Journal of Coastal Research 811-R16 Fort Lauderdale, Florida Fall 1996 . Late Quaternary Coastal Records of Rapid Changes In the Eastern Baltic!

Anto Raukas

Institute of Geology Estonian Academy of Sciences 7 Estonia Ave Tallinn EEOlOO, Estonia ABSTRACT _

RAUKAS, A., 1996. Late Quaternary coastal records of rapid changes in the eastern Baltic. Journal of Coastal Re­ ,tllllllll:.. search. 12141,811-816. Fort Lauderdale IFlorida I, ISSN 0749-0208. • • In the eastern Baltic area, comprising the countries of Estonia, Latvia and Lithuania, and the St. Petersburg and f!I31l~_W!_--- ...... ~. Kaliningrad Districts of Russia, there are a lot of phenomena suggesting rapid changes in sea level due to different factors. At the end of the Pleistocene, the present-day Baltic Sea was a big Ice-dammed (local Ice lakes) or Ice­ ==;;;; &-&3 influenced (Baltic Ice Lake) lake with complicated water-level fluctuations. The drop of the Baltic Ice Lake at Bilhngen in Central Sweden about 10,300 yr BP resulted in the drainage of 25-30 m. A typical freshwater Ancylus Lake mollusc fauna discovered beneath the brackish water Litorina Sea mollusc fauna in a tectonically rising area near the set­ tlernent of Partsi on the island of Hiiumaa, Estonia, provides evidence of the catastrophic lowering of the water level by at least 25-;30 m at the end of the Ancylus stage about 8500 yr BP.

ADDITIONAL INDEX WORDS: Baltic Sea, Eemian Sea, transgression. regression, sea-level change. Holocene, Late­ glacial.

INTRODUCTION accompanied by an abrupt lowering of the water level. The end of the Baltic Ice Lake and the formation of the Yoldia Rapid changes taking place in natural environments are of Sea are connected with the drainage caused by the recession fundamental importance for better understanding of man-in­ of the ice from Billingen in Central Sweden some 10,300 yr duced processes which should be recognized and managed. BP (SVENSSON, 1991), In Estonia, near Parnu (Figure 1), the Shoreline displacements of the past provide a major key to fall in water level was some 25-30 m (TALVISTE, 1988), The understanding of on-going processes and assist in prediction rapid lowering of the Ancylus Lake level on Hiiumaa Island of changes to be expected in the coastal area in the future. rFigurcs 1 and 2) and in NW Estonia has been estimated at The rather small Baltic Sea poses problems characteristic of 20-25 m (KESSEL and RAUKAs, 1967). After the connection many inland seas. This almost land-locked area of brackish of the Baltic Sea with the ocean at the beginning of the Li­ water (average salinity of surface water only 7-8'/', J. is sep­ torina (Mastogloia I stage, the shore displacement became in­ arated from the ocean by the narrow and shallow Danish fluenced by eustatic sea-level change which, in turn, was con­ Straits and has a very sensitive eco-system which suffers trolled by climate change and tectonic movements. from considerable pollution. On the contemporary coasts of the eastern Baltic, the last Technological developments and the ensuing progress in decades have witnessed remarkable activation of erosion pro­ marine transport were accompanied by a dramatic increase cesses and longshore displacement of sediments has intensi­ in human impact which the Baltic has experienced more than fied. The frequency of extremely strong storms has increased. any other sea in the world. Some changing environments in Storms cause especially great damage on sandy beaches the Baltic reflect global trends, others only local and regional which are least resistant to erosion. In the autumn-winter trends which, nevertheless, are important to compare with period, when the water level is relatively high, storms pile global scale processes. up great water masses and the coastal formations even on The Baltic Sea is a young body of water which formed only the backshure are subject to strong wave activity 10[NIKU some 12,000 years ago rKvxsov and RAlJKAc;. 1971l. In the and GRAN() 1992), Therefore, long-term environmental mon­ early stages of development, the present-day Baltic was a big itoring in combination with research into the past processes ice-dammed (local ice lakes) or ice-influenced (the Baltic Ice in the eastern Baltic area will be of great importance. Lake) body of water with complicated water-level fluctua­ tions. Later it was twice connected with the ocean. This was GEOLOGICAL SETTING OF THE STUDY AREA

The study area, comprising the countries of Estonia, Latvia 95051 received and accepted in ret-ision 30 May 19.95. 1 Contribution to rGCP Project 367: Late Quaternary Coastal Re­ and Lithuania, and the Sf. Petersburg and Kaliningrad Dis­ cords of Rapid Change. tricts of Russia (Figure 1), belongs structurally to the north- 8 12 Raukas

~ 10 km

"' ...... I'''' \1 '''.. "'i_ tta an i .~i - . P::::] 1 \-; .....,...;~ ".. .. L :: E3 ~I uk sn et ..: " · · ~ ~p l an ~"· : ~ 2 ..\:( Figure 2. Ancylus shorelines on the Island of Hiiumaa (NW Estonia): " (1) area above the Ancylu s tran sgression (A.); (2) area above the Ancylus '­r I regression (AVl )...... ~ " .. , .. ~ "'... J \ s~ r" ...... , J ,,/ ...... ,. Jl"V~ -, ,., "1 / ...... oJo.. _ K lai pe da ' ...... ,~./ also encountered (MIJDEL, 1994). The present average rise of r LITHUANIA JSELARUS th e world ocean level does not remarkably affect th e evolu­ '\ -.,. tion of the beaches in th e northern part of th e study area; in f ...... ,. v ...... '\..,.- ...... that area du e to cru stal upli ft (2--4 mm per year), th e coast '" r" - \ 100 km is risin g more rapidly th an th e level of th e world ocean (about r Vilnius. I I I r , 1.5 mm an nually). However, th e sinking southe rn part of th e

Figure 1. Locat ion of the study a rea with th e maximum shoreline of th e study area would be endangered, especially due to acceler­ Ancylus Lak e (A, ). ated sea -level rise resulting from the "greenh ouse effect".

RAPID SEA-LEVEL CHANGES DURING THE EEMIAN INTERGLACIAL western pa rt of th e East-European Platform . The boundary between the Fenn oscandian Shield and the Platform is de­ In th e territory under discussion, th e Eemian period cor­ fined by the northern limit of sedim entary rocks an d it ru ns relates with Stage 5e of th e deep-sea record, which is dated thro ugh the Gulf of Finland. Depending on tecton ical pecu­ roughly between 125 and 115 ka (SHAC KLETONand OPDYKE, liarities, th e bedrock of different age crops out in the form of 1977). Sever al meth ods, including th e counting of an nual lay­ sublatitudinal belts, starting from Vendian and Cambria n ers in fres h-water sediments (MULLER, 1974), suggest th e du­ rocks in th e north (North Estonia ) an d ending with Mesozoic ration of about 10,000 years for th e Eemian interglacial pe­ an d Neogene rocks in the south (Lithuania). In th e territory riod. Fauna and flora rema ins in Eemian deposits ind icate under considera tion, th e distribution of Quaternary sedi­ considera bly higher temperatures during th e intergl acial pe­ ments is controlled by th e composit ion and topograp hy of th e riod compared to those at present. It is generally conclud ed bedrock (TAVAST and RAU KAS , 1982). that sea levels at/o r close to the climatic optimum of th e Ee­ As pa rt of th e vas t East-European Plain, the study area is mian interglacial were 5- 15 m higher tha n nowadays characterized by a flat surface topography with small abso­ (SHACKLETON an d MATTHEWS, 1977). lute and relative heights. The highest point of the area, th e Ther e are two basically differen t viewpoints in the eas te rn Suur-Muna magi Hill (317.6 m), is part of the Haanja Upland Baltic area as regards the conto urs of the Eemian Sea in th e in Es tonia (Figure 1). In th e topography, hilly heights and Baltic depression and the sound s through which it was con­ slightly undu lating plains domin ate. nected with the Atlantic Ocean (RAUKAS, 1991b). Accordin g The sea- level history in the ea stern Baltic regio n has been to GRICHUK (1989) , th e Baltic Sea basin was connec ted with cont rolled by th e unequ al land uplift which has affected dif­ the North Sea via th e Dan ish Straits, th rough th e present ferent areas in differ en t ways. In the northern an d centra l lak e system of Vanern and Malar in Central Sweden and th e regions of th e study area, the ancient coastal formations are area of the current Kiel Canal on th e J utland Penin sul a. Like located several ten s of metres above water level; in the south­ LAVROVA (1961), he ass umes a connection betwee n the Baltic ern part of the a rea, correlative coasta l formations lie a t a an d White Sea basins through the sys tem of sha llow sounds dept h of up to 60 metres below sea level (RAUKAS, 1991a ). and th e lakes Onega an d Ladoga. This means that the tran s­ Severa l sinking and lifting blocks with anoma lous heights are gression of Eemian age must have been synchronous in the

J ournal of Coastal Research, Vol. 12, No. 4, 1996 IGCP :i67 Special Section north of Eurasia as demonstrated by dating techniques, in­ erosion-resistant rocks and deposits, and insufficient time to cluding the ESR-method (MOLODKOV and RAlJKAH, 1988l. form shoreline features. In the shallow basin, waves were According to the second, less established reconstruction, small and their destructive power inconsiderable. There was the contours of the Eemian Sea in the Baltic basin closely not any remarkable longshore drift either which might have coincided with the Litorina Sea limit, and therefore the con­ contributed to the development of large beach formations nection with the ocean could have been via the Skagerrak, (RAlJKAH, 1992). Kattegat and Danish Straits (BLAGOVOLIN et al., 1982). Res­ More information about the water-level fluctuations is olution of the problem concerning the connection of the Baltic available on the Baltic Ice Lake which was formed after the Sea with the White Sea during the Eemian Interglacial is of ice margin had retreated from the Pandivere Upland in principal importance from the standpoint of palaeogeograph­ North Estonia (Figure 1) about 12,000 yr BP (KVASOV and ical and palaeoclimatological reconstructions and study of RAuKAs, 1971) and came to the end when the recession of rapid coastal records. the ice margin from the Central Swedish end moraines re­ In the Baltic Sea, Eemian marine beds are known from sulted in a drainage of the waters at Billingen. The drainage different heights (LnVRAND, 1987). For instance, at Rybac­ took place immediately or shortly after the formation of the koye and Sinjavino in the Neva River Lowland near St. Pe­ Salpausselka II in Finland and can be traced morphologically tersburg in Russia, they occur at a depth of 5-45 metres be­ as a series of marginal deltas 27-28 m below the marginal low sea level; while in the Mga section in St. Petersburg, they deltas formed before the drainage, giving clear amplitudes for are at a height of 10 metres and in the Krasnoretskoye sec­ the extremely rapid shoreline change. As the history of the tion (on the Karelian Isthmus between the Gulf of Finland Baltic Ice Lake in the eastern Baltic area has recently been and Lake Ladoga) 12 metres above sea level. The Eemian summarised in several publications (DONNER and RAUKAs, layers are at their deepest on the island of Prangli (north of 1989, 1992), we shall focus on the somewhat more hypothet­ Tallinn), where they lie at a depth of -61 to -75 m and in ical drainage of the Ancylus Lake. the mouth of the Luga River (-50 to -60 m), Thus great variations in elevations of similar deposits within the same CATASTROPHIC LOWERING OF THE pollen zones may be explained by glaciotectonics rather than ANCYLUS LAKE the sedimentary history, because all the above-mentioned sections are situated in the zone of intensive glacial erosion. The classical theory of VON POST (1928) purports that the Because of the lack of disturbances, completeness of the pro­ Ancylus Lake furiously drained its waters via the Svea River file and low altitudes (LnvRAND, 1991), the Prangli (Figure about 30 m down into Lake Vanern at Degerfors in Central 1) section seems to furnish the best standard for reconstruct­ Sweden, this thesis was later debated (FREDEN, 1979). ing the rapid shore-line changes for the Eemian Sea basin, BJORCK(1987) locates the discharge channels for the Ancylus but such calculations will be complicated due to the difficulty Lake to the western side of Lake Vanern, where two long and of establishing reliable accumulation rates. narrow straits-Uddevalla and Otteid seem to have func­ tioned. By his opinion, these narrow hydraulic dams had act­ FRESHWATER STAGES OF THE BALTIC ed as thresholds which regulated the water level both in the Baltic basin and Lake Vanern, Although alternative successions of Baltic Sea stages have IGNATIUS et al. (1981) subdivided the Baltic offshore sedi­ been suggested from time to time, the present concept of the ments into three main lithological units repeatedly observed development seems to be rather well established. The fresh­ in cores from the different parts of the Baltic Sea: 1) glacial water stages of local ice lakes and the Baltic Ice Lake were varved clays; 2) massive sulphide-rich clays, termed transi­ replaced by the Yoldia stage during which short-term brack­ tion clays; and 3) massive or finely laminated muds with rel­ ish water conditions existed in the western and more or less atively high organic content, termed postglacial muds. The freshwater conditions in the eastern part of the Baltic basin. transition-clay unit is broadly correlative with the Ancylus The Yoldia Sea, in turn, was transformed into the freshwater stage. The deposition of postglacial muds started most prob­ Ancylus Lake. Around 8,500 14C years ago, the Baltic was ably with the establishment of brackish conditions at the be­ reunited with the Atlantic via the Danish Straits (WINN et ginning of the Litorina stage. al., 1986). Since then, all succeeding stages have been ma­ It is difficult to draw the lithostratigraphic and biostrati­ rine, beginning with the Litorina (or transitional Mastogloia) graphic borderlines between the Yoldia and Ancylus sedi­ Sea. ments, at least in the eastern part of the basin (AK~~R et al., The literature dealing with proglacial lakes in the study 1988; HAlLA and RAuKAs, 1992). The boundary between the area is fairly extensive; but, in some respects, all the recon­ transition clays and postglacial muds, on the contrary, is ex­ structions are somewhat hypothetical, as they are frequently tremely well defined and consistent. IGNATIUS et al., (1981) based on the contemporary topography. However, due to un­ consider it as a boundary between the Ancylus and Litorina even neotectonic movements of the runoff threshold, the po­ stages. As the events of the catastrophic outflow of the An­ sition of shorelines has changed beyond recognition since late cylus Lake are absent in Sweden, the question concerning the glacial times. Similarly, one cannot always rely on coastal source of such a great and clear change in sedimentary con­ sediments of ancient lakes which are small in size and often ditions is still open. simply lacking. Pronounced shoreline phenomena are absent WINTERHALTER (1992) explains it with the inflow of saline due to the flatness of topography, the occurrence of relatively water, which caused massive flocculation and deposition of

.Iournal of Coastal Research, Vol. 12, No.4, HJ96 814 Rauk as

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•. , o, p." "" ~ ,? ~ ~c.", • • &> ~~~~• • •' . .~ 40 ~ ~~~~~~, ' , :.~~~~:~ ~ . : " ~~.> 2 " -:: .. .'::.:. <: 50.., 11 10 . . . ' ~",,~~~. :~~~ 1M • •. . ; .~Ir'~ .i1§> o .M4A¥ ~~ '<1 _: : . ~ ': ~ :: ...... :.... : :b~_ ...;... ~. " , ,~'.. ' : . : ~ . .:.. ~ '.~" ..' :: 3 ~ " . ~. · ...,. . ':"'"~~~W-q:" ?&.'i.'>"S'8.l? o@...~...~••• o"o~ <:;6c> ~ ~.~ <::::>~ i~ • •• • . : . .. .. ; ...... ' ''. o ' Figu re 4. Water level cha nges of the Baltic Sea at Kcpu, Islan d of Hiiu­ ~~.o. OO O~Qoo·... oa" .. ~~ .. " ' . . . maa in NW Est onia (1) western Latvia (2) and western Lithuan ia (3) with . ' . ' . I r ... ; ,Gulf of Bothnia fres hwater mollu scs in its lower part (at an absolute height (ERONEN, 1982) and nea r the coas ts of Estonia (KESSELand of 10-14 m) and brackish water molluscs in th e topmost part RAUI

Jo urnal of Coastal Research, Vol. 12, No.4, 1996 IGCP367 Special Section 815

Danish Straits gradually and only a minor quantity of the "Late Quaternary Coastal Records of Rapid Change" and for oceanic water could have penetrated further to the east, the invitation to contribute a paper to this volume. I am where slightly brackish water conditions appeared around grateful to Mrs. Helle Kukk who helped me with the English 8,000 14C yr BP as recorded by littoral diatoms IHYVARINEN language of the manuscript and to Mr. Rein Vaher for draw­ et al., 1992). ings. My travel was supported by the International Science Foundation and research by Estonian Science Foundation SHORELINE DISPLACEMENT DURING THE (Grant No. 326). BRACKISH-WATER BALTIC SEA LITERATURE CITED Since the reunion of the Baltic Sea basin with the ocean at the beginning of the transitional Mastogloia stage, the shore AKER, K.; ERIKSSON, B.; GRONLUND, T., and KANKAINf<:N, T., 1988. displacement has been controlled by two factors: eustatic sea­ Sediment stratigraphy in the northern Gulf of Finland. Geological level change and isostatic uplift. While the former ought to Survey of Finland. Special Paper, 6, 101-117. BJORCK, S., 1987. An answer to the Ancylus enigma? + Presentation be uniform all over the Baltic, the latter varies with regions of a working hypothesis. Geologisha Foreningens i Stockholm For­ resulting in different patterns of shore displacement in dif­ hurullingar, 109, 171-176. ferent areas (HYVARINEN et al., 1992). In the eastern Baltic BLAGOVOLIN, N.S.; LEONTYEV, O.K.; MURATOV, V.M.; OSTROVSKY, area, the rate of uplift broadly diminishes from north to south A.B.; RYCHAGOV, G.I., and SEREBRYANNY, L.R., 1982. Sea basins and shorelines in Eastern Europe in Pleistocene and Holocene.In: and, in the area of the Gulf of Finland, from southwest to Palaeogeography of Europe During the Last 100,000 Years (Atlas­ southeast being at its lowest in the St. Petersburg region. monograph), Moscow; Nauka, 9-15. (in Russian). In the Helsinki area, the isostatic uplift exceeded the eus­ DONNER, J. and RAuKAs, A., 1989. On the geological history of the tatic sea-level rise but in Estonia, transgressive trends pre­ Baltic Ice Lake. Proceedings of the Academy of Sciences of the Es­ vailed in Mastogloia and early Litorina times. The Litorina tonian SSR, 38, 128-137. DONNER, J. and RAUKAs, A, 1992. Baltic Ice Lake. In: RAuKAs, A transgression appears to have culminated at different times and HYVARINEN, H., (eds.), Geology ofthe GulfofFinland. Tallinn: in different areas, so that the peak is delayed towards the Estonian Academy of Sciences, 262-276 (in Russian with English margins of the land uplift zone (KEsSEL and RAUKAs, 19841. summary). In Estonia, the transgression continued until at least 6,000 ERoNEN, M., 1974. The history of the Litorina Sea and associated yr BP; in areas with zero uplift (northern Latvia), the trans­ Holocene events. Societas Scientiarum Fennicae, Commentoiiones Physica-Mathematicae, 44, 79-195. gressive trend most probably continued as long as eustatic ERoNEN, M., 1982. The course of shore displacement in Finland. sea level kept on rising; however, the rapid eustatic rise had Holocene Sea Level Fluctuations, Magnitude and Causes. Columbia probably ceased by about 5,000 yr BP, after which regressive S.C.: University of South Carolina, 43-60. trends in shore displacement became prevalent even in the FREDEN, C.. 1979. The Quaternary History of the Baltic: The west­ ern part. Ada Universitatis Upsalieneis. Symposia Universitatis marginal parts of the Baltic uplift area (HYVARINEN et al., Upsaliensis-Annum Quingentesimum Celebrantis. Uppsala, 1, 1992). Short-term fluctuations in relative sea level have been 59-74. registered in some areas and are considered to be local in GRICHUK, V.P., 1989. The History ofFlora and Vegetation ofthe Rus­ origin. The tides with an amplitude of 1-5 ern are barely no­ sian Plain in the Pleistocene. Moscow: Nauka, 184p. (in Russian). HAlLA, H. and RAUKAs, A., 1992. Ancylus Lake. In: RAUKAs, A. and ticeable, and their geological effect is insignificant. More sig­ HYVARIN~:N, H. (eds.), Geology of the GulfofFinland. Tallinn: Es­ nificant changes in the water level, ranging from 2 to 4.5 m, tonian Academy of Sciences, pp. 283-296. (in Russian with En­ are caused by persistent winds and differences in the air glish summary). pressure. It means that contemporary beach ridges may be a HYVARINEN, H.; RAUKAs, A. and KESSEL, H., 1992. Mastogloia and couple of metres higher above the normal water level and at Litorina Seas. In: RAUKAs, A. and HYVARINEN, H. (eds.), Geology of the Gulf of Finland. Tallinn: Estonian Academy of Sciences, some distance inland from the shore. 296-312. (in Russian with English summary). IGNATIUS, H.; AxBERG, S.; NIEMISTO. L., and WINTERHALTER, B., CONCLUDING REMARKS 1981. Quaternary Geology of the Baltic Sea. In: VOIP[O, A. (ed.I, The Baltic Sea. Amsterdam: Elsevier, 54-104. In the eastern Baltic, there are a lot of phenomena sug­ KESSEL, H. and RAUKAs, A, 1967. The Deposits ofthe Ancylus Lake gesting rapid sea-level changes due to different factors. Re­ and Litorina Sea ill Estonia. Tallinn: Valgus, 134p. (in Russian with English summary). search into those phenomena will be of primary importance K~~SS~:L, H. and RAU KAS , A., 1979. The Quaternary History of the for predicting ongoing processes and future environmental Baltic Sea: Estonia. Acta Universitatis Upnaliensi«. Symposia changes in the densely populated area with advanced indus­ Universitatis Upsaliensis. Annum quingentesimum Celebrantis. try and agriculture. The investigated Partsi section in Hiiu­ Uppsala, 1, 127-146. maa Island allows, for the first time in the Baltic region, the KESSEL, H. and RAUKAs, A, 1984. Correlation of the Baltic ancient coastal formations in Estonia and Sweden. Proceedings of the rate, timing and amplitudes of the Ancylus transgression to Academy ofSciences of the Estonian SSR. Geology, 33, 146-1.';7(in be established with a rather high precision. The high reso­ Russian with English summary), lution studies in the Baltic will promote better understanding KLIEWE, H. and JANKE, W., 1978. Zur Stratigrahie und Entwicklung of the global coastal scenarios. des nordostlischen Kustenraumes der DDR. Pettermanns Geogra­ phische Mitteilungen. 22(2), 81-89. Kvxsov, D.D., and RAuKAs, A.V., 1971. On the Late-glacial history ACKNOWLEDGEMENTS of the Gulf of Finland. Lzuestiya Vsesojuznogo Geographicheshogo Obschestca, 102, 432-438 (in Russian). First, I would like to thank Dr. David B. Scott and Dr. Ian LAvRovA, M.A, 1961. The relation between the Boreal interglacial Shennan for inviting me to the IGCP Project 367 meeting transgression in the north of the USSR and the Eemian trans-

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gression in Western Europe. Trudy lnstituta Geologii Ahudemii liarities of the formation of transgressive coastal deposits. Quater­ Naul: Estonsko» SSR, 8, 74-82. (in Russian with English sum­ noire, 2 (3/4), 126-130. mary). RAuKAs, A., 1991b. Eemian interglacial record in the northwestern LIIVI{AND, E., 1987. Regional type section of the Eemian marine de­ European part of the Soviet Union. Quaternary International, 10­ posits on Suur-Prangli. Proceedings or the Academy or Sciences or 12, 183-189. the Estonian SSR. Geology, 36, 20-26. (in Russian with English RAuKAs, A., 1992. Evolution of Ice-Dammed Lakes and Deglaciation of the Eastern Peribaltic. In: BILLWITZ, K, JA(;ER, K-D. and JAN­ summary), KE, W. reds.), Jungquartiire Larulsch.aftsriiurne. Aht.uelle Forschun­ LIIVRAND, E., 1991. Biostratigraphy 01' the Pleistocene Deposits in gen zwischen Atlantil: und Tienscluin. Berlin: Springer-Verlag, pp. Estonia and Correlations in the Baltic Region. Stockholm Univer­ 42-47. sity. Department of Quaternary Research, Report 19. Stockholm. SIIACKLETON, N.J. and MATTHI';WS, R.K., 1977. Oxygen isotope stra­ 114p. tigraphy of Late Pleistocene coral terraces in Barbados. Nature, MIIIlEL, A., 1994. Geological background of the present regional up­ 268, 618-620. lift anomaly in Estonia. Proceedings 01' the Estonian Actulemy 01' SHACKLETON, N.J. and OPDYKE, N.D., 1977. Oxygen isotopes and Sciences. Geology, 43, 69-80. palaeomagnetic evidence for early Northern Hemisphere glacia­ MOLLER, H., 1974. Pollenanalytische Untersuchungen und Jahres­ tion. Nature, 270, 216-219. schichtcrzahlungcn an der eemzeitlichen Kieselgur von Bispingen/ SVENSSON, N.-O., 1991. Late Weichselian and Early Holocene shore Luhe. Geologische Jahrbuch, A21, 149-169. displacement in the Central Baltic Sea. Quaternary International, MOLoDKov, A. and Ri\uKAs, A., 1988. The age of Upper Pleistocene 9, 7-26. marine deposits of the Boreal transgression on the basis of elec­ TALVISTE, P., 1988. Parnu iimbruse geoloogilise arengu mude!. In: tron-spin-resonance lESR) dating of subfossil mollusc shells. Bo­ MASSO, T. and RATTMiEPI', T. (cds.), IX Eeeti Geotehniha Konoer­ reas, 17,267-272. entsi Teesid. Tallinn: ENSV Riiklik Ehituskomitce, 49-50. TAvAsT, E. and RAuKAs, A., 1982. The Bedrock Relief of Estonia. OI{VIKU, K. and GRANO, 0., 1992. Contemporary coasts. In: Ri\uKi\s, Tallinn: Valgus, 194p. (in Russian with English summary). A. and HYVAlUNEN, H., (eds.), Geology ofth« GulfofFinland, Tal­ W1NN, K, AVEIWIECK, F.-R., ERLENKEusER, H. and WERNEI{, F., linn: Estonian Academy of Sciences, 219-238 (in Russian with En­ 1986. Holocene Sea Level Rise in the Western Baltic and Ques­ glish summary). tions of Isostatic Subsidence. Meyniania, 36, 61-80. POST, L. VON., 1928. Svea alvs geologiska tidsstallning. Soerige» WINTEI{!{i\LTIm, B., 1992. Late-Quaternary stratigraphy of Baltic Geologiska Undersokning, C 347. Stockholm, 132p. Sea sediments. A review. Bulletin of the Geological Society ofFin­ RALIKAs, A., 1991a. Transgressions of the Baltic Sea and the pecu- land, 64(2), 189-194.

Journal of Coastal Research, Vol. 12, No.4, 1996