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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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Virkkala, K., 1963. 196i|. On ice-marginal ice-marginal features in southwestern Finland. Bulletin de<br />

la Commission geologique g6ologique de Finlande Finlande 210, 2L0, 1-76.<br />

L-76.


ISBN 95r-690-628-l<br />

Helsinki 1996<br />

Yliopistopaino

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