi end<br />
moraines moraines and the the interlobate complex between Kiihtelysvaara and and Jaamankangas<br />
are given in site si te descriptions based on updated versions versions of Rainio's previous<br />
excursion guides. The examples were selected either because they represent represent the<br />
general features of the ice-marginal ice-marginal deposits or because their location is is important<br />
for the interpretation of the North Karelia deglaciation deglaciation and the genesis and<br />
conelation correlation of the Younger Dryas end moraines.
v<br />
42<br />
V Rainio, Rainio,Il. H. 1993. The The Heinola deglaciation and Salpausselkä readvance<br />
as recorded in in the lithostratigraphy of the the distal distal area of Salpausselkä<br />
I at Ihalainen, Lappeenranta, Lappeenranta, Finland. Finland. In: Geological Geological Survey Survey of of<br />
Finland, Current Research 1991-1992. Autio, Autio, S. (ed.). Geological Survey<br />
of ofFinland, Finland, Special Paper 18, 18,53-62, 53-62, 1993. 1993.<br />
A sequence of <strong>fi</strong>ne-grained varved sediments, 22 m m thick, thick, mainly mainly composed of elay clay<br />
and and <strong>fi</strong>ne frne silt was was studied studied in in a limes limestone tone quarry 1 km from the the distal distal flank of<br />
Salpausselkä 1. I.<br />
The flat surface ofthe of the <strong>fi</strong>ne-grained, frne-grained, water-laid water-laid deposits deposits is at 65-70 m a.s.l. a.s.l. The level<br />
of the Baltic Ice Lake (BI) was at no more more than than 105 m m a.s.l. at this this site. Hence, the the<br />
elevation of the Yoldia Yoldia Sea (YI) was at at 67-68 m a a.s.l. .s.l.<br />
Between 23 and and 16.75 m the the abundance of elay clay fraction fraction (0
43<br />
withdrew again from Salpausselkä I for at least 186 years before the Baltic Ice Lake<br />
drained drained to the level of ofthe the Yoldia Yoldia Sea. The sharp change from fat clay to coarse silt<br />
manifests manifests the dis discharge charge of the Baltic Ice Lake (BIll) (BIII) to the level of the Yoldia Sea<br />
(YI).<br />
The <strong>fi</strong>ndings frndings presented here are imcompatible imcompatible with the varved varved clay chronology of<br />
Sauramo Saura-o and Niemelä. Niemelä. The Ihalainen sequence shows shows that Salpausselkä I is<br />
terminal, not not recessional, and that that there there is a gap of ofat at least 500 years in the varved<br />
clay chronology chronologT of ofSouthern Southern Finland. Finland. The Lappeenranta Lappeenranta results results are, however, from<br />
a different glaciallobe glacial lobe area that that those of of Sauramo and Niemelä. Niemelä.<br />
If the bottom of the discharge öscharge varve varve was deposited 10 643 years before AD AD 1950<br />
(Strömberg, 1990), 1990), the bottom-most layers layers of of the the <strong>fi</strong>ne-grained <strong>fi</strong>ne-grained sediments started to<br />
deposit no later than 11 543 years before before AD 1950. According According to Sauramo's<br />
chronology, chronology, the ice margin stopped at Salpausselkä salpausselkä I 660 years before the Baltic<br />
Ice Ice Lake Lake (BIll) (BIII) dropped to the the Yoldia Yoldia (YI) level. Niemelä maintains that 1037 years<br />
separated the the beginning beginning of the sedimentation sedimentation of Salpausselkä land I and the discharge of<br />
the Baltic Ice Lake. If these <strong>fi</strong>gures frgures are are applied applied to Ihalainen, Ihalainen, the the Salpausselkä<br />
readvance came to an an end and Salpausselkä I I started started to deposit at at 11 303-11 803-11 680<br />
years before AD 1950. 1950. The turning turning point of the Heinola Heinola glaciation glaciation and the<br />
Salpausselkä Salpausselkä readvance would would then then have been at at 11 LL 457-11 457-rL 834 884 years before AD<br />
1950, 1950, and and the the <strong>fi</strong>ne-grained frne-grained sediments would would have started to deposit at Ihalainen at<br />
11 LL 821-12 82L-L2 198 years before AD 1950. These These <strong>fi</strong>gures <strong>fi</strong>gures are minimum ones.<br />
VI Rainio, H., Saarnisto, M. M. & Ekman, Ekman, I. I. 1995. Younger Dryas end<br />
moraines moraines in Finland and NW NW Russia. Russia. In: In: IGCP IGCP 253 - Termination of<br />
the Pleistocene Pleistocene - - <strong>fi</strong>nal report. Lundqvist, J., Saarnisto, M. & & Rutter, N.<br />
(eds.). Quaternary International, 28, 179-192.<br />
(eds. ). Quaternary International, 28, L7 I -I92.<br />
This paper is the frnal <strong>fi</strong>nal report of project IGCP-253 on Finland, Russian Karelia and<br />
Kola. Kola. It describes describes briefly the the location, structure and the relation to the highest sea<br />
line of the Younger Dryas end moraines moraines in these areas. Problems related to the<br />
correlation correlation of the ice-marginal ice-marginal moraines, including the Keiva moraines on the Kola<br />
Peninsula, are discussed discussed and issues are de<strong>fi</strong>ned that that require require further research. The<br />
connection connection of the late-glacial late-glacial Baltic Sea to the White Sea and the drainage channels<br />
of Lake Onega are discussed.<br />
The The paper summarizes summarizes the the views views expressed by the authors in their earlier papers.<br />
It is emphasized that the front of the continental ice sheet responded to climatic and<br />
glaciological changes differently in different different parts parts of the ice sheet. This may partly<br />
explain explain the age discrepancy between sectors ofchains of chains ofmorphologically of morphologically apparently<br />
continuous continuous end moraines. moraines. In any any case the ice ice margin responded to climatic and<br />
glaciological changes at somewhat different times in different sectors of the<br />
Scandinavian Scandinavian ice sheet.
44<br />
The conclusion is that that at at the the time time Salpausselkä l I was formed in in southern Finland<br />
the the margin margin of the the continental ice sheet sheet withdrew in North Karelia, Karelia, depositing a set<br />
of ice-marginal ice-marginal deposits over a wide zone. The The Tuupovaara Tuupovaara end moraine represents represents<br />
the the youngest youngest frontal frontal position position correlative conelative with with Salpausselkä 1. I. lts Its position suggests<br />
that that the the sector sector of of the the Koitere Koitere end end moraine moraine east east of of Lake Lake Koitere, Koitere, which which is<br />
contemporaneous with Salpausselkä II, had already started started to to deposit towards the<br />
end end of of the the formation formation of of Salpausselkä 1. I. The The orientation orientation of of the the Tuupovaara T\rupovaara end<br />
moraine moraine suggests suggests that, that, at at the the end of the the Salpausselkä l I stage, the the ice margin margin east<br />
of of Lake Koitere Koitere was located at at the the same level level as during during the the Salpausselkä Salpausselkä II stage.<br />
Thus, the the Koitere Koitere end end moraine moraine and its extension extension in Russian Russian Karelia may may represent<br />
both both the the late late Salpausselkä Salpausselkä l I stage and the Salpausselkä Salpausselkä II stage.<br />
The The <strong>fi</strong>ndings frndings presented by Rainio Rainio on the relation relation of the the end moraines in the the eastern eastern<br />
part of North North Karelia Karelia to to the the Salpausselkäs since 1972 L972 are summarized as folIo follows ws<br />
(Fig. 3):<br />
1) 1) At the the beginning beginning ofthe of the Salpausselkä Solpousselkci.I I phase phase the front front ofthe of the continental ice sheet<br />
ran ran from Värtsilä along the the Finnish-Russian Finnish-Russian border border to Möhkö, where it crossed into<br />
Russian Russian Karelia. Karelia. 2) The The Tuupouaara Tuupouaara end moraine moraine probably deposited at a late<br />
Salpausselkä Salpausselkä l I phase. 3) Salpausselkä Salpausselkit 11 II and a d the Koitere end moraine mnraine are largely<br />
contemporaneous. However, deposition of the eastern part of the formation, formation, east of<br />
Lake Koitere, Koitere, may have started started during during the late late Salpausselkä l I phase, at the same seme<br />
time time as that that of the Tuupovaara Tuupovaara ice-marginal ice-marginal formation. formation. The Koitere Koitere end moraine is<br />
physically physically correlative correlative with wit}r the Rugozero Rugozero (Rukajärui) (Rukajtirui) end end moraine rnoraine in Russia. 4) The<br />
Pielisjärvi Pielisjärui end end moraine moraine was deposited after after the the Baltic lee Ice Lake had had drained and is<br />
probably contemporaneous with with Salpausselkä III III in southwestern southwestern Finland. Finland. It is<br />
physically physically correlative correlative with with the Kalevala Kaleuala moraine moraine in in Russia. Russia.<br />
The divergent divergent concepts of Finnish Finnish and Russian researchers and their grounds for<br />
correlating correlating East Karelian end end moraines moraines with with the the Salpausselkäs and the end<br />
moraines moraines of North North Karelia are discussed.
DISCUSSION<br />
A hundred hundred years ago, Salpausselkäs Salpausselktis I and 11 II could be traced without without dif<strong>fi</strong>culty difliculty from<br />
western westem Finland to North Karelia despite the inadequacy inadequacy of research tools, from<br />
maps to communications. communications. This was possible because, in the supra-aquatic areas of<br />
southern southern Finland, the Salpausselkäs are very distinct, distinct, wide landforms landforms rising above<br />
their surroundings; surroundings; besides, the best roads ran along them. them. No wonder then that<br />
already already in the 18th century, century, Argillander had had been able to unite, not only the various<br />
parts of the Salpausselkäs, Salpausselkäs, but also also those those of the Jaamankangas-YhdyshaIju<br />
Jaamankangas-Yhdysharju-<br />
Salpausselkä Salpausselkä 11 II chain chain at at a time time when when there were no scienti<strong>fi</strong>c scientifrc grounds for classifying<br />
these "sandy eskers" or explaining explaining their their origin. origin.<br />
The trouble started in North Karelia, Karelia, where where the the ice-marginal ice-marginal formations are<br />
discontinuous, discontinuous, and sm smaller aller ridges are often often mainly mainly composed of till. Salpausselkä I<br />
has, accordingly, accordingly, not only only one, indisputable indisputable extension.<br />
The main reason for this this change in in the the mode of occurrence of the end moraines<br />
seems to be that the eastern eastern part of North North Karelia Karelia is is supra-aquatic and so<br />
unfavourable unfavourable to the the deposition of major major glaciofluvial end moraines. They tended to<br />
prefer sites with glacial lakes lakes in front front of of the ice. ice. Glaciofluvial marginal plains<br />
continue continue right up up to to the border of the the supra-aquatic area.<br />
The investigation of ofthe the frontal positions positions of ofthe the ice sheet sheet and deglaciation has been<br />
problematic in North Karelia and numerous opinions have have been expressed about the<br />
question in the course course of of this this century. century. North Karelia is also a key area in solving<br />
the relation between between the Salpausselkäs and other other Finnish Finnish end moraines with the<br />
end end moraines moraines in Russian Karelia.<br />
The front of the Scandinavian ice sheet at the time<br />
Salpausselkä I was formed<br />
45<br />
In the Kitee-Värtsilä-Tohmajäni Kitee-Värtsilä-Tohmajärvi area, the northeastern northeastern end of Salpausselkä I looks<br />
as if it has been divided into several parallel, but large, large, ice-marginal formations.<br />
This is clearly visible in the the big interlobate interlobate esker at at Peijonniemi, where there are<br />
three successive successive ice-marginal ice-marginal formations formations of some size over a distance of 5 km: the<br />
marginal plains of of Päivärinne and Kaurila-Musko Kaurila-Musko and the Nenosenlampi esker<br />
delta, delta, which is also the youngest. youngest. The 1- kmJong km-long Kiimakorpi ridge extends from the<br />
esker esker delta towards towards the fokälävaara Pykälävaara ice-marginal ice-marginal formation, the southern end of ofthe the<br />
Tuupovaara end end moraine, 5 km away. Hence, the T\upovaara Tuupovaara moraine is at the<br />
so-e same level as the youngest youngest part of Salpausselkä I.<br />
Judging by the the general trend of the outermost outermost parts of salpausselkä Salpausselkä I land and the<br />
striations, striations, the search for the extensions should should start in in the northeast or northnortheast.<br />
There There is no distinct continuous continuous chain of end moraines in that direction.
46<br />
In a zone zone about 10-km wide there are, however, however, a number of of moraines deposited at<br />
the the front of the the iee ice sheet that that eonstitute constitute a ehain chain possibly indieating indicating the position position of<br />
the the iee ice front during the the early early stage of ofSalpausselkä Salpausselkä I. I. This This ehain chain erosses crosses the Russian<br />
border at Möhkö, Möhkö, llomantsi Ilomantsi (Rainio, 1978, 1980, 1991 [IV]). tIVl).<br />
The glaeiofluvial glaciofluvial plains plains between Patsola and and Saarivaara Saarivaara that developed at the level<br />
of ofthe the Baltie Baltic lee lce Lake Lake (BI) support support the hypothesis that the front front of ofthe the iee ice sheet ran<br />
from from Patsola to to Möhkö Möhkö during during the the early early stage of of Salpausselkä I.<br />
From From the above and the loeation location of ofthe the sueeessive successive end moraines moraines at at the northeastem<br />
northeastern<br />
end of Salpausselkä Salpausselkä I I and the the Tuupovaara T\rupovaara end moraine, we ean can eonelude conclude that the<br />
front front of of the the iee ice sheet sheet withdrew withdrew from from Kitee Kitee and and from northeast northeast of Patsola in<br />
partieular, particular, whereas farther west it remained remained stationary stationary at Salpausselkä Salpausselkä I.<br />
The Salpausselkä Salpausselkä ares arcs east east of ofLake Lake Päijänne are at at a fairly fairly eonstant constant distanee, distance,20-25 20-25<br />
km, km, from from eaeh each other. other. The southem southern end of of the the Tuupovaara Tuupovaara end moraine is is 22 km km<br />
from from Salpausselkä Salpausselkä 11 II (Rainio, 1983 [I], p. 73), whereas its its northem northern end is 10 km<br />
from from the the Koitere end moraine. moraine. Henee, Hence, the the Tuupovaara Tuupovaara moraine marks marks the the si site te to<br />
whieh which the the iee ice sheet had had retreated retreated at the the time time Salpausselkä I I was forming. forming. If the<br />
Patsola-Möhkö line line refers to to the the initial situation, situation, then then the the iee ice sheet sheet had had retreated retreated<br />
at Petkeljärvi 15 km km farther than than during the the same time time at at Värtsilä.<br />
FF<strong>IN</strong>L<strong>AND</strong> <strong>IN</strong> L A ND<br />
;;äiä wi<br />
s9<br />
Shalgovaara<br />
9r.9" -<br />
iX aay<br />
RUSSIA<br />
Fig. 3, 3. Major Major end rnoraines moraines in Finl.and Finland and Russian Karelia (mod.i<strong>fi</strong>ed (modi<strong>fi</strong>ed<br />
from (rom Rainio et ol, al, 1995).<br />
1995),
47<br />
The orientation of the Tuupovaara T\rupovaara end moraine moraine suggests that, at the end of the<br />
Salpausselkä Salpausselkä I phase, the ice margin margin east of Lake Koitere Koitere was located at the same snme<br />
level as during the Salpausselkä 11 U phase. phase. Thus, the eastern part of the Koitere icemarginal<br />
formation and its extension extension in Russia Russia may may represent represent both the late<br />
Salpausselkä Salpausselkä I phase phase and the Salpausselkä 11 II phase. phase.<br />
The Tuupovaara T\rupovaara end moraine moraine excludes the possibility suggested by Hirvas (1980),<br />
Ignatius et al. (1980) and Nenonen Nenonen (as late as 1984) (see Kujansuu Kujansuu & Nenonen,<br />
1987) 1987) that during the Salpausselkä Salpausselkä I phase the front front of ofthe the ice sheet extended from<br />
Värtsilä to the Koitere end moraine moraine immediately immediately northeast northeast of Kiihtelysvaara<br />
(Rainio, 1983, 1983, p. 75).<br />
The relationship between Salpausselkä Salpausselkä 11 II and and<br />
the Pielisjärvi end mo moraine raine<br />
According to Sauramo Sauramo (1958, p. 397), 397), Jaamankangas was alandform a landform complex<br />
deposited at the front of ofa a readvanced ice ice sheet ("Dabei war sicherlich ein Vorrücken<br />
des Eisrandes eingetreten"). Analysis Analysis of of glacial lobe lobe dynamics led Salminen &<br />
Hartikainen (1985, pp. 11-12), later supported supported by by Eronen Eronen & Vesajoki (1988, p.824), p. 324),<br />
to much the same conclusion, namely, namely, that that after after the the Salpausselkä salpausselkä II phase the<br />
Lake-District glaciallobe glacial lobe was was initially in the the southern part of the Höytiäinen basin<br />
and that after it had withdrawn the North Karelia lobe readvanced to take its place.<br />
and that after it had withdrawn the North Karelia lobe readvanced to take its place.<br />
Together with their bordering kettle holes, the components of Yhdysharju<br />
(Connection esker) that join Jaamankangas Jaamankangas and are buried buried in its ice-marginal<br />
deposits imply that that the ice sheet withdrew from Salpausselkä II to the level of<br />
Jaamankangas Jaamankangas and that the end moraine deposited at at the front front of it without the<br />
oscillation oscillation of ice extending extending to the distal side of Jaamankmgas Jaamankangas (Rainio, 197s, 1973, pp.<br />
11-13, 11-13, 70-71; 1990, 1990, p. 33; 1991 [IVl, [IV], p. 43).<br />
According to to Eronen and vesajoki Vesajoki (1988, p. 320), "the "the slope of the Jaamankangas<br />
delta surface in a distal distal direction direction from about 1,20 120 m to 105 m a.s.l., along with the<br />
relatively relatively rough rough topography, indicates that a lowering lowering in water water level took place<br />
during deposition deposition of the the glaciofluvial sediments." This This is possible but, then again,<br />
the part of Jaamankangas Jaamankangas above the 105-m level may be a sandur as are the<br />
uppermost uppermost parts of many other other marginal marginal plains (Repo 1957, pp. 14g, 149, 166; 1g60, 1960, pp.<br />
10-11). The The upper part of Janmankangas Jaamankangas has abundant meltwater channels, which<br />
become become shallower shallower and less less frequent frequent in a distal direction direction (Rainio 1928, 1973, pp. 14-16;<br />
Lyytikäinen 1982, 1982, p. p. 39).
48<br />
The The relationship relationship between the the Central Central Finland and and<br />
Pielisjärvi end end moraines<br />
Nenonen (1993, (1993, pp. 48-50; 48-50; 1995b, pp. 79-80) 79-80) has postulated postulated that the the Central Finland<br />
end moraine moraine might might be contemporaneous with with Salpausselkä 111 III and the the Pielisjärvi<br />
end end moraine. The Jyväskylä readvance would would then have have occurred at least in central central<br />
Finland. Finland. This This concept concept requires, however, the ice ice sheet sheet to have have withdrawn for for about<br />
80-200 km at at the the central central part of of the the Salpausselkä are arc and and remained remained behind<br />
Salpausselkä Salpausselkä III and and the Pielisjärvi end moraine. Such Such an event would would have lasted<br />
several centuries. centuries.<br />
A A network network of of eskers ties ties Jaamankangas, Jan-ankangas, but also the the rest rest of of the the Pielisjärvi Pielisjärvi end<br />
moraine, to the same deglaciation cycle as the chain of the Salpausselkä Salpausselkä 11- II- Koitere<br />
end moraine. moraine. The Sarvinki-Vallisärkkä-Ahveninen esker clearly passes through through the<br />
formation. The Marjosärkkä esker runs runs through Jaamankangas, Jaa-ankangas, every now and then<br />
being being buried buried in it. An event event corresponding to the the oscillation oscillation of of ice ice - the the Keuruu Keuruu<br />
deglaciation -- Jyväskylä Jyväskyla readvance - could not not have occurred in North Karelia. Karelia.<br />
Had it done so, shoreline displacement displacement at the Lake-District glaciallobe glacial lobe would would have have<br />
been quite quite different from that at the neighbouring neighbouring lobes. lobes. Owing to uplift, uplift, the highest highest<br />
shoreline on the the proximal side of the the Pielisjärvi end end moraine and Salpausselkä 111 III<br />
would be at a distinctly lower level than than at at the the Lake-District glaciallobe. glacial lobe. There is,<br />
however, nothing nothing to support this this concept, at at least least on on the the proximal side side of of the the<br />
Pielisjärvi ice-marginal formation. The The highest shoreline shoreline in in the subaquatic areas of of<br />
Höytiäinen Höytiäinen and and Pielinen Pielinen is at the the same level level as as it is in the the end end moraine, moraine, not not<br />
conspicuously lower (Sauramo, (Sauro-o, 1928; Saamisto, Saarnisto, 1970; Hyvärinen, Hyvärinen, 1966a).<br />
Besides, Besides, the the ice front front would would have twisted twisted and tumed turned so much that, that, for that that reason<br />
if no other, other, the the hypothesis hypothesis seems improbable.<br />
At At sites where end moraines moraines connecting ice-marginal complexes should exist, exist, there<br />
is no sign sip. ofthem of them for for hundreds ofkilometres, of kilometres, only only interlobate interlobate deposits, and and most most of<br />
them are are distinct östinct longitudinal longitudinal eskers. eskers. This This does does not not necessarily necessarily nuHify nullify the<br />
hypothesis, hypothesis, but nor nor does it support it. it.<br />
Shoreline displacement in in North Karelia<br />
At At some key key sites in in North North Karelia Karelia shoreline displacement displacement is is still still not not known known weH well<br />
enough, and very very speci<strong>fi</strong>c specifrc claims cannot therefore be based based on it.<br />
it.
49<br />
At Valkeasuo, on the distal side of ofthe the northem northern end of ofSalpausselkä Salpausselkä H, II, the levels of<br />
ponds are only 5 m below the base level of late-glaeial late-glacial erosion. Somewhat farther<br />
north, at Kiihtelysvaara, the levels of ponds ponds are about 10 m lower than the surfaees surfaces<br />
of adjaeent adjacent plains. Taking into aeeount account the gradient of uplift, it may well be that<br />
there was onee onoe a late-glaeial late-glacial lake at the present site of the ponds. Being at a<br />
slightly higher level than the Baltie Baltic lee Ice Lake, this this lake then regulated the level of<br />
deposition. Therefore, the plains are at a higher higher level than might be expeeted expected from<br />
the rest of Salpausselkä. Salpausselkä. The eonelusion conclusion drawn drawn from this is that the iee ice sheet<br />
withdrew from Salpausselkä 11 II at Kiihtelysvaara Kiihtelysvaara somewhat earlier than elsewhere<br />
(Saarnisto 1970).<br />
The same sa'ne situation prevails at the front of of Salpausselkä 11 II over a distance of 20 km lr-<br />
south of Onkamo. Onkamo. A few tens of of metres metres above the level of BIll, BIII, there seem to have<br />
been been several smalllakes small lakes that that regulated regulated the growth of the Salpausselkä plains. The<br />
elevations elevations of these these plains and those formed formed in the Valkeasuo glaeiallake glacial lake may have<br />
prompted Sauramo Sauramo to eonelude conclude that Salpausselkäs Salpausselkäs land I and II joined eaeh each other in<br />
N North orth Karelia.<br />
When When the iee ice sheet withdrew from Salpausselkä 11 II at Kiihtelysvaara, a glaeiallake<br />
glacial lake<br />
formed in the valley of of the the present river river Pielisjoki Pielisjoki and drained to the Jänisjoki<br />
watereourse watercourse between the Yhdysharju-Tervasuo Yhdysharju-Tervasuo deposits and Heinävaara along the<br />
distal side of of Salpausselkä salpausselkä 11 II (Rainio, 1990, p. 35). Bb). At At that site there is a very<br />
distinet distinct aneient ancient ehannel, channel, whose threshold, threshold, at at an elevation of about 120 m, is at the<br />
Ilomantsi railway. The level level of this this glacial glaeiallake lake controlled eontrolled the growth growth of the plains<br />
of of Yhdysharju (Connection (Conneetion esker). The elevations of the summit plains plains are almost<br />
the snme same as as those those of of the plains at the northern northem end end of Salpausselkä 11 U attributed to<br />
the the Baltic Baltie Ice lee Lake. Lake. Consequently, they, they, too, are included ineluded in the srme same gloup group (e.g.<br />
Eronen & Vesajoki, 1988, 1988, Fig. 2, pp 319 and and B2B). 323). Among them are the plains at<br />
Kruununkangas and Kerolankangas, Kerolankangas, Paihola, and the Kaukaansärkät esker.<br />
It lt is not known known for sure when the waters of ofthe the Pielisjoki Pielisjoki valley north of ofYhdysharju Yhdysha{u<br />
(Connection esker) esker) started to flow along a new channel, ehannel, thus causing eausing the water level<br />
and the base base level of erosion to drop. drop. The <strong>fi</strong>rst <strong>fi</strong>rst lowJying low-lying tracks lead to the distal<br />
side of salpausselkä Salpausselkä II, to valkeasuo, Valkeasuo, where the base level of of erosion was, as<br />
mentioned above, still close elose to the the level of the Baltic Baltie Ice lee Lake, even after drainage<br />
of this lake.<br />
We cannot, eannot, therefore, state categorically eategorieally what wh at the the base level level of erosion was at the<br />
time Jaamankangas Jaamankangas started to deposit. It may have been the same as the level of<br />
the Pielisjoki glacial glaeial lake or some other ephemeral water surface surfaee at a considerably<br />
eonsiderably<br />
higher elevation than the contemporaneous eontemporaneous Baltic Baltie Sea. It is also possible that<br />
Jaamankangas Jaamankangas did not start to deposit until after the drainage of these ephemeral<br />
glacial glaciallakes lakes and the Baltic Baltie Ice lee Lake (saarnisto, (Saamisto, 1970). The sur<strong>fi</strong>cial sur<strong>fi</strong>eial parts of
50<br />
Jaamankangas are composed of sandur deposits up to 15-20 m thick, as indicated by<br />
the the abundance ofchannels. of channels. At any rate, the channels show that towards the the end of<br />
depositiou deposition of Jaamankangas J aamankangas the base level of erosion was close elose to that of the Yoldia<br />
Sea (Saarnisto, 1970; 1970; Rainio, 1973). 1973). The seme same elevation is also represented by the<br />
other plains of of the Pielisjänd Pielisjärvi end moraine and the extramarginal plains in the<br />
Pielisjoki valley (Rainio, 1973).<br />
Final phases of the Alleröd Nleröd chron at at Ilomantsi<br />
Eronen Eronen and Vesajoki (1988, p. 321) 321) pointed out "that there is is no distinct break-off<br />
zone in the eskers eskers in the domain ofthe of the Norht Karelian lobe. It is thus apparent that<br />
the the Heinola Heinola deglaciation and the following following readvance were limited to the region<br />
occupied by the the Lake Distriet District lobe."<br />
Eronen and Vesajoki are are referring to a very small-scale map (op. cit. p. 319, Fig. 2).<br />
Most Most of the the eskers on it are short short and discontinuous, and do not not continue continue through<br />
the the Salpausselkä I I zone. The large Petkeljärvi-Putkela interlobate esker, however,<br />
seems to begin outside the the Salpausselkä Salpausselkä I I zone and to to pass through through it. As the the key<br />
area for for interpreting interpreting the the continuity of the the esker is located at the the Finnish-Russian<br />
border and also on the Russian side of o<strong>fi</strong>t, it, the issue is is dif<strong>fi</strong>cult diflicult to to settle. settle. The part of of<br />
the the Petkeljärvi Petkeljärvi esker elose close to the the Russian Russian border border displays displays features typical typical of of an an<br />
ice-marginal formation. formation. It is possible that that the the esker and its apparent continuation,<br />
the Tolvajärvi esker, represent two different different deglaciation cyeles. cycles.<br />
If, If, on the the other other hand, hand, the the Tolvajärvi Tolvajärvi esker and the the Petkeljärvi-Putkela esker are<br />
part part of the same esker chain chain (cf. Frosterus Frosterus & Wilkman, Wilkman, 1915, 19L5, pp. 70-72) 70-72\ (Fig. 1),<br />
they they represent represent the the very very deglaciation deglaciation cyele cycle during which which the ice ice sheet sheet withdrew<br />
through the Salpausselkä I zone. The relationship of the Petkeljärvi-Putkela chain chain<br />
and the associated lateral Iateral eskers to the other Quaternary formations in the vicinity,<br />
the the Koitere Koitere ice-marginal ice-marginal formation formation in particular, is such that the chain chain probably<br />
represents represents the the last deglaciation deglaciation stage. stage. This would imply that there there was no<br />
readvance to Salpausselkä Salpausselkä as coneluded concluded by Eronen and Vesajoki, at least at the the<br />
North North Karelia Karelia glaciallobe.<br />
glacial lobe.<br />
It is hard hard to imagine imagine a fairly large large oscillation oscillation taking place place at one glacial lobe and<br />
not in an adjacent adjacent area. For For the deglaciation deglaciation his history tory of of Finland as a whole, whole, it would<br />
be important to establish establish whether whether the the Petkeljärvi-Putkela esker was deposited by<br />
the same glacial river as the Tolvajärvi esker, esker, which which has been associated associated with it<br />
(Frosterus & Wilkman, Wilkman, 1915, 1915, pp. 70-72). 70-72).In In other words, words, did did the Petkeljärvi-Putkela<br />
and Tolvajärvi eskers eskers deposit deposit during during the same deglaciation deglaciation stage?
Interpretation of bottom deposits<br />
51<br />
Punkari & Boulton (1995, Fig. Fig.4, 4, p. 7) have reinterpreted reinterpreted the succession of ofbottom bottom<br />
deposits at Lappeenranta immediatelyon immediately on the distal distal side of of Salpausselkä Salpausselkä I described<br />
by Rainio (1993, V) and the very very aspects on which which Rainio Rainio based his conclusions.<br />
According to them, the lowest part part, of the succession, the A layer, in which the<br />
material is <strong>fi</strong>ne frne grained and mainly composed of of clay, clay, represents represents a short withdrawal<br />
during the deposition of of Salpausselkä I, when when the ice sheet sheet was 2-4 km L- from the site<br />
of deposition. Rainio interpreted this this as representing representing the withdrawal withdrawal of the ice,<br />
whilst the following B layer layer referred referred to readvance readvance during the Heinola<br />
deglaciation-Salpausselkä readvance. readvance. According Accordingto to the the interpretation of Punkari and<br />
Boulton, the B B layer and and the the roughly 6-m-thick, fairly fairly coarse-grained silty, in places,<br />
coarse silty C layer refer to the time time when the ice front front withdrew from Salpausselkä<br />
I to to Salpausselkä Il. II. For Rainio, Rainio, the C layer represents the time when Salpausselkä<br />
I I deposited. Boulton Boulton and Punkari postulate that that the the shallow clayey layer overlying<br />
the C layer is contemporaneous with with Salpausselkä Salpausselkä Hand, II and, in general, general, with BIll. BIII.<br />
Rainio contends that it also represents represents the withdrawal of ice ice from Salpausselkä I to<br />
Salpausselkä H. II.<br />
The interpretation of ofPunkari Punkari and and Boulton Boulton turns turns cause and effect upside down: At<br />
its front an ice sheet creates creates a a large large glaciofluvial ice-marginal ice-marginal formation formation and<br />
immediately outside it a a clayey clayey deposit. During During the <strong>fi</strong>rst hundred hundred years years of<br />
withdrawal the sediment becomes coarser. coarser. Enough Enough coarse silt and <strong>fi</strong>ne frne sand are<br />
available to form deep layers over a distance distance of up to 20 km from the withdrawing<br />
ice front. when When a really large ice-marginal formation, formation, the Taipalsaari marginal<br />
plain, starts to deposit, deposit, the the bottom sediment becomes rich in clay fraction; not a very<br />
convincing interpretation.<br />
Even Even more compelling evidence evidence for the interpretation of Rainio against that of<br />
Boulton and Punkari is is the edstence existence of the the supra-aquatic ridge ridge of Salpausselkä II<br />
between the Ihalainen sempling sampling site and the ice sheet withdrawing from<br />
Salpausselkä I. I. The ridge ridge extended extended for at at least least 5 km in in both both directions and thus<br />
prevented coarser coarser material from being transported transported en en masse from the direction of<br />
the ice sheet to Ihalainen. Moreover, bottom deposits are rare between<br />
Salpausselkäs Salpausselkäs I and II Il and there do not seem to be any flatJying flat-lying deposits<br />
coresponding corresponding to to the the Ihalainen C layer in in the 1:100 1:100 000-scale OOO-scale map sheet area of<br />
Lappeenranta. Lappeenranta. According to the interpretation of Punkari and Boulton, these<br />
deposits deposits should abound abound there.
52<br />
The The arguments presented presented by by Rainio Rainio in in 1985 1985 can be used as supplementary evidence.<br />
Thus, Thus, between Salpausselkäs I I and 11 II there there are till-covered deformed glaciofluvial<br />
deposits over a large area. Remruns Remains of clay clay deposits deposits occur occur in many many places and chruns chains<br />
of ofeskers eskers do not not pass through through the the end moraines.<br />
Referring Referring to to Okko Okko (1962) and Rainio Rainio (1985a [11)), [II]), Punkari and Boulton Boulton (p. 7) write<br />
that that the the readvance has has been justi<strong>fi</strong>ed justifred by the the presence of of cross striations striations and<br />
attribute attribute the the turning of flow flow directions to glaciallobe glacial lobe dynamies. dynamics. The use of a single<br />
argument argument like like this this is is misleading, misleading, for for the the readvance of of the the ice ice sheet is is based on<br />
several arguments, as shown above. Among other other things, things, striations with different öfferent<br />
orientations orientations support the the concept concept of the the readvance.<br />
The The Salpausselkä readvance readvance<br />
Inferences about about the the readvance of the the ice ice sheet to to Ss I I and and the the Central Central Finland<br />
ice-marginal ice-marginal formation formation are based based primarily on the the fact fact that that many many glacial features features<br />
change change sharply sharply at these these formations.<br />
formations.<br />
It has also been been argued that that the the concentration of till-covered sediments in in certrun certain<br />
zones zones need not necessarily be due to one single advance. In Sweden, Sweden, Persson Persson (1983)<br />
and Lundqvist Lundqvist (1987) have attributed attributed similar similar stratigraphies stratigraphies to aseries a series of halts halts in in<br />
the receding ice front front (Lundqvist, 1990, p. 20).<br />
Aseries A series ofbriefhalts ofbriefhalts does not, however, explain the sudden change in in striation, the<br />
difference in the the base base levels levels of glaciofluvial sediments and and the the break in in the network network<br />
of ofglacial glacial rivers. rivers. The eskers eskers continue across the the marginal marginal terraces of ofSs Ss 11 II and the<br />
Pielisjärvi end end morrune, moraine, which were formed during during long-lasting stillstands, but not<br />
across Ss land I and the the Central Central Finland ice-marginal formation.<br />
The most important points points supporting supporting the the readvance are the the presence of abundant<br />
till-covered, till-covered, varved varved bottom bottom sediments sediments on on the the proximal side side of of Salpausselkä Salpausselkä I I<br />
(Berghell, 1904; Frosterus Frosterus & Wilkman, Wilkman, 1915; 1915;Virkkala, Virkkala, 1948, 1948, p. p. 31; Sauramo, 1958,<br />
p. 274; Hirvas & & Nenonen, 1980, 1985, 1985, 1987; Rainio, Rainio, 1982, L982, 1985a [11]; [II]; Nenonen,<br />
1984; Kujansuu & & Nenonen, 1987) and the the numerous observations of clay lumps<br />
transported transported by the the ice sheet or of deformed clay (Berghell, 1898, pp. 35-36; Rainio,<br />
1984 1984 a,b, a,b, 1985a 1985a [11)). [II]). These These subtill subtill varved varved clays are are most most easily easily attributed attributed to<br />
readvancing readvancing ice.
CONCLUSIONS<br />
54<br />
In the course of time, different methods have been used in attempts to establish the<br />
position of the ice sheet front in North Karelia at the time the Salpausselkäs<br />
formed. Results have differed accordingly. The greater the emphasis on one<br />
particular method, the more surprising tr1t" gmrlings In the course oftime, different methods have been used in attempts to establish the<br />
position of the ice sheet front in North Karelia at the time the Salpausselkäs<br />
formed. Results have differed accordingly. The greater the emphasis on one<br />
particular method, the more surprising the fmdings have have been. been. This is partly due due to<br />
the the fact fact that that the nature nature of the material on which which one particular method was based based<br />
was was not not studied studied suf<strong>fi</strong>ciently suf<strong>fi</strong>ciently and and partly because the the basic basic principles and and the<br />
nomenclature nomenclature were only poorly de<strong>fi</strong>ned.<br />
The The introduction introduction to to the the present thesis thesis outlines outlines the the arrival anrival of of the the principles of<br />
modern modem geological thinking thinking in Finland Finland and and the the his history tory of of research research into into the<br />
Salpausselkäs Salpausselkärs - from from a convenient roadway to to part part of of a network network of of sandy eskers,<br />
and from from a water water divide to to an ice-marginal formation. formation.<br />
The original original objective of the the study, study, to to establish the the position of the the continental continental ice<br />
sheet front front in eastern North Karelia, Karelia, has been achieved. All three Salpausselkä end end<br />
moraines moraines have have their their counterparts counterparts in North North Karelia. The The front of of the the ice sheet sheet<br />
continued from the Salpausselkäs eastwards more more or or less as proposed at the turn of<br />
the the century. The The main main difference lies lies in the the position of of the the ice ice front front during during the<br />
deposition of Salpausselkä I.<br />
Both the differences between chains of ice-marginal ice-marginal deposits and and the lack of distinct<br />
end moraines can be attributed attributed to to differences in the the behaviour of the the ice sheet at at<br />
different times and under different different conditions. In North Karelia, Karelia, Salpausselkä land I and<br />
Salpausselkä Salpausselkä II II differ differ in structure. structure. Salpausselkä Salpausselka I is is mainly mainly composed of<br />
glaciofluvial marginal marginal plains, but but in the the proximal part of of the the wide wide glaciofluvial<br />
plains of Salpausselkä Salpausselkä II there there is a a very very large large end end moraine moraine ridge. ridge. Even Even in in<br />
supra-aquatic supra-aquatic areas, areas, Salpausselkä Salpausselkä II II has has a clear clear counterpart, counterpart, the the Koitere Koitere end<br />
moraine, but but Salpausselkä I I has none.<br />
One reason reason for for this this seems seems to be be that during the the Salpausselkä I stage the continental<br />
ice sheet front, instead instead of remaining remaining stationary stationary in in North Karelia Karelia as it it did did farther farther<br />
west, withdrew. withdrew. This This is is indicated by by the the presence of a wide zone of successive end<br />
moraines at Kitee-Tohmajärvi; moreover, the the ice front front seems to to have been at the<br />
Patsola- Möhkö line at the time time offormation of formation ofthe of the Salpausselkäs, and the northern northern<br />
end end of the the Tuupovaara end end moraine chain chain is is about 10 10 km closer closer to the the Koitere Koitere end<br />
moraine moraine than than its southern end end is is to Salpausselkä II.<br />
In In the the supra-aquatic area northeast of ofVärtsilä, Värtsilä, Salpausselkä I I does not have such<br />
a well-developed well-developed counterpart counterpart as the the two two other other Salpausselkäs. Salpausselkäs. elose Close to the<br />
Finnish-Russian border, there is is a discontinuous zone of ice-marginal deposits and
55<br />
hummoeky hunmocky moraines that may represent represent the early stage of Salpausselkä salpausselkä I,<br />
partieularly particularly as, direetion-wise, direction-wise, it eould could be an extension of of Salpausselkä 1. I. The plains plains<br />
in the the Baltie Baltic lee Ice Lake about 10 km km northeast northeast ofPatsola eorroborate comoborate the eoneept concept that<br />
the iee ice front initially ran from Patsola to Möhkö Möhko at the time Salpausselkä I formed.<br />
The The Tuupovaara T\rupovaara end end moraine deposited deposited during during the late stage of ofSalpausselkä Salpausselkä 1. I. The<br />
relationship between the end moraine moraine at Tuupovaara Tuupovaara and Koitere suggests that the<br />
part of the Koitere end moraine east of Koitere Koitere represents represents the end of the<br />
Salpausselkä Salpausselk:i I phase and the Salpausselkä II phase.<br />
The landform system most most clearly clearly eontemporaneous contemporaneous with Salpausselkä II is the<br />
Koitere end moraine. Running uninterrupted uninterrupted from from northeast northeast of the village village of<br />
Kiihtelysvaara to the the Russian Russian border (Rainio, 1978, 1985b, 1991 1gg1 [IV]; Frosterus &<br />
Wilkman, wilkman, 1915), 1915), the moraine moraine eontinues continues without without a break into Russian Karelia. It<br />
includes the Selkäkangas Selkäkangas iee-marginal ice-marginal formation, fomation, known sinee since the early days of<br />
work on these formations formations (e.g. Ramsay, 1891).<br />
The boundary boundary between these iee-marginal ice-marginal formations is is marked marked by the eontaet contact of<br />
two two large large glaeiallobes, glacial lobes, The Lake District District and the North Karelia lobes, lobes. where there<br />
is a gap in the the ehain chain of iee-marginal ice-marginal deposits.<br />
The third ehain chain of iee-marginal ice-marginal deposits, the over 100-km-long lOO-km-Iong Pielisjärvi moraine,<br />
is fairly eontinuous, continuous, extending extending from from Jaamankangas Jaamankangas to the Russian border. From its<br />
position, if nothing else, it is younger younger than than Salpausselkä 11. II. Between the north end<br />
of of Salpausselkä Salpausselkä II II at at Kiihtelysvaara and and Jaamankangas there is an interlobate<br />
complex eomplex and and three three eskers. eskers. These These eskers eskers extend to Jaamankangas and are buried by<br />
its delta delta deposits. deposits. Shoreline Shoreline displacement displaeement shows that this chain ehain of end moraines mo raines did<br />
not deposit deposit until after the drainage drainage of the the Baltic Baltie Ice lee Lake, and that it is of about the<br />
same same age as Salpausselkä Salpausselkä III in southwestern southwestern Finland.<br />
The The Pielisjärvi end moraine extends 50 km northeastwards from the large marginal<br />
plain of Jaamankangas Jaamankangas to Uimaharju UimahaIju (Rainio, 1985b). The marginal plains and<br />
valley trains of the formation are at about 105 m a.s.l., clearly elearly below the level of the<br />
Baltic Baltie Ice lee Lake Lake (Saarnisto, 1970; 1970; Rainio, 1985b). The Pielisjärvi Pielisjärvi end moraine was<br />
thus formed after the the drainage of the Baltic Baltie Ice lee Lake Lake and, accordingly, aeeordingly, is younger younger<br />
than Salpausselkä II. 11. The Pielisjärvi end moraine may also be time-correlative time-eorrelative with<br />
Salpausselkä Salpausselkä III (Sauram (Sauramo, o, L929, 1929, Rainio, 1985b).<br />
Northeast Northeast of Uimaharju, UimahaIju, the ice-marginal iee-marginal deposits was deposited mainly on supraaquaticaquatie<br />
terrain except exeept north of Lake Lake Koitere Koitere where it was deposited in a glacial glaeial<br />
lake. This area excluded, the ice-marginal iee-marginal formation extends as an almost unbroken<br />
moraine moraine ridge across aeross the Russian border.
56<br />
The Pielisjänri Pielisjärvi end end moraine does not have a distinct counterpart at the Lake Lake<br />
District glacial lobe between Päijänne Päijänne and North North Karelia, demonstrating that the the<br />
glacial lobes differed in dynamics.<br />
Numerous arguments support the the concept that the continental continental ice sheet readvanced<br />
twice for tens of kilometres in late-glacial time, frrst <strong>fi</strong>rst before before the formation of<br />
Salpausselkä I land and then again before the deposition of the Central Finland Finland end<br />
moraine. For one thing, in the proximal proximal zones zones of these end end moraines moraines the younger till<br />
is underlain by by a a sequence of older deglacial deposits. Most Most of the observations of<br />
this this sequence are of deformed glaciofluvial deposits. TilI Till and bottom deposits have<br />
been obseryed observed in cuttings, although although less often. often. Striations can usually be attributed<br />
to readvance of the ice. Differences in base levels of erosion between glaciofluvial<br />
deposits of different ages are sometimes considerable. Eskers do not pass pass through<br />
these ice-marginal formations. formations. The lithostratigraphy of the bottom bottom sediment sediment on on the<br />
distal side of Salpausselkä Salpausselkä I I also supports this this interpretation.<br />
The outcome of the the present present study study is briefly:<br />
1) 1) Arguments presented to support support the major major oscillations oscillations in southern southern Finland - the the<br />
Heinola deglaciation-Salpausselkä readvance and and the Keuruu Keuruu deglaciation-Jyväskylä<br />
deglaciationJyväskylä<br />
readvance readvence - are more conclusive than than those those presented presented to refute refute them. them.<br />
2) At At the beginning beginning of the the Salpausselkä I I phase phase the front front of the the ice sheet sheet ran from<br />
Värtsilä Värtsilä along the the Finnish-Russian Finnish-Russian border to Möhkö where it crossed the border border to<br />
Russian Karelia. Karelia.<br />
3) The Tuupovaara end moraine moraine was deposited during during a late Salpausselkä I phase.<br />
4) Salpausselkä Salpausselkä II and the the Koitere Koitere ice-marginal ice-marginal systems systems are largely contemporary.<br />
contemporar5r.<br />
However, However, deposition deposition of the the eastern eastern part part of the the moraine, moraine, east of Lake Lake Koitere, Koitere, may<br />
have started started during the the late Salpausselkä Salpausselkä I I phase, at the the same time as that that of the the<br />
Tuupovaara T\rupovaara end moraine. moraine.<br />
5) The Pielisjärvi end moraine was deposited after after the Baltic Ice Lake Lake had drained drained<br />
and and is probably synchronous synchronous with with Salpausselkä Salpausselkä III in southwestern southwestern Finland. It is<br />
physically correlative conrelative with the the Kalevala Kalevala mo moraine raine in Russia.
Closing words<br />
A hundred years ago, Rosberg summed up the situation situation in research into the<br />
Salpausselkäs Salpausselkl,s with the words: "Men fragan frägan är ännu längt längt ifrän slutdiskuterad" (But<br />
the issue issue is still far from settled") settled") (Rosberg, 1899, p. 1).<br />
ACKNOWLEDGEMENTS<br />
ACIOYOWLEDGEIVIEIYIE|<br />
57<br />
Back in summer 1968, I received an an invitation invitation from from Reino, "Reiska" Repo - my<br />
Karelian friend and superior superior - to visit him at his study study area in Lohja. We drove<br />
along admiring Salpausselkä. And And there, there, between the lines lines and the cuttings, Reiska<br />
appointed me to continue continue his work work in North North Karelia. Karelia. Later Later he watched with<br />
enthusiasm enthusiasm as new new chains of ice-marginal ice-margi:lal formations foruations were were found. found. In summer 1973, 1928,<br />
destiny destiny permitted him one more <strong>fi</strong>eld freld trip trip - to these very landforms landfoms - before he fell<br />
fatally ill. It was on that that trip trip that that he he said to to me: me: 'No 'TrIo matter matter if results prove me<br />
wrong; wrong; the the main thing is, we get results." results." Thank Thank you, Reino.<br />
This This work work began began then then in 1968. Since then I I have have received assistance, encouragement<br />
and and support support from countless people; people; the the following following list list includes includes but a few.<br />
First and foremost, I thank my my wife, Kaija, Kaija, and and my my children, children, Ohto, Viena and<br />
Kuisma, Kuisma, for for their understanding understanding and forbearance.<br />
I warmly thank Aino Aino and Antti Ihanus Ihanus as well well as as Arja and Erkki Ihanus for putting<br />
up up with me during the long periods periods that I used Tohmajärvi as my base.<br />
My old friend and teacher, Professor Marjatta Okko, set me on the path path to science<br />
and research before she moved on to more demanding demanding duties. She bears bears no<br />
responsibility for my stumbling progress progress along the the path.<br />
The The Geological Survey Survey provided provided the the ideal a-bience ambience for for a study of this nature. The<br />
director general, Professor Veikko Veikko Lappalainen, followed followed my progress with with keen<br />
interest; interest; Dr Kalevi Virkkala, Dr Raimo Raimo Kujansuu, Kujansuu, Dr Matti Saarnisto and Dr<br />
Tuulikki Grönlund, Grönlund, heads of department, department, and Dr Kauko Kauko Korpela, research director,<br />
were generous with both both encouragement and pressure; pressure; and my long-time superior,<br />
Dr Pentti Lindroos, Lindroos, gave my work his blessing.<br />
I want to thank Professors Toive Aartolahti and Veli-Pekka Veli-Pekka Salonen who as<br />
reviewer of my work critically read the the manuscript manuscript and gave gave valuable comments.
58<br />
Timo Timo Ruohomäki was a a highly highly capable and and most industrious industrious <strong>fi</strong>eld freld assistant for for a<br />
decade and more. more. Practical Practical man man that that he he is, he saw saw to to all all the the day-to-day day-to-day<br />
arrangements and, nnd, if necessary, necessarlr, was ready ready to to work work round round the the dock. clock. Despite the<br />
years the the study study took, took, his his con<strong>fi</strong>dence never never wavered. At At various various times times I also had<br />
invaluable invaluable help help in both both <strong>fi</strong>eld <strong>fi</strong>eld and of<strong>fi</strong>ce of<strong>fi</strong>ce from from Arto Arto Kiiskinen, Maila Koivisto, Koivisto, Harri Hani<br />
Kutvonen, Piritta Oksanen, Seppo Putkinen Putkinen and Seppo Töllikkö. TöIlikkö.<br />
Over the years, the the cartographers, cartographers, Satu Satu Moberg, Moberg, Pirkko Pirkko Oranne, Oranne, Hilkka Hilkka<br />
Saastamoinen and Hilkka Vesterinen, found neat solutions solutions to many of the the problems problems<br />
involved in drawing diagrams diagrams and maps. TaIja Tarja Koski Koski and Eija Taimi, Taimi, for their part,<br />
patiently analysed my my endless endless soil soil sampIes. samples.<br />
The The staff staff of of the the Geological Survey Survey library library endured endured my my sometimes outlandish outlandish<br />
requests for for books and and maps. Thank Thank you you Kristiina I{ristiina Alho, Alho, Kat Katja ja Kononen, Kononen, Helka Helka<br />
Lauerma, Eija Törmälä, Törmälä, Lahja Lahja Voutilainen and Liisa Liisa Vuorela. Vuorela.<br />
Without Without the the valuable valuable editorial editorial assistance of of Caj Caj Kortman, Kortman, Sini Sini Autio Autio and and Stiina Stiina<br />
Seppänen, my my publications publications would have been the the poorer.<br />
Pertti Pertti Lahermo has been a good friend friend throughout, throughout, a colleague with with whom I I could<br />
always always left left off steam. steqrn.<br />
Carola Eklundh Eklundh and and Gillian Gillian Häkli Häkli put put my my words into into Swedish and English English aptly<br />
and promptly. Special thanks thanks to Gillian Gillian for translating this this manuscript.<br />
And And these these are are but but a few few of the the many many friends friends and and colleagues who who provided provided<br />
encouragement and assistance. Making Making science is group group work work indeed.<br />
Finally, Finally, I I thank the the Foundation Foundation for Research Research of Natural Natural Resources in in Finland and<br />
the the North North Karelian Karelian fund fund of of the the Finnish Finnish Cultural Cultural Foundation Foundation for for awarding me a<br />
grant for for the the study.<br />
study.
REFERENCES<br />
59<br />
Aario, R- & Forsström, L., 1978. Koillismaan ja Pohjois-Kainuun<br />
Aario, R. & Forsström, L., 1978. Koillismaan ja Pohjois-Kainuun<br />
deglasiaatiostratigra<strong>fi</strong>a. Geologi 30 (6), 45-53. 45-5 3.<br />
Aario, R. R & Forsström, L., 1979. Glacial Glacial stratigraphy of of Koillismaa Koillismaa and North<br />
Kainuu, Finland. Finland. Fennia Fennia 157 I57 (2), 1-49. L-49.<br />
Aartolahti, T., T.,1972. 1972. On On deglaciation in southern and western western Finland. Fennia 114,<br />
84 p.<br />
Agassiz, L., 1840. Etudes ftudes sur sur les glaciers. glaciers. Neuchatel: Neuchatel: privately published. published. 346 p.<br />
Alhonen, P., 1971. 1971. On On the early Flandrian stratigraphy and vegetational history of<br />
the North North Satakunta area, western Finland. Bulletin Bulletin of of the the Geological Society of<br />
Finland 43 (1), 39-46.<br />
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ISBN 95r-690-628-l<br />
Helsinki 1996<br />
Yliopistopaino