-Iournal of Coastal Research Charlottesville. Virginia

Holocene Eustatic Oscillations of the Baltic Sea Levell

Va. M. Punning

Institute of Geology Estonia Academy of Sciences Boulvard Estonia 7 Tallinn 200101 USSR ABSTRACT _

PllNNIr--;(;, Y.M., 1~)H7. Holorene eustat ir oscillations of the' Haltic Sea 1('\,eL -lournal of Coastal UI'....warch , ;l\ ..0, ;)or)-;) 1;1. Charlot tesvill«, ISSN 07 4 ~)-O~()H. ~ ~""""., Geochronolog-ical, hiost.rut.igraphic and g'eomorpholog-ical researches have heen used to . refine the Holocene northern Baltic territories ofthe USSR. The Baltic Sea coast over this ••• • ••• epoch has been characterizcd by neotectonic movements, so that without knowledge of relationships hetween vertical movement rates ofcrustal motion and custatic oscillations it is difficult to conduct inter-reg'ional correlations. To determine the eustatic curve for the Baltic the author assumed the rate of long-term (inherited) vertical movements in the past ]O,()OO ycars to he constant, and on this basis g-lacioisostatic uplift curves were plotted. The Baltic eustatic curve sug-g-csts a progresaive alternation of transgressive and reg'ressive conditions for reg-ions with different ~lacioisostaticuplift g'radients. In the early and middle Holocene time there are four rrunsgrossive/rvgrcsstve cycles (9,700 - 9,000,9,000 -7,900, 7,900 - 6,700 and 6, 70() - 5,600 14 C yr BP) have been identified which can be co rrelated with the Yoldia, Ancylus and two Littorina stages. The height of the Aneylus Lake level was nearly 16 m above the world ocean level. The proposed eustatic curve for the Baltic is used t.o make int.erregion al corr-elations.

AJ)J)ITlONAL INDEX WORDS: nalf/c Sea, custotic ()s('l!latioT/.\ Holocene, scu It'['l'!.

INTRODUCTION FARRELL and CLAHK, 1976), testifying to a very complex distribution pattern of melt water in the The problem of world ocean level oscillations has world ocean and emphasizingthe necessity of study­ been attracting a great deal of attention in the past ing regional eustatic oscillations in different parts decades. A successful solution of this problem would of the world ocean and in the seas linked wit h it, par­ enable a better understanding to be reached of the ticularly the Baltic. intricate processes of development and decay of Discoveries of coastal land forms at various ele­ Pleistocene continental glaciers, as well as the dy­ vations, associated fossils and buried lagoonal and namics of present glaciation. Geomorphological lacustrine-swampy depsits have made it possible and radiocarbon data have been used to plot dozens for the entire Baltic Sea coast to be integrated on of curves of eustatic level oscillations either for the the basis of geomorphologic, biostratigraphic and world ocean or individual seas during the past 10­ geochronological researches into a systematization 15,000 years. All these curves fall essentially into of the geological history of the basin. However, two groups: those exponentially approaching the these studies have also revealed the intricate de­ present level and the oscillatingones characterizing velopment of the basin and some of the difficulties short-term regressions, against a background of an involved in reconstructing eustatic sea level oscil­ overall rise and a temporary rise above the present lations for the area. The works of HAUSEr-.; (19:t1). level in the second half of the Holocene. RAMSAY (1929), SAIJl{Al\10 (19:19), ORVIKlT (1960, Many new factors have lately come to light (e.g 1969), KAAIUAINEN (1966) and many others have helped to work out and elaborate concepts on late 1Editorial Note: Wi' ore pleased to publish the J..:nJ{lish ucrsion o] and postglacial crustal movements in the eastern papers presentedat the 19<'12 INQUAS.vmposium (Shorelines Com­ Baltic. However, because of differences in the mission) held in Moscou: Russian rrrsion« uvr« prci-iousl» published intensity and sign of these movements it was in collection hy Naukannd Moscow Staio Uniivrsitv publishers: This papa INlS kindly edited b.v RW Fairbridue. J)epartml'nt of(;('o!ogico! impossible to identify the component of eustatic Science. Columbia Uniocrsitv. Nell' "t'orh, NY' IOU2?, us« oscillations. 506 Punning

Geochronology ofthe early Holocene Baltic in ruled out that the deposits in south-western Estonia the USSR's northern Baltic territories previously dated by us as Echineis stage (KESSEL and PUNNIN(i, 1969b) in reality were formed in a The primary task for establishing eustatic oscil­ regression of the Yoldia Sea. lations in the basin involves geomorphological and About 8,900 years ago, due to (isostatic) land biostratigraphic identification of individual indica­ uplift, a linkup between the Baltic and the world tor levels and their accurate referencing to the time ocean in the Degerfors area in the middle part of scale. As a result of many years of research (KESSEL Sweden was interrupted (OLSSON and FREDEN, and RAlJKAS, 1967; PUNNING, 19{)9; KESSEL and 19(9) which created the Ancylus lake in the Baltic PlTNNING, 1969a, b: 1974, 1976) it is now possible basin. The water level in the closed basin was rapidly to reconstruct the development history of this part rising due to intensive thawing of the ice sheet. of the Baltic basin. Lithologic- geomorphological researches were used In front of the retreating continental ice margin as a basis for clear identification of coastal for­ separate proglacial lakes formed in depressions of mations of the Ancylus lake at numerous places in the basin. Upon liberation from ice on the Slupsk western and northern Estonia, which in contrast to Bank, the eastern coast of the Gulf of Riga and the the Yoldian or the Echineis formations have been northern slope of the Pandivere l lpland, these pro­ dated with respect to typical freshwater molluscan glacier lakes were able to join up with the main fauna and a diatom complex. The maximum level of Baltic glacial lake (KVASOV, 1975). After the retreat the Ancylus lake transgressive phase in northern of the ice from the Bilingen ridge in the middle part Estonia, in the vicinity of Tallinn, is 37 ill higher of Sweden at about 8.01.5 Be (NILSSON, 1968). sea than t he present sea level. Serving as datum points water found its way into the Haltic and this was the in northern Estonia are also lagoonal sapropels in beginning of the first Holocene marine stage, known the Kakhala (8.595±75, 'fa-59) and Yulemiste as the Yoldia Sea. Yoldia Sea deposits have heen (8,400±90, Ta-(91) areas. traced solely within a narrow coastal strip. On the The age and length of the Ancylus stage, as well basis of a few data principally obtained in south­ as its culmination time have been determined by us western Estonia, the length of the Yoldian stage by dating the organogenic deposits occuring in the was estimated by us to have lasted 700 years (from Ancylus lagoons or buried beneath Ancylus coastal 10.nOn to 9.300 yr BP) with the transgression cul­ Iormations (KESSEL and PUNNINC, 1969 b, 1974). minating from 9,700 to 9,500 yr HP (KESSEL and In numerous sections both for the northern and PUNNING, 19(9). western Estonia we have dated buried peat bogs However, a new dating of a lagoonal sapropel where sedimentation had discontinued on account from the Syyamyagi swamp near Tallinn raises cer­ of lake transgression 8.HOO - 8,400 yr BP. In an tain doubts as to the trustworthiness of these con­ overgrown lagoon (lyelyakhtme) near Tallinn, sap­ clusions. A complex of lagoonal sapropels at 42 m ropels ceased to accumulate 8,260±70 yr BP elevation, according to Pork's data (KESSI<:L and (Ta-272) and peat formation commenced. About PORK, 1971) contains in its bottom part a brackish­ 8,000 yr BP peat formation had begun over a wide water to freshwater diatom flora which is replaced emerging strip both in the Leningrad area and in in the upper part by freshwater to lacustrine facies. northern and western Estonia. On the evidence of This means that sedimentation had started in a all data com bined the cu lmination of the Ancylus lagoon which was converted later into a coastal lake. transgression in this region took place between The age of lagoonal sapropels, 8,91f)±90 yr BP R,400 and 8,2()() yr BP. (Tln-I:35), permits us to establish the tirne when the The Ancylus Jake regression continued until level of the regressive Baltic was at a level now 7.600 yr BP when there was apparently a minor elevated to 42 m in height. transgression in the transition time between the It is to be noted that no unambiguous radiocar­ Ancylus and Littorina stages. Deposits of this trans­ bon datings permitting a boundary of the Yoldia gression have so far been established by us only in Sea to be dated with greater accuracy have so far single section in southwestern Estonia. In the Kolga been obtained from any other area adjoining the section Kessel has indentified a brackish-waterflora Baltic basin. The absence of molluscan shells in off­ of diatoms characteristic of the Mastogloian stage shore deposits and a low salinity (1-2 0/ 00) of water (KESSEL and PUNNINC, 1969 b). The radiocarbon in the basin likewise add to the difficulty of identify­ sapropel age, viz. 7,505± 165 (Ta-126), tentatively ing datum deposits of the Yoldia Sea. It is not to be yields also the time of transgression culmination.

.Journal of Coastal Hesearch, VoL :L No.4, HHn Holocene Ellstat ic Oscillations in Baltic Sea 507

The height of the respective coastal forms extrap­ inference has been drawn by numerous research­ olated for the territory of northern Estonia, 22m, is, ers studying the movement of the Baltic shore­ however, in good agreement with the heights of lines (KESSEL and MIJDEL, 197:1; ERONEN, 1974; indicator lines of early Littorina transgressions. M()J{NEH et al., 1976). The progress of the Littorina Sea has been studied Figure 1 shows water level indicators for north­ by us in the Leningrad region, Estonia (KESSEL, ern Estonia (Tallinn area), dated by the radiocar­ PUNNING. 1969b, 1976) and Lat via ((;RIN BE R(~S et bon method. In the early Holocene there are la­ al , 1975). Depending on the rate of vertical crustal goonal sapropels, and in the middle and late movements, the highest Littorina Sea shorelines Holocene there are coastal forms, corresponding to are of different ages, so that studies at sites wit h dif­ the successive culminations of development phases ferent neotectonic gradients have made it possible of the Baltic. The rate of present uplift in the to identify and date four transgressive phases. In Tallinn area is 2.!) mm!yr(ZHELNIN, 1~}64). Extrap­ northern Estonia a transgression culmination was olating this rate to 1,000 years back and separating dated6,900 yrBP, in southwestern Estonia the cor­ the respective values from datum level heights, we responding phases were dated G,400, 6,000 and obtain a "'reduced" spectrum. The heights of the 4,700 yr BP. The respective coastal formations in specific" reduced" shorelines depends on the posi­ northern Estonia lie at absolute elevations of 2:~, tion of the Baltic level with respect to the present 21,20, and 1~3 m, and in the southwest at6 - H m one at the moment offormation of the coastal form elevations (KESSEL and MIIDEL, 197:q. or the accumulation of lagoonal deposits and a total During the Limnia stage the Baltic Sea had a glacioisostatic uplift of the area concerning until the regressive character. Until today we have suc­ present time. ceeded in confidently dating on ly one of its develp­ The results of radiocarbon dating of specimens ment stages about 4,000 years ago. The COITes­ from old coastal deposits in tectonically stable ponding coastal deposits in northern Estonia reach platform areas indicate that the ocean level follow­ an elevation of about] 2 m above sea leveL ing the retreat ofcontinental glaciers was rising in a fluctuating manner with an alternation of long Changes in the level of the Baltic basin transgressive periods and short-term regressions. Particularly informative among these curves are After fifteen years of research activities we have the ones proposed by FAIHHHII)(~E (1971, 1976), succeeded in achieving a fairly confident dating of M(")J{NEf{ (1976), TERS (197;3) and TOOLEY (1974). about 10 development phases ofthe Baltic basin in All these curves are based on abundant factual the Holocene, each having corresponding coastal material and therefore discrepancies between them formations characterized by biostratigraphic and can only by explained away by the effect oftectonic geomorphological methods. movements that are not easily accountable. Fair­ In rather early studies (HAllSE0J, 19 I :~; RAMSAY bridge's curve appears to our mind to be par­ et al , 1929) it was already shown that the central ticularily valid, especially for the interval of 12,000 and southern parts of the Baltic shield were subject - [),OOO years ago. Multiple transgressions above to vertical movements in the post-glacial time, the the present level in the second half of the Holocene total amplitude of the movements decreasing south­ are denied by numerous researchers. Eustatic os­ wards (KAAJ-uAJNEN, ]966; NIKOLA,JEV et al , 1967). cillations in 1he Baltic are expected to be syn­ Neotectonic movements are, as a rule, sub­ chronous with the world ocean oscillations, except divided into two components (OHVIKll, 1960); an for the Ancylus lake which was isolated from the inherired type and a glacioisostatic one, t he latter world ocean. It is to be noted that undertaking the being due to the removal of the glacial load and the reconstructions we also tried other eustatic curves, restoration of the original state of strained astheno­ hut we found Fairbridges to be in agreement with sphere. The Baltic shield and the adjoining East­ our data. European platform are relatively stable tecton­ Fairbridges eustatic curve is shown in Figure 1. ically. Apart from wave-like glacioisostatic move­ At present all requisite data are available for cal­ ments, this region is subject to a tectonic regime culation of the total glacioisostatic uplift with ref­ inherited from the Paleozoic. It appears that the erence to different moments in time. The points in inherited tectonic regime set up in the Holocene has the figure, obtained bv summing up the heights of not essentially changed and, therefore, this compo­ reduced sign levels and the respective world ocean nent may be assumed approximately constant. This levels with an opposite sign, give the magnitudes of

.Iournal of Coastal Research, Vol. :~. No.4. 19H7 Punning

IJ.M 50

50

'1O

30

20 to

0 - to 8 -20

-30 of -2 03

Fig-lin> 1 f-{p('on:-;I !"lid ion of a glacioPllst at ic uplift for nort hern Estonia ~ Tallinn). 1 sea 1('\'('\ indicators (principallv 11('-dated lagoonal dr-pns it s: :z ---- n·du('pd :-;ealovo l indicat OI'S(cakulat pd mag-nit udes of inherit ('

.Iournal of ('o(i:-;Ial I{PSPi:u'('h. Vol. :l, ;'\Jo. -1. I !IK7 Holocene Eustatic Oscillations in Baltic Sea [)()9

197~l). latter in the first approximation being compared 11t > h, (KELLY, This means that a relative with the present one, and the parameters of the difference between h, (true) and ~ (observed) rises glacioisostatic curve. For the latter to be described with a decrease in residual decompensation, and more adequately, we give this curve for northern the practical utilization of the curve appears to be Estonia in the semilogarithmic system of coor­ feasible until 7,000 or 6,000 yr BP. dinates (Figure 3). We obtain a straight line de­ Figure .l shows glacioisostatic rise curves for ter­ scribed by the equation 19h, = kt 19h., where ho and ritories with a large uplift gradient (southeastern h, are, correspondingly, the magnitudes of com­ Finland, northern Estonia, Saaremaa Island) and plete compensation relative to the moment of re­ small one (southwestern Estonia, southern Sweden). moval of loading (to) and of residual compensation The plotting of the curves is based on datings of at the moment of time t (t is a time interval in lagoonal sapropels (PUNNING, 1968: BERGLUND, thousands years from the zero- moment). To be able 1964; ERONEN, 1974,1976); the rates of inherited to plot such curves it is sufficient to have two dated lift in the reconstructions were assumed to be the coastal forms or lagoonal deposits marking the eleva­ following: southeastern Finland (Helsinki) - ;~.O tion of the sea level in the past with respect to the mm/yr(ERONJ<~N, 1974); northern .Estonia (Tallinn) present level. The fact that practically all values of - 2.5 mrn/yr; Saarernaa 1.- 2.0 mrn/yr; southwestern residual compensation obtained (see Figure 2) lie on Estonia (Pyarnu) - 1.1 mm/yr (ZHELNIN, 1964); the straight line in Figure J is another evidence for and southern Sweden - 1.4 mm/yr (BEHCLlJND, the validity of the proposed eustatic curve for the 1964). Baltic Sea. It is to be noted that because of incom­ 'I'he k values decrease from -0.[)6 in the Helsinki = c-- kt plete compensation the formula h, ho in area to -0.14 in the Blekinge, which is quite under­ ~= kt reality converts into ho c- .in this case K> k, if standable (in terms of former ice coverage).

h,M

50

50

'1O

30 2 to f

10

0

-10

-20

-30

-'10

Figure 2. Shoreline displacemerus in northern Estonia and sout he ast ern Finland. a -eust.atic curve for the Baltic; b-- -calculated shorelines; I-Tallinn; ~- Helsinki.

.lournai of Coastal Hesearch, Vol. ;~, No.4, 19H7 r)}O Pllnning

I 10 .9 8 7 5 5 f J z 1 a {)(tO~m

Figul'p :L (;Iaciof>u:-;tat ir uplilt CllI'V('~. 1 Tallinn; ~ Hr-l sinki.'! Pvarnu: 1 Hlekingp.

Relationships between the rates of water level water conditions prevailing in t he basin during rise in the basin and of total tectonic uplift in any the change-overs of marine-to-lacustrine-t 0-marine region enables us to reconstruct the change-over of condit ions. regressive and transgressive phases for t he given Conditions of formation of coastal landforms, region. If d-E/ ell" > 1, this J11eanS that the given marine and continental deposits at any specific territory was flooded, whilst in t he case of dEl dT' < moment in time' are different, being dependent on 1 there existed conditions favourable to the forma­ the' dEld'I' rat in which is det ermined by the neotec­ tion of lagoons and their conversion into coastal tonic characteristics of the site concerned. lakes or to the formation of coastal landforms under It is well known t hat individual phases in the Lit­ short decelerations or regressions (dEl d'T = 1). torina st age in different parts ofthe Baltic are meta­ The values of dE can he found from the eustatic chronous. As seen from Figure 4. the smaller the curve for the Haltie Sea and d'T can he calculated magnitude of isostatic uplift curves (see Figure :3), from t he formula T = h, + fro' where is t he rat p of Lc. t he less t he magnitude of compensat ion, the present vertical movement. earlier hegin all transgressions, a relatively slow Figure 4 gives the dE/dT relutionships for 200­ transgression being replaced by a very sharp re­ year periods for different regions. (~uite prominent gression. Preslimablv, it is these principles (par­ are four transgressive periods common to all inves­ t icularilv t he large differences in t he beginnings of tigation points. I{(}gression in- between t hem per­ the transgression in the 1st and ;~ I'd cycles) that mit U~ to divide the early-middle Holocene history underlie the dist inct ive identification of'the Echineis of t he Halt ic Sea basin into four transgressive­ and Mastogloian stages in certain areas of the regressive cycles: 9,700 - 9.000, 9,()()() - 7.90(), Haltic. () hviouslv, these local transgressions can­ 7.900 - f),700, (),700 - f>,HOO years ago. As to time, not provide a basis for identifying independent they can be correlated with the Yoidian, Ancvlus stages in the development of the entire basin. and two Littorina stages, transitional semifresh- The eustatic curve for the Baltic Sea significantly

.lournal of Coast a] ({cs{'aJTh, Vo!. :1, !\(I. 1. 1~H"I Holocene Eustatic Oscillations in Halt ic Sea 511

de. dT 20

~ ~ ~ f\S ~ 10 ~

"J f ,2 iJ(IOJJ~m

-to ~ ~ ~

-20

Figure 4. Transgressive-regressive cycles in different Baltic rpgions. 1- -Helsinki; 2- Tallinn; :~-- -- Pyarnu; 4 - - Rlekinge. simplifies interregional correlations. Identification sea level with respect to the present one. of individual stages or phases with respect to bio­ Figure 2 shows the reconstruction of shoreline stratigraphic features involves great difficulties. displacements in northern Estonia and southeas­ since characteristic parameters of the water in the tern Finland. The latter region has been minutely basin, such as temperature and salinity, were studied by EnONEN (1974. 1976), resulting in the changing rather slowly. Furthermore. initially, im­ reconstruction ofa shoreline curve (ERONEN, 1976) portant differences were arising first of all between (see Figure 4) which is to a certain extent different the main basin and its bays or lagoons. Strati­ from that obtained by us (see Figure 2). To calcu­ graphic comparisons with respect to deep-water late the glacioisostatic uplift, we employed the ac­ deposits involve particular difficulties because of cumulation ages of the upper and lower sapropel intermixing of differently-aged deposits. layers in the Hangassuo section (ERONEN, 1976). It Knowing the heights of two dated indicator lines should be noted that data obtained in studying this and the rate of present vertical movement for the section were also employed by Eronen. but he he­ territory concerned, we can easily reconstruct the lieves that a peat had been deposited beneath it. In spectrum of shoreline levels by using the formula H, our opinion, such an assumption is not sufficiently = tT0 + h, - E, where H, is the height of shorelines valid, particularily because in dating basal layers of with respect to the present sea level; To is the rate of peat bogs we often obtain as excessively old age due vertical movement at the present time; t- is time; to the"hard-water effect" A younger age for the h, is residual compensation; and E is the height of Preboreal transgression is evidenced. moreover, by

.Iournal of Coastal Research, Vol. :L No.4, HlH7 Punning

the dating of basal layers in the Haapasuo swamp, BERGLUND, B. E., 1964. The post- glacial shore dis­ 80 - 90 km southwest of Hangas suo swamp (ERO~EN, placement in eastern Hlekinge, southeastern Sweden. T (Series C). 119B. 1976, 1964). sc: ERONEN. M., 1974. The history ofthe Littorina Sea and In southern Sweden, in Blekinge, HEHCLllND associated Holocene events. Commentaries in Physics (1964) studied buried lagoonal deposits at Serevika and Mathematics (Helsinki), 44( 4). . and Hallarumsa sites. The deposits contain as un­ ERONEN, M., 1976. A radiocarbon-dated Ancylus trans­ questionably Ancylus-Lake diatom flora, their age gression site in southeastern Finland. Boreas, os. being dated from buried pine stumps. On the basis FAIRHRIDGE, R. W .. 1961. Eustatic changes in sea level. In: I'hvsi:....· and chemistry oj"the Earth VolA. of these materials Berglund dated the Ancylus stage FAI HHRID(;E. R. W .. 1976. Shellfish-eating precerarnic from 9,800 to 8,000 years ago. However, it seems lndians in coastal Brazil. Science, 191. evident that the wood remains are redeposited and FARHELL. W.E. and CLARK, .J.A., 197{). On post­ their age cannot reflect the true existence time of glacial sea level. Geophvnical Journal ofthe Royal Astro­ the lagoon. nomical Society: 46. CRACHOV, A.F. and DOLUKHANOV, P.M., 1970. Post­ In the southern Baltic KOLP (1974) indentified glacial uplift of the earth's crust in Canada and Finno­ some submarine terraces and correlated them with scandia according to radiocarbon datings. Baltica. 4. certain stages in the development of the early Baltic IIn Russian] Sea basin. Although in the Holocene the O-isobase (;RINHERCS. E.F.; KESSEL, K.YA.: PUNNING, VA. M. K. and RAYAMYAE, R.A.. 197fJ. Application of of this locality drifted (EHONEl\;, 1~)7 4) and it is dif­ radiocarbon filet hod to st udying old- Baltic transgres­ ficult to reconstruct the magnitudes of tectonic sions in Latvia. In: The Status ofMcthodological Studies movements, we believe that establishing relation­ in the Field ofAbsnlut« (;eochroflology. Moscow: Nauka ships between terrace formation ages and the time Pu hlishers, IIn Russian] scale, as done by Kolp, is not sufficiently valid. The HAUSEN. B.. 1~)7:L Crber die Entwicklung del' Ober­ recent dating 9, ;j60± 110 yr HP (TIn-S 18) wit h res­ flachenformcn in den russischen Ostseelandern und an­ grenzenden Gouverments in der quartarzeit.. Fennio; pect to organogenic deposits from a core near the :l4(:l). island of Rugen from about 21 m depth indicates KAARIAINEN. E .. UH)(). Land uplift in Finland com­ that identification of a Yoldian terrace at 60 m puted wit h t he aid of precise levellings. Annale» Aca­ depth (KOLP, 1974) appears to be premature. dcmiac Scientarium Fcnnicae (Series A). 111(90). KE LLY. M .. 197:L Radiocarbon dated shell samples from Nordresrromfjord, West Greenland, with com­ CONCLUSION merits on models of glaci(}-isostatic uplift. Grenlands Undcrsauel.«, 1)9. The eustatic curve for the Baltic Sea obtained by KE LNIN, C. A., 1D64. Accuracy and potentialities of the us for the late Holocene is not yet sufficiently ac­ rnet hod of repeat eo levelling. In: Modern and Latest Crustal Mooemcnt» in Hallie Areas. Vilnjus. [In Russian] curate. Its refinement requires very accurate indi­ KESSEL, H.YA. and MlIDE L, A., 197:~. On late- and cator lines, since the oscillation amplitude of the post-glacial crustal rnovement in Estonia's territory. sea level in this time interval was relatively small. lzivstiva Aleadcmii Nau» Estonia SSR Seriya Khimi­ 'rhus, with the help of the proposed eustatic curve cheskava (;eolo~i.V(J. ~2(;~). for the Baltic we can make corrections in datings of KESSEL, I-l.YA. and PUNNING. YA.M.K., ]969. On dist ribut ion and stratigraphy of Yoldian Sea deposits in deposits, carry out interregional correlations and Estonia's territory. Izvesti.l'(] Akadenlii Nauh Estonia correlate individual shorelines for the entire Baltic. SSH Scriv« Khimicheshava Geologiyu; 18(2). If the spectrum of coastal forms has been clearly KESSEL, H. YA. and PUNNING, YA.M.K., 1974. On the identified by means of biostratigraphic, geomor­ age of the Ancylus stage in Estonia (from radiometric data). Lzucstiva A ho dcmii Nauh E ... tonia SSR Seriya phologic and radiologic methods, it becomes pos­ Khimichcshriyu (/eolof.?l:ya. 2:l( 1). sible to specify the magnitudes of neotectonic KESSEL, H. YA. and PUNNING. VA. M. K., 1976. On the vertical movements. age of the Littorina transgression in the Leningrad region. Izrestiya Aluulcmii Nauk Estonia SSR Seriya Khimicheshnya (;eol()~iya. 2f)(;~). LITERATlJRE CITED KESSEL. H.YA. and RAllKAS, A.V., 1967. Coastal 1)eposits of the Ancylus Lake and Litiorina Sea in ARTYlJSHKOV, E. V., 1967. On establishment of the Estonia. Tallinn. isostatic equilibrium of the earth's crust. Fizika Zemli KOLP. 0., 1974. Submarine lTferterrassen in der sud­ (Physics of the Earth), 1. [In Russianj lichen Ost- und Nordsec als Marken eines Stufenweise BERGGVIST, E.. 1977. Post-glacial land uplift in north­ erfolgen Holozanen Meeresansteigen. Baltica, 5. ern Sweden: some remarks on its relation to the present KVASOV. D.D.. 197f). The Late-Uuaiernary History of rate of uplift and the uncompensated depression. Gco­ Eastern Europe's Major Lakes and Inland Seas. Moscow: logislu: Foreninuens i Stockholm Forhorullinuar. 99. Nauka Publishers. [In Russian] Holocene Eustatic Oscillations in Halt ic Sea

MORNER, H.A., 1976. Eustatic changes during the Movements, Volcanism and Earthquakes in Continents last 8,000 years in view of radiocarbon calibration and and Ocean Floor. Moscow: Nauka Publishers. ITn new information from the Kattegat region and other Russian] northwestern European coastal areas. Palaeo­ PUNNING, YA.M.K.. 1969. Applying radiocarbon method geography, Palaeoclimatology and Palaroccolouv, to the study on the history of sheet glaciation in the 19. Upper Pliestocene and of the evolution of old-Baltic NIKOLAEV, N.I.: BAHAK, V.1. and MEKYANTSEV, water reservoirs in the early and middle Holocene on the A.I., 1967. Some neotectonic problems of the Baltic Baltic territories. Thesis, University Department of Shield and the Norwegian caledonides. Baltica, (:q. Geology and Mineral Sciences, Tallinn. NILSSON, E., 1968. Sodra Sveriges s enkvartara historia. RAMSAY, W.. 1929. Niveauverschiebung, eisgestaute Geokronologi, issjoar och landhojing, Kunglige Veten­ Seen und Recession des Indlandeises in Estland. Fen­ skapsahademi (Fjarde Serie), 12(1). nia, 52(2). OLSSON. I. U. and FREDEN, C.. 1969. Radiocarbon SAURAMO, M., 19:19. The mode of the land upheaval in measurements from the Degefors area, Sweden. Geo­ Fennoscandia in late Quarternary time. Pennia, 66(2). logiska Foreningens i Stockholm Forhandlinuar, 91. TERS, M., 197~. Les variations de niveau marin depuis ORVIKU, K.K., 1960. On neotectonic movements in 10.000 ans, le long du littoral atlantique francais. In: Le Estonia on the basis of geological data. In: Neotectonic Quaternaire G{'odynamique, Stratigraphie et Environ­ Movements in Baltic Areas. T'artu. ment. Commission National Francais INQtJA. ORVIKU, K.K.. 1969. The effect of crustal uplifts on the 1'OOLE Y, M., 1974. Sea-level changes during the last geological- morphological development of Estonia's ter­ 9,000 years in northwest England. Geographical Jour­ ritory in post-glacial time and in the Holocene. In: Latest nal; 140.

o RESUMEN 0 Investigaciones geocronologicas. hioestratigraficas y geornorfologicas han permitido precisar las zonas holocenas de la URSS en el Norte del Mar Haltico. Durante ese periodo esta costa se caracterizo pOI' movimientos neotectonicos, de tal forma que para obtener correlaciones interregionales es necesario conocer la relacion entre las tasas del movimiento verti­ cal de la corteza y las oscilaciones eustaticas. Para determinar la curva eustatica del Mar Haltico el autor supone que la tasa a largo plazo del movimiento vertical en los ultimos 10.000 anos ha sido constants, dibujando con esta base las curvas ascenso glacioisostatico, Las curvas eustaticas del Mar Baltico sugieren una alt ernancia de regresion y transgresion para regiones con diferente gradiente ascensional glacioisostatico. En la primera e intermedia epocas del Holoceno se han encontrado cuatro ciclos transgresivos/regresivos (9.700 - 9.000; 9.000 - 7.900; 7.900 - 6.700; 6.700 - 5.600) antes de la epoca actual los cuales se han correlacionado con los estados Yolida, Ancylus y dos Littorina. La amplitud del nivel del agua en ellago Ancylus estuvo aproximadamente 16 m POl'encima del nivel del oceano. La curva eustatica propuesta se ha utilizado para establecer correlaciones interregionales.--Miguel A. Losada, Unioersidad de Cantabria. Santander, Spain

o ZUSAMMENFASSLJNG 0 Geochronologische, biostratigraphische und geomorphologische Forschungen wurden durchgefuhrt., urn die Holozan­ kuste del' auf dem Ostsee liegenden UdSSR-Gehiete hessel' zu bestimmen. Die holozane Ostseekiiste zeigt neotek­ tonische Merkrnale: est ist dann notig, eine Kenntnis del' Beziehungen zwischen vertikalen Bewcgungsverhaltnisse del' krustalen Bewegungen unfeustatische Schwingungen zu haben, urn interregionale Wechselbeziehungen zu durchfuhren, Urn die eustatische Kurve des Ostsees zu bestimmen, wurden die Verhaltnisse del' langfristigen (geerbten) vertikalen Bewegungen del' vergangenen 10.000 .lahre konstant angenommen zu sein; glazioisostatische Kurven wurden dann eingezeichnet. Die eustatische Kurve des Ostsees schlagt eine zunehmende Ahwechselung der uberschreitigen und ruck­ laufigen Umstande in Gebiete mit verschiedenen glaz ioisostatischcn Aufschwungskurven VOl'. Wahrend del' Fruh- und Mittelholozanzeir wurden vier uberschreitige/rucklaufige Kreise (9.700 - 9.000, 9.000 - 7.900,7.900 - 6.700, und 6.700­ 5.600 14C Jahre BP) ident.ifiziert, die mit den Yolida-, Ancylus- und zwei Littorina-Stufen in Wechselbeziehung hringen lassen. Das Ancylus- See- Niveau stand 1H m holier als dem heutigen Meeresspiegel. Interregionale Wechselbeziehungen werden mit del' vorgeschlagenen Ostsee- Kurve benutzt.--Stephen A. Murdock, CERF, Charlottesville, Virf.tinia, llSA

o RESUMB: 0 Les donnees de geochronologie, biostratigraphie et geomorphologie mont.rent que la mer baltique etait caracterisee par des mouvements neotectoniques a I'Holocene. Sans connaitre les relations entre Ie mouvement vertical de la croute terrestre et les oscillations eustatiques, il est difficile d' etablir des correlations inter-regionales. Pour determiner la courbe eustatique de la Haltique, les mouvements verticaux along terme (herites) des derniers 10.000 ans sont supposes constants. La courbe de la montee glacio-eustatique est adjustee sur cette base. La courbe eustatique suggere quil y a une alternance progressive de conditions rransgressives et regreasives pour chaque region, avec des gradients de montee glacio-eustatique differents achaque fois, Au debut et au milieu de l' Holocene, on denombre quatre cycles transgression! regression (9.700 - 9.000, 9.000 - 7.900,7.900 - 6.700 et 6.700 - .s.600 avant nos jours). lis peuvent etre correles avec les etages de Yolida, Ancylus et deux de Littorina. La hauteur de niveau de I eau du lac d'Ancylus etait environ a16 m au dessus de celui de la mer. La courbe eustatique proposae pour la Haltique est utilisee pour faire des correlations entre regions.>- Catherine Bressolier, EPHf;, Montrougr, France tfllffflp:. ~

-Iournal of Coastal Research, Vol. ;{. No.4, 19k7