Geo log i cal Quar terly, 2002, 46 (2): 165–188

The maxi mum ice sheet limit of the Vistulian Gla ciation in northeast er n Poland and neighbour ing are as

Tomasz KRZYWICKI

Krzywicki T. (2002) — The maxi m um ice sheet limit of the Vistulian Glaci ation in northeast ern Po land and neighbour ing areas. Geol. Quart., 46 (2): 165–188. Warszawa.

This paper outlines a new ap proach to recon struc ting Vistulian ice sheet limits in NE Po land and ad jacent areas of Lithu ania and Belarus. It is based on geo logi cal in vesti ga tions of land forms and depos its either of a hypo theti cal boundary to the Vistulian ice sheet limits. The main con clu sions are: 1 — the area was cov ered twice by the Vistulian ice sheet; the first time dur ing the Świecie Stadial (67–50 ka BP) and the second time during the Main Stadial (24–12 ka BP); 2 — the limit of the older stadial was farther to the south a that of the youn ger one; 3 — due to cover ing of the Eemian sed i ments by the ice sheet of the Świecie Stadial the limit of the Vistulian Gla ci ation has moved about 15–20 km southwar ds.

Tomasz Krzywicki, Pol ish Geo log i cal In sti tute, Rakowiecka 4, 00-975 Warszawa, Poland, e-mail: [email protected] (receiv ed: June 13, 2001; accepte d: De cember 11, 2001).

Key words: north east ern Po land, Vistulian Gla ciation, Eemian Inter gla cial, ice sheet limit, tills.

INTRODUCTION (Astapova et al., 1987; Karabanov, 1987; Valtchik et al., 1990; Gaigalas, 1995; Kondratiene, 1996; Satkunas et al., 1997). The other ice sheet of the Vistulian Gla ci ation that cer tainly advance d onto the area of northern Poland was that of the Main This pa per deals with the limits of the Vistulian Gla ci ation Stadial (Leszno-Pomeranian). At the end of the glaci ati on a in north east ern Po land and neigh bour ing ter ri to ries of Lith u a- conti nu ous retre at of the ice sheet occurred, inter rupted by nia and Belarus. It is a summ ary of the Ph. D. thesis short stagna ti on events (of the rank of phases and subphases) (Krzywicki, 1999b). marked by moraine belts. A sim ilar idea was ear lier pos tu lated The aim of the work was to inves ti gate which of the ice by Żurek (1975), Ber (1990) and Lisicki (1993). The stagna ti on sheets of the Vistulian Glaci ati on advance d onto the area of pe ri ods were usu ally sta ble, rarely with os cil la tory fluc tu a tions, northeas tern Poland, as well to recon struc t and deli mit its maxi - lo cally of a transgressive char acter. It seems that the only ex - mum extent . cep tion was the lo cal Wigry transgres sion that oc curred be - The Oldest (Toruń) Stadial, two thin gla cial tills found by tween the max im um advance of the ice sheet and the Pom er a - Makowska (1976) and Drozdowski (1986) in the Lower nian Phase (Lisicki, 1993). Vistula region, is not consid ered in this paper, which deals with In the north the re search area em braces up lands and the ice sheet limits of the two Vistulian Glaciations: the Świecie outwash plains of young-glacial re lief. These are fragm ents of Stadial and the Main Stadial. the Mrągowo Lakeland and Mazury Great Lakes Dis trict, Many Polish authors have suggest ed that the ice sheet of the Mazury Plain, part of the Ełk Lakeland and Rajgród Lakeland, Świecie Stadial extende d into northern Poland, though its pres- as well as the Augustów Plain, Dainava Plain and part of the ence east and south of the Mazury Great Lakes Dis trict has not Centra l Neman Lowland. In the south, the study area covers been proved. Both Lithu a nian and Belarussian authors suggest fragm ents of old-glacial uplands of the Kolno Upland, that there was no ice sheet in their coun tries at that time Białystok Upland, Sokółka Hills, Hrodna Upland and Lida 166 Tomasz Krzywicki

Plain, with in ter ven ing de pres sions of the Kurpie Plain, the Leszno Phase slightly far ther south, across the area of Biebrza Val ley, High Neman Lowland. The re search area co - Szczuczyn and Wąsosz, ap proach ing the macroforms de- vers 26 sheets of the De tailed Geo log i cal Map of Po land, scale scribed later by Musiał (1984) as the slope of a marginal con- 1:50 000 and oc cupies a total area of approx i m ately 7700 km2. tact and glaciofluvial kame rampart. The Lith u a nian and Belarussian parts cover about 3000 km2. In the Kurpie Plain, Rühle and Sokołowska (1961), Słowański (1971), Bogacki (1976) and Kozłowska and Kozłowski (1995b) drew the ice sheet limit of the Bal tic Gla - PREVIOUS RESEARCH ciation across “old” frontal morai nes sur rounded by the youn - gest outwash plain depos it s. Galon and Roszkówna (1961), Kalniet and Karaszewska Be fore 1939 Pol ish in ves ti ga tions of the last gla ci ation in (1972), Różycki (1972a, b, 1978), Mojski (1972), Straszewska northeas tern Poland were limit ed to the Suwałki area (1975), Wołk-Musiał (1980) and Żurek (1984) drew the line (Wołłosowicz, 1926, 1928; Pietkiewicz, 1928; Pawłowski, across the northern border of the Biebrza Val ley. Żurek (1975), 1933). Woldstedt (1935) publi shed a map of the Quater nary more over, con sid ered that the ice sheet en tered the Biebrza de pos its of East Prus sia with the ice sheet limit of the Vistulian mar ginal val ley as far as the Ełk and Jegrznia rivers, as shown Glaci ati on marked, trending along the Narew River val ley near by the Kuwasy ket tle hole. Łomża, south of Mońki and north of Sokółka (Fig. 1). The Ber (1972a, b, 1974, 1982) and Żurek (1975) claimed that maxi m um extent of the Pomer a nian Stadial was shown as the ice sheet limit of the Leszno Phase in the southern part of runing across the northern margin of the Mazury Lakeland. The the Augustów Plain ran across the northern slopes of the “Is - first Pol ish at tempt to summa rise the Qua ter nary stud ies of East lands” of Sztabin, Jastrzębna, Nowy Lipsk and Lipsk. A simi lar Prus sia was the pa per by Galon (1937), which also include d a opinion was express ed by Bogacki (1976), who as sumed that map of mor pho logi cal landsca pes of East Prussia construc ted the ice sheet reached the Biebrza Val ley, cover ing the whole of on the basis of Woldstedt’s map (1935). Galon (1937) include d the Augustów Plain. the whole Lakeland within the ex tent of the ice sheet of the Ber (1975b) repo rted that the ice sheet limit of the Leszno Pom er a nian Stadial, with its limit runnin g across the area of Phase which, as he assum ed, coin cide d with the maxi m um ex- Mikołajki, Orzysz and Ełk. tent of the North Pol ish Glaci ati on, trends across the Kolno Up- After 1939, studies of Quater nary depos it s and extent s of land and along the northern end of the Biebrza Valley (from ice sheets in north eastern Po land be came more sys tem atic. Cwaliny through Kowalewo, Łodygowo, Bęćkowo, Grajewo, Majdanowski (1947) drew the ice sheet limit of the Vistulian Danowo, Kosiły, Dręstwo Lake, Woźnawieś and Tajno Lake). Gla ci ation south of Szczytno, north of Rozogi, be tween Pisz Re cently, Ber (1999, 2000), quoting Liszkowski (1993), has and Biała Piska, north of Grajewo, south of Rajgród, north of con sid ered that glacioisostasy had an impact on the maxi m um Sztabin and along the Wołkuszanka River val ley. Halicki ex tent of the Vistulian Gla ci ation and the po si tion, di rec tion (1950, 1951) recog nise d, on the basis of palynological studies , and extent s of reces sion-oscillation marginal zones. depos it s of two more glaciations above Eemian Inter gla cial de - Glacioisostasy op er ated pri mar ily along lon gi tu di nal tec tonic pos its: Gla ci ation V (North Polesie or North Pol ish Glacia tion) faults of the deeper base ment. The mar ginal zone of the Main and Glaci ation VI (Bal tic Glaci ation). The for mer reached the Stadial of the Vistulian Gla ci ation co in cides, ac cord ing to Ber area of Supraśl, Gródek and Jałówka (Halicki, 1951). Farther (1999, 2000), with the longi tu di nal Sajno-Rygol fault. east, Belarus, Halicki drew the limit of Gla ci ation V across Marcinkiewicz (1973) recon struc ted the extent of Svisloch, Porozow, Lyskov, Ruzhana, Byten and south of young-glacial reli ef on the basis of the analy sis of topo graphi c Baranovitchi. Pachucki (1961) mapped the Neman Ice Lobe in maps of the South Mazury and the Suwałki area, at a scale of the Suwałki area. Kondracki (1952) disti nguishe d 9 belts of 1:25 000, under sta nding its limit as a boundary betwe en an area fron tal mo raines de pos ited dur ing the Bal tic Gla ci ation. That abounding with ket tle holes and an area with a regu lar drainage au thor drawn its max imum ice sheet limit across Nidzica, sys tem. Marcinkiewicz (1973) suggest ed that this boundary Szczytno, Śniardwy Lake and Ełk. corre sponded to the maxi m um extent of the last glaci ati on. Since the begin ning of the 1960s most authors assum ed, Kociszewska-Musiał (1978) alone assum ed that the af ter Galon and Roszkówna (1961), that the maxi m um limit Vistulian ice sheet advance d only onto the East Suwałki of the Bal tic Gla ci ation in north east ern Po land co in cided with Lakeland, whereas in the west ern part it filled major de pres - the Leszno Phase. Those authors drew the limit line betwe en sions and valley s. Lipowiec and Szczytno, north of Rozogi, across Jeże, north of In recent years there were also some attem pts to draw the Szczuczyn, north of Grajewo, south of Rajgród, across the ice sheet limit of the Vistulian Gla ci ation far ther to the south. northern slopes of Sztabin “Island” and south of the These at tempts were based on thermoluminescence dating, and Wołkuszanka River val ley. A general out line of this limit re - were stimu lated pri marily by the con scious ness that there is a mained basi cal ly unchange d in later papers, although several dif fer ence (cf. Halicki, 1950, 1951) betwe en the degree of de - au thors in tro duced some mod i fi ca tions. The lim its were nuda ti on in the zone typi cal of old-glacial areas and that in the drawn across the area of Szczytno, Rozogi, Jeże, Grajewo, area locat ed to the north — al though out side the com monly ac- Rajgród and the southern part of the Augustów Plain. In the cepted ex tent of the Bal tic Glaci ation. These are the Mława and Kolno Upland, Szafer (1955), Rühle and Sokołowska (1961), Przasnysz ar eas, the Białystok Upland and the Sokółka Hills, as Mojski and Rühle (1965) and Mojski (1972) drew the limit of well as the Biała Piska region and northern areas of the Kolno The maxi m um ice sheet limit of the Vistulian Glaci ation in northeast ern Po land and neighbour ing ar eas 167 s r o h t u a

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. g i F 168 Tomasz Krzywicki

Fig. 2. Borehole

Up land. Re search work ers empha size the fresh ness of the land - tills older than the Main Stadial were also ini ti ated in the neigh - scape of the area, the varied topog ra phy, steep slopes and a bour ing ar eas. dense sys tem of small valleys. Marks (1988) discov ered that the ice sheet W3, coeval with Fedorowicz et al. (1995), using TL datings, as cer tained that the Œwiecie Stadial (60–55ka BP), reached the areas of P³ock, the ice sheet front of the Vistulian Gla ciation may have reached Lidzbark Warmiñski, Nidzica and Szczytno. In Warmia and the area of Bia³ystok. Banaszuk (1995) based his strati graphi - the West Mazury Lakeland, the limit of the ice sheet W3 co in - cal conclu sions mainly on TL datings from the Knyszyn For - cides with the maxi m um extent of the Vistulian Gla ci ation. In ests, young-glacial areas of northeas tern Poland (Banaszuk et suc ceed ing pa pers Marks (1990a, b, 1991, 1994, 1997a, b) up- al., 1994) and the Narew River val ley (Banaszuk, 1996). The held these ideas. Lindner (1992) was of the opinion that the result s of his inves ti ga ti ons show that the Toruñ Stadial ice Œwiecie Stadial ice sheet advance d again onto the Lower sheet had the great est ex tent of all the Vistulian ice sheets (ap - Vistula region and, possi bly , onto Warmia and the northern proxi m ately 110 ka BP), reaching Brañsk, Wysokie part of the Mazury Lakeland. On the basis of pet rograph i cal Mazowieckie and the Nurzec River. The Œwiecie Stadial ice stud ies and ex am i na tions of er rat ics Lisicki (1998) and Ga³¹zka sheet covered only the East Suwa³ki Lakeland, and it was the et al. (1998) moved the hypo thet i cal line of the maxi m um ex- last glaci ation in that re gion. It is pos si ble that the ice sheet front tent of the Œwiecie Stadial southward s to the M³awa area. of the Main Stadial stopped in the extre me north of the There is no contro versy among geol o gist s on the extent of lakelands, with ice tongues moving southwards into depres - the last gla ci ation (Poozerie Gla ci ation) in Belarus. The ice sions. sheet limit was drawn by Voznyatchuk (1956) and upheld by Af ter the pub li ca tions by Makowska (1976, 1979, 1980) on Vaytekunas (1968) and Voznyatchuk et al. (1972), and is com - the stra tig ra phy of the Vistulian Gla ci ation de pos its in the monly ac cepted by Belarussian researc h work ers. It runs across Lower Vistula region, studies on the possi ble greater extent of the northern slopes of the Hrodna Upland, enter s the Neman River val ley near Hrodna and then turns southwards to the The maximum ice sheet limit of the Vistulian Glaciation in northeastern Poland and neighbouring areas 169

type sec tions

Aziory area (hence the name of the ice lobe). Goretskiy (1983) Phase) and Baltija Stadial. The stadials re flect two ice sheet ad - and Karabanov (1987) moved the line several to tens of kilo- vances, of which the for mer had a greater extent. metres southwards. There is a com mon opinion that the ice sheet did not enter the Neman River val ley south of Skidel. Only Chepulite (1978, 1986) claimed that the youngest glaci - RESEARCH METHODS ation tills spread as far as south of the Dainava Plain, the Cen - tral Neman Lowland and Hrodna Upland. Astapova et al. (1987) consid ered that the ice sheet of the The present report is based on the analy sis of geolog i cal in- Late Poozerie Stadial had its greatest extent during the Poozerie vesti gati ons of depos it s and landform s in the broadly under stood Gla ci ation (Baltijskij horizon, Orshanskij Megastadial) zone of maxi m um extent of the Vistulian Gla ci ation, the anal y sis 17–18 ka BP. of topo graphi c maps with parti cu lar regard to geomorphological Belarussian sci en tists (Karabanov, 1987; Astapova et al., prob lems, an anal y sis of the re sults of pet ro graph i cal-lithological 1987; Valtchik et al., 1990) have not found any de posit s and in ves ti ga tions (used to con struct the De tailed Geo log i cal Map of geomorphological feature s of the early Poozerie Gla ci ation. Po land, scale 1:50 000), palynological studies of Eemian Inter- Ac cord ing to Astapova et al. (1987), the ice sheet of the gla cial sites, and thermoluminescence datings of tills, lac us trine Srednie-Poozerskij Megastadial (Dvinskij subhorizon), that and ice-dam lake de pos its. corre sponds to the Œwiecie Stadial, proba bly reached the north- Topo graphi c and geomorphological maps, at a scale of ern border of Belarus, not overste pping it. 1: 25 000, were also analy sed. These gave evi dence for distri - Lith u a nian ge ol o gists and ge og ra phers, among oth ers buti on of frontal and dead-ice morai nes, kames, eskers and gla - Gaigalas (1995), Kondratiene (1996) and Satkunas et al. cial tunnel val leys, outwash fans, morai ne “islands ” of an older (1997), agree that ice sheet transgres sions occurred only during morainic pla teau within outwash plain depos it s, out crops of a the later phase (Upper Nemunas) of the Nemunas Gla ci ation. till basement within outwash plain and ice-dam de pos its, top o- They dis tin guished the Gruda Stadial (in clud ing ¦¦iogeliai graphic lows which in the past may have formed marginal val- 170 Tomasz Krzywicki p a m

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. g i F The maxi m um ice sheet limit of the Vistulian Glaci ation in northeast ern Po land and neighbour ing ar eas 171

Fig. 4. Geo logi cal cross-section A–B: Mrągowo Lakeland, Kurpie Plain

leys or drainage routes for the pra-Neman (Nemunas) River, lus trate the typ i cal geo log i cal struc ture of the sub-sur face Pleis- channel lakes and dead-ice troughs. tocene depos it s, and form a basis for the construc tion of geo- 62 carto graphi c borehole secti ons were analy sed from the log i cal cross-sec tions and fur ther anal y ses (Fig. 2). Pol ish part of the research area, and sev eral tens of borehole Es pe cially detailed anal yses were made on 16 sheets of the secti ons from Belarus and Lithu a nia. 24 type secti ons were se- De tailed Geo log i cal Map of Po land, at a scale of 1:50 000, lected. These are char acter ised by the fol low ing fea tures: (Maksiak, 1992; Kozłowka and Kozłowski, 1993, 1995a, b, — the pro files were analysed for palynology and age de ter - 1996a, b, 1997, 1999; Krzywicki, 1996, 1999a, 2001a, b; Żuk, mi na tions; 1997, 1998a, b; Kacprzak, 2000; Lichwa, 2000; Ber, in prepa - — the age of any one of the litho logi c hori zons is supporte d ra tion). Geo log i cal documentations were also analysed, pro - by 2 methods, e.g. the lithotype is de ter mined us ing pet ro- viding much infor m ati on on the lithol ogy of end morai nes, graph i cal stud ies with ad di tional TL datings; kames and outwash fans. — they possess the most complet e sequence s of the The aim of the work was to study the youngest glacia l de- Vistulian Gla ci ation de pos its; pos its, in clud ing tills. Their dis tri bu tion, ex tent, thick ness and — they show a char ac ter is tic de vel op ment of de pos its, lithol ogy were exam ined. Supposed extent s of the youngest most typ ical for the study area. ice-dam lakes, which came into ex istence during the trans gres - These profil es prove the age of Late Pleisto cene depos it s, in sion and regres sion of the youngest glaci ati on ice sheet, as well par tic u lar the Vistulian Gla ci ation and the Eemian Inter gla cial as the drain age routes of the an cient Neman River wa ters to the depos it s, throughout the study area. In some cases they also il - drainage system s of the Biebrza, Narew and Vistula during the 172 Tomasz Krzywicki

Fig. 5. Geo log ical cross-section C–D: Augustów Plain, Biebrza Val ley, Sokółka Hills ice sheet re treat of the Vistulian Gla ci ation, were also in ves ti - it is proba ble. The thickness of the intergla cia l depos it s varies gated. A number of geolog i cal cross-secti ons were construc ted. from 0.5 to 7.2 m (Fig. 7a, b). They show the geolog i cal struc ture of the Mid-Late Pleis tocene In the Hrodna Upland, and High and Centra l Neman Low- de pos its in the re search area (Figs. 3–5). land intergla cia l depos it s fill abandoned river channels in the Neman River val ley (Pavlovskaya, 1998). Some Belarussian and Lithu a nian ge olo gist s suggest that in this area the whole of PALYNOLOGY Eemian Inter gla cial de pos its are over lain by a till or its re sid - uum (Voznyatchuk, 1956; Chepulite, 1966; Kryger et al., 1971). Other authors (Voznyatchuk, 1960; Pasyukievich et al., Ap prox i mately 45 Eemian Inter gla cial sites have been de - 1972; Goretskiy, 1980) consid ered that some of the Eemian scribed so far and inves ti gated within the zone of the maxi m um Inter gla cial sites (Pyszki, Poniemuń and Druck) pos sess only a extent of the Vistulian Glaci ati on in northeas tern Poland, west - periglacial solifluction cover. Karabanov (1987) claims that ern Belarus and south west ern Lith u ania. These are sites of la - there is no precis e answer to the questi on whether the Eemian custrine organic sedi m ents both uncov ered and covered by gla- depos it s are covered by a till or not in the pe ripheral zone of the cial depo s its, most of ten by the Vistulian Gla ci ation till, its re - Hrodna Upland near the Neman River. In west ern Belarus, the siduum or glaciofluvial de posit s (Fig. 6). The cli ma tic op ti mum most widesprea d Eemian deposit is bog lime, often covered of the Eemian Intergla cia l is recorded in 10 sites, and in 2 more with peat, 1–8 m in thickness (Karabanov, 1987). The maxi m um ice sheet limit of the Vistulian Glaci ation in northeast ern Po land and neighbour ing ar eas 173

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ł z o o l r r e a a o 9 a t r a o o i o i 9 i K K M K ( B B c ( ( V B S ( H 1 174 Tomasz Krzywicki The maxi m um ice sheet limit of the Vistulian Glaci ation in northeast ern Po land and neighbour ing ar eas 175 s t n e m i d e s

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Fig. 8. Di agram of the co ef fi cients O/K and K/W in the up per tills of NE Po land

The sites at Czeszczewlany, Białe Jezioro and Komotowo are Re sults of lithological-petrographical in ves ti ga tions per - undoubt edly locat ed within the extent of the youngest ice sheet. formed for the follow ing sheets of the De tailed Geo log i cal The lack of a till hori zon above Eemian Inter gla cial de pos its re - Map of Poland, at a scale of 1:50 000, were ana lysed: Wielbark sults proba bly from later erosiona l and denu dati on proces ses. (Jeleński, unpubl.), Lipowiec (Zawidzka, unpubl.), Świętajno A geo log i cal (palaeobotanical) cri terion is one of the most and Spychowo (Fert et al., unpubl.), Myszyniec im por tant cri te ria per mit ting the de lin ea tion of the ice sheet (Komacka-Makowiecka, unpubl.), Ruciane-Nida, Łyse, Pisz limit, showing that the Vistulian ice sheet did not advance onto and Kolno (Makarewicz and Zaczkiewicz, unpubl.), Biała the Mazovian and Podlasie lowlands (Banaszuk, 1995, 1996, Piska (Honczaruk, unpubl.), Rajgród, Rygol and Rudawka 1998; Fedorowicz et al., 1995). (Gronkowska-Krystek, unpubl.), Augustów Sta tion (Kenig, unpubl.). Vistulian Gla ci ation tills are ab sent from the bore - holes in the west ern part of the re search area (near LITHOSTRATIGRAPHY OF TILLS Ruciane-Nida, Łyse, Pisz and Kolno). Fur ther more, a spe cial repor t was pre pared (Gron - kowska-Krystek, unpubl.) for 26 till samples col lected for in - The ma jor fea ture that al lows the dis tinc tion be tween tills is vesti gati ons in the southern part of the Augustów Plain and Up- the pet ro graph i cal com po si tion of the gravel frac tions. This pa- per Biebrza Val ley (near Sztabin and Lipsk) (Krzywicki, per com pares the pet ro graph i cal com po si tion of peb bles from 1997a, b). the upper m ost tills from the Polish part of the resea rch area, us- Pet ro graph i cal anal y ses of grav els from 62 car to graphic ing this data to constract a stratigrap hi cal suc ces sion. boreholes , hand-auger holes and expo sures were perform ed. The meth od ol ogy of pet ro graph i cal stud ies was out lined by Petrographic co ef fi cients were cal cu lated for each sample. Lisicki (1998). Samples must contai n at least 100 grains, 5–10 Arith me tic means of these co ef fi cients for in di vid ual till ho ri - mm in di am e ter. The anal y sis in cludes the cal cu la tion of the zons were also cal cu lated. Fig ure 8 shows the mutual rela ti on - per cent age con tri bu tion of par tic u lar groups of Scan di na vian ships betwe en the groups of coef fi cie nts. 5 lithotypes can be rocks (crys tal line rocks, limeston es, dolomites, sandstone s, dis tin guish among the up per most till ho ri zons: B2, B1, B1bis, W2 quartzites and quartz grains) and local rocks (limestone s, marls, and W1. Lithotype B1 occurs only east of Suwałki and sandstone s, siltstones and claystones). Propor ti ons betwe en Augustów (Ta ble 1). Figure 9 shows exam ples of borehole dif fer ent rocks in each sample are char acter ised by sec tions contain ing tills of vari ous lithotypes. These re sults petrographic co ef fi cients: O/K, K/W and A/B, where: O — to - were com pared with the re sults of pet ro graph i cal in ves ti ga tions tal of sed imen tary rocks (lime stones, dolomites, sandstone s con ducted by Kenig (1998) in the Mazury and Suwałki and shales), K — total of crystal li ne rocks and quartz grains, W lakelands (Fig.10). — to tal of car bon ates (limeston es, dolomites), A — to tal of Values of pet ro graph i cal co ef fi cients O/K, K/W and A/B rocks non-resistant to weather ing (limestone s, dolomites, sand- (within the same lithotype) differ slightly from one study to an- stones and shales), B — total of weather ing-re sistant rocks other. The follow ing conclu sions arise from the analy sis of (crystal li ne rocks, quartz grains and sandstone s). petro graphical in ves ti ga tions: 1. They may have a great util ity in the lithostratigraphy of tills. The maxi m um ice sheet limit of the Vistulian Glaci ation in northeast ern Po land and neighbour ing ar eas 177

2. Tills B2 can be corre lat ed with the younger stadial of the Ta ble 1 Vistulian Gla ci ation, tills B and B cor re late with the older 1 1bis The co effi cients O/K, K/W and A/B in the up per tills stadial of the Vistulian Gla ci ation, tills W2 cor re late with the of NE Po land younger stadial of the Wartanian Gla ci ation, tills W1 cor re late with the older stadial of the Wartanian Gla ci ation. Litho - Num ber of Mean val ues of pet ro graph i cal co ef fi cients 3. It should be stressed that the youngest till (lithotype B2) type sam ples O/K- K/W-A/B occurs in the fresh morainic pla teaux with gla cial tun nel val - B2 7 2.39–0.45–2.14 leys. This supports Majdanowski’s proposal (1947) that glacia l B1 21 1.92–0.55–1.71 tunnel valley s are the best indi ca tor of the limit of the youngest B gla ci ation, con sid ered here as the Main Stadial of the Vistulian 1bis 13 1.38–0.80–1.10 Glaci ati on, 32–13 ka BP (cf. Shackleton and Opdyke, 1973). In W2 22 1.69–0.62–1.49 4 cases (Kiejkuty, Wojnowo, Racibórz and Pikły) out of 6, tills W1 11 1.53–0.72–1.38 B2 are un derlain by tills B1. 4. Tills B1 or B1bis from the area lo cated out side the maxi - mum extent of the Main Stadial alway s form the highest hori - zon (ex cept for two cases: the Krasne and Hanus boreholes in The first group include s only one date of 180.0 ka BP the Augustów Plain, where the upper till is weath ered and its (Żurek, 1990) (profil e 1 in Fig. 11). The second group contai ns lithotype cannot be define d). 2 dates — 118.4±17.8 (UG-2606) and 123.0±18.4 ka BP 5. In the Augustów Plain, Odranian Gla ci ation tills are sit u - (UG-2611) (profil es 2 and 3 in Fig. 11) (Fedorowicz, unpubl.). ated very high (boreholes Kolnica, Kolonia Jastrzębna, The third group include s 5 dates (profil es 4–8 in Fig. 11), from Jastrzębna II, Nowy Lipsk), and they are often overlai n by tills 47.0±7 to 63.0±9 ka BP (Lub-2088-90, UG-172) (Butrym, B1bis (in the last 3 boreholes ). In Krasnybór, tills W2 oc cur near unpubl.; Olszak and Fedorowicz, unpubl.; Olszak, unpubl). 4 the surface and are over lain by tills B1bis. of them were made on tills, one (the youngest ) on clayey mud. 6. De vi a tions from the av er age val ues of petrographic co ef - The fourth group include s 4 dates from muds and muddy clays fi cients O/K, K/W and A/B are very rare. They can re sult from — from 23.5±3.5 to 31.8±4.8 ka BP (profil es 9–12 in Fig. 11) the oc cur rence of de tached till frag ments of a dif fer ent age. Till (UG-2607-09, 2619) (Fedorowicz, unpubl.). from depths of 13.8–15.4 m (Nowy Lipsk borehole) , with coef - The anal y sis of TL and pet ro graph i cal in ves ti ga tions from ficie nts of 0.77–1.61–0.54, can serve as an exam ple. the Augustów Plain and Upper Biebrza Val ley were the sub ject 7. In at least 7 borehole secti ons, the upper tills are weath- of a sepa rate pa per (Krzywicki, 1997a). Its main conclu sion ered and the re sults had to be re jected. Weathering processes was that tills oc cur ring at the sur face are not of the same age ev- oper ate d over some areas during glaciations (periglacial cli - erywhere, and the “islands ” are composed of 2 or more tills of mate) and warmer peri ods (mod er ate clim ate), and were proba - dif fer ent ages. bly influ ence d by local geomorphological and microclimatic Dates from the Augustów Plain point to the occur rence of condi ti ons. Weathering zones often occur in the upper parts of older and younger tills of the Wartanian Gla ci ation and one till the youngest tills. of the Świecie Stadial. The younger dates from muddy de posit s 8. In 10 borehole secti ons from the areas of Ruciane, Pisz, sug gest the Grudziądz Interstadial and Main Stadial, prior to Łyse and Kolno, the first till (from top) is the Odranian Gla- the ice sheet ad vance. ciation till. TL dates can often help in stra tigra phy when consid ered to - gether with the result s of other inves ti ga ti ons. If we as sume the greater re li abil ity of pet ro graph i cal stud ies TL DATINGS over TL datings, and tie down the above-mentioned groups of co ef fi cients to par tic u lar lithotypes (re sult ing in strati graphi cal conclu sions ), we must re ject 2 of the thermoluminescence The thermoluminescence method (TL) was broadly used datings from the Augustów Plain. for abso lut e age deter mina ti ons in the 1980s and early 1990s. It was pri maril y em ployed to exam ine clays and muds, but also tills and sands. This was a standard method to estab li sh the stra - STRATIGRAPHY OF VISTULIAN GLACIATION tig ra phy dur ing the prep a ra tion of the De tailed Geo log i cal DEPOSITS Map of Poland . The author had at his disposal result s of 34 TL dates of near-surface depos it s from the study area. 17 of them come Unti l the 1950s it was comm only accept ed (Woldstedt, from the Augustów Plain and Upper Biebrza Val ley. One dates 1929; Kondracki, 1952; Szafer, 1953) that the last gla ci ation was kindly ren dered acces sible to me by Pro fes sor Żurek. An - was divided into the Leszno, Poznań and Pom er a nian phases other one com es from the paper by Żurek (1990). The most im - (cor re spond ing to latives of the Brandenburgian, Frankfurti an por tant datings for the present study are those from the and Pom era nian phases in Germ any). The Leszno Phase was Augustów Plain and Upper Biebrza Val ley (Fig. 11). They can con sid ered to have the greatest ex tent. be grouped into 4 time groups. Studies by Makowska (1976, 1979, 1980, 1986) result ed in the new stra tig ra phy of the Vistulian Gla ci ation in Po land. 5 178 Tomasz Krzywicki

Fig. 9. Ex am ples of bore holes with dif fer ent till lithotypes

tills dis tinguishe d by her were ascri bed to 3 stadials (Toruń, The Belarussian authors use the strati graphic scheme pro- Świecie and Main stadials) or to 2 glaciations: Toruń and Bal tic posed by Voznyatchuk (1972, 1976). He di vided the Poozerie (Vistulian) glaciations, which are sep arated by dated marine (Valdai) Glaci ati on into 5 zones or subzones, equiv a lents to depos it s. A warm period be tween the Toruń and Świecie stadials and interstadials. Starting with the Middle Vistulian stadials was termed by Makowska the Gniew Interstadial or these are as fol lows: Dvinskij (Kalininskij, Srednie-Poozerskij Krastudy Interstadial (1976, 1980), later named the Krastudy Megastadial) subhorizon, Srednie-Poozerskij subhorizon Inter gla cial (1986). (Krasnaya Gorka Megainterstadial) and Baltijskij ho ri zon Re sults of Makowska’s (1976, 1979, 1980, 1986) inves ti - (Ozerie, North Poozerie, Late Poozerie, Poozerie, Poozerie gati ons in the Lower Vistula region were later partly upheld Gla ci ation sensu stricto). More de tailed stratigrap hic schemes, by Drozdowski (1986) and, in Warmia and the western part of based on palynological studies , have recent ly been worked out Mazury, by Marks (1988). Marks recog nise d 3 tills of the (Yelovicheva et al., 1996, Yelovicheva, 1997; Yelovicheva Vistulian Glaci ati on (W2, W3 and W4), cor respond ing to the and Sanko, 1999). Yelovicheva et al. (1996) divided the middle tills BII, BIII and BIV of Makowska (1976). and upper parts of the Poozerie Gla ci ation into 2 parts: the Me - A sim i lar sub di vi sion of the North Pol ish Gla ci ation was dium Level and Naroch Level — Late Gla cial. The Me dium also ac cepted in the In struc tion for the De tailed Geo log i cal Level is subdi vided into 8 minor units: megastadials (cool pe- Map of Poland (1991). riods) and interstadials (warm peri ods). Miezhinskij I Stadial Current ly, some Pol ish authors (Lindner, 1987; Marks, corre sponds to the Świecie Stadial. The Orshanskij IV Stadial 1990a; Mojski 1997) accept strati graphic schemes of the corre sponds to the Main Stadial. The lates t paper by Vistulian Gla ci ation based on Makowska’s papers with Yelovicheva and Sanko (1999) quotes a serie s of radio car bon three main tills (1979, 1980). These schemes are well tied to and TL dates from depos it s of the Poozerie Gla ci ation in stratigraphi c schemes of the Upper Pleisto cene of northern Belarus. These dates are not given in the chart of stratigraphi c Eu rope (e.g. Behre, 1989), and to their corre la ti on with 18O schemes of the Vistulian Gla ci ation (Fig. 12). isotope stages (Shackleton and Opdyke, 1973; Mangerud, In Lith u ania, there are two equiv alent stratigrap hic schemes 1992), as well as to the climatostratigraphic scheme pro - of the Vistulian Gla ci ation, named the Nemunas Gla ci ation. posed by Wysoczański-Minkowicz (1982), and supporte d The first scheme was proposed by Gaigalas and Yartsev (1992) by age de ter mi na tions. and Gaigalas (1995). It re fers to palynology sites in southern The maxi m um ice sheet limit of the Vistulian Glaci ation in northeast ern Po land and neighbour ing ar eas 179 and north ern Lith u a nia (Jonionys, Rokai and Biržai). The Varduva Stadial (69 ka BP) is an equiva lent of the Świecie Stadial. The youngest cool pe riod is divided into 2 stadials: the Gruda Stadial (22 ka BP) with the ¦iogeliai Phase, and Baltija Stadial (17 ka BP). The stadials are sep arated by the Pavyte Interstadial. Guobyte and Pavlovskaya (1998) made an attem pt to link the upper parts of the Lithu a nian and Belarusian stratigraphi c schemes of the lat est gla ciation (Up per Nemunas and Orshanskij Stadial of the Poozerie Gla ci ation, cor re spond ing to the Main Stadial of the Vistulian Gla ci ation). Re search around the Lith u a nian/Belarusian bor der re sulted in the con clu sion that the upper stadial of the Nemunas/Poozerie Gla ci ation can be divided into the Gruda/Ozerie; Šventiany/Švenčionys and Baltija/Braslav phases, corre spond ing to the Brandenburgian (Leszno), Frankfurtian (Poznań) and Pom er a nian phases. An other Lith u a nian strati graphic scheme, pos tu lated by Satkunas and Grigyene (1997), and corre lat ed with other Euro - pean stratigrap hic schemes (Satkunas, 1997b), also refers to palynostratigraphy. Fig. 10. Min im al and maxi m al val ues of petrographic coef fi cient s accord - The Nemunas Gla ci ation was divid ed into the lower, mid- ing to: a — Kenig (1998) and b — author dle and up per parts. Paly no logi cal ly stud ied de pos its of warm peri ods of the lower and middle Nemunas (7 units) were inves - ti gated in 2 sites at Jonionys-on-Nemunas near Merkine and Mickunai near Vilnius. Warm peri ods are sepa rat ed by 7 cool or Pre-Grudziądz Stadial (Mojski, 1979). The Świecie Stadial peri ods, labell ed with the name of Nemunas followe d by a ice sheet ad vanced, ac cord ing to Lisicki (1996, 1997), onto the number and a letter . A cool period corre spond ing to the Mrągowo Lakeland from the north. Gałązka et al. (1998) con- Świecie Stadial is marked by a symbol Nemunas 2a. The upper sider that the till of the older Vistulian Gla ci ation con tains Nemunas de pos its (Nemunas 3) of the Gruda Stadial, ¦¦iogeliai more errat ics from the Baltic-Cland and Finn ish area, i.e. com - Phase and the Baltija Stadial are sep arated in this scheme by de- ing from the east, than from Sweden. A sim ilar dom ina ti on, but posit s of the Antaviliai and Ula interstadials (Satkunas, 1997a), still more accen tu ate d, is also observe d within the younger till al though the strati graphi cal po si tion of these interstadials is un- of the Vistulian Gla ci ation. It suggests that the centre of this clear, be ing cur rently un der re vi sion. gla ci ation was located to the east (Fin land, Cland Islands ) dur- The lat est Lith u a nian re search (Blazhauskas et al., 1998) ing both these stadials, but in the Świecie Stadial it moved to has shown that organic depos it s (peats, gyttja), exposed in high the west ern part of the area. banks of the Ula River and ear lier con sid ered to have repre - The Świecie Stadial ice sheet cov ered the north ern part of sented interstadial depos it s, are younger and repre sent the Kurpie Plain as far as Kolno, Wąsosz and Klimaszewnica, re- Older Dryas, AllerÝd and Younger Dryas. Recent inves ti ga - leased a small ice tongue into the Biebrza Val ley, reached the tions of the Antaviliai sec tion lo cated near Vilnius (Satkunas front of Sokółka Hills in the vi cin ity of Dąbrowa Białostocka, and Hütt, 1999) also show that lacus tri ne depos it s, corre lat ed and relea sed an ice tongue into the Nurka River val ley. In with the Antaviliai Interstadial, are older and rep re sent the Belarus the ice sheet by passed the Hrodna Up land, re leas ing an Drenthe-Warthe (Lublin) Interstadial. Satkunas and Hütt ice tongue into the Neman River val ley as far as Hrodna. It also (1999) consid ered that there are no sites with interstadial or reached the val ley east of Hrodna, cov er ing it with a large ice interphasial depos it s of the younger part of Vistulian Glaci ati on lobe as far as the Svisloch River Mouths and Dubrowlany. From in Lithu a nia and other Bal tic countri es. Therefore, there is no there, the eastern edge of the ice lobe ran to wards Skidel, climatostratigraphical ev i dence for es tab lish ing stadials, Ostryna and Motyle, to wards the pres ent Belarus/Lith u a nia bor- phases and interstadials during that period. der. The extent was de lim ited taking into ac count one of the most im portant geomorphological cri teria , namely, the occur - VISTULIAN GLACIATION — RECONSTRUCTION OF rence of gla cial troughs with lakes (Majdanowski, 1947). The CLIMATIC CHANGES AND ICE SHEET LIMITS absenc e of lakes in the old-glacial landsca pe (only this kind of landsca pe is observe d within the area of the Świecie Stadial ex - tent) is a very im portant indi ca tor of landsca pe matu rit y. Only A recon struc tion of geolog i cal events of the Early Vistulian scarce rel ict lakes oc cur within that zone. It is as so ci ated with Gla ciati on can only be approx i m ate becaus e no depos it s of this the period of filling of lake troughs with sedi m ents age have been found in northeas tern Poland. (Więckowski, 1966). Another geomorphological crite rion — During the period of 74–59 ka BP (cf. Mangerud, 1992) an- the pres ence (in some areas of max im um extent) of outwash other cooling of the clim ate result ed in an ice-advance. In Po- plains — show ing a kame ter races charac ter, morphometrically land this pe riod is called the Świecie Stadial (Makowska, 1986) as so ciated with marginal forms — was also con sid ered. 180 Tomasz Krzywicki g n i t a d

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. g i F The maxi m um ice sheet limit of the Vistulian Glaci ation in northeast ern Po land and neighbour ing ar eas 181

Fig. 12. Stratigraphi cal sub divi sion of the Vistulian Glaci ation (Nemunas, Poozerie)

Among morphogenetic crite ria , the occur rence of mo - The thermoluminescence method (TL) enable d age deter - raines, as well as the mu tual re lation ships between end mo - mi na tion of gla cial and glaciolacustrine de pos its within the raines and betwe en morai ne outli ers on outwash plains were area of the maxi m um ice sheet limit of the Świece Stadial. The also taken into consid er ati on. The most im portant group, how- distri bu tion of sites of Eemian depos it s , which are not covered ever, are geo log ical crite ria. These in clude the ex tent of glacial by gla cial de pos its, al lows iden ti fi ca tion of the po ten tial max i- till related to the ice ad vance. The Świece Stadial till was iden - mum ex tent zone of the Vistulian Gla ci ation. ti fied on the ba sic of pet ro graph i cal in ves ti ga tions which com - Af ter the retrea t of the Świecie Stadial ice sheet, there be- prised determinating the per cent age dis tri bu tion of gan a warm period called the Grudziądz Interstadial or petrographic groups in gravels extra cted from tills. Interpleniglacial. It lasted from 59 to 24 ka BP (cf. Mangerud, 1992). Deposit s of that age are known from many sites 182 Tomasz Krzywicki l a i d a t S

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. g i F The maxi m um ice sheet limit of the Vistulian Glaci ation in northeast ern Po land and neighbour ing ar eas 183

Fig. 14. Space-time schema of the Vistulian Gla ci ation in NE Po land and ad ja cent area

through out Po land (Mojski, 1988), but the most charac ter is ti c The ice sheet limit of the Main Stadial was recon stru cted in sec tion is a floristic suc ces sion from Konin-Maliniec I, where this work largely on the basis of the occur rence of glacia l tunnel an cient flora is ad di tion ally 14C-dated at > 42.9 ka BP val leys (Majdanowski, 1947). However, the limit was modi fie d (Kozarski, 1991). The Grudziądz Interstadial was char ac ter ised in many places be cause of use of other crite ria, first of all geo - by a cool, sub arc tic cli mate. Dur ing its first phase, forest less logi cal and geomorphological ones. tundra reigned with a wil low-horsetail com munit y. Later, Więckowski’s studies (1966) on the sedi m enta ti on rate in stunted birch and herbs becam e domi nant. Scattered lake troughs suggest that the reli ef was shaped during a pe riod birch-trees, typ ical of ar eas near the po lar for est limit, ap peared younger that the Świecie Stadial. During a pe riod of at the cli matic opti mum of the interstadial. There were also 12 000–13 000 years, af ter the ice sheet re treat from the area of vast, open spaces overgrown with herbs and mugwort. At the Mazury, Suwałki and Centra l Neman Lowland, most of lake end of the interstadial, stunted birch ap peared again. Av er age troughs may have be come filled with sedi m ents only by 20–35 %. tem pera ture s in July for centra l Poland ranged from 10 to 11°C The Main Stadial ice sheet cov ered the Mazury Plain as far as (Kozarski, 1991) during the clim ati c opti m um. Szczytno, Świętajno, Spychowo, Karwica Mazurska, Turośl, Another cool pe riod, called the Main or Leszno- Łacha, Jeże and further along the high morai ne belt separat ing the Pomeranian Stadial, started at ap prox im ately 24.0 ka years BP. Kolno Upland from Ełk Lakeland, as far as the town of Grajewo. The Main Stadial ice sheet reached its maxi m um extent be - From there, the ice sheet re leased a broad ice lobe into the Biebrza tween about 18 and 20 ka BP (ice-dam lake depos it s from Val ley as far south as the Białystok Upland near Goniądz. The east- Hoża-on-Neman un der ly ing the Poozerie Gla ci ation till, dated ern edge of that lobe ran along the Netta River valley to the village s at 18–200 ka BP). The Pomer a nian Phase is dated in the of Bór and Gabowe Grądy. The ice sheet cov ered the north ern and Suwałki Lakeland at approx i m ately 15.5 ka BP. The ice sheet middle parts of the Augustów Plain as far as Krasne, Ostryńskie and re treated from north east ern Po land at ap prox i mately Gruszki. North of Rudawka the ice sheet limit crossed the Po - 14.0–14.5 ka BP (Kozarski, 1991). land/Belarus bor der. In Belarus the ice sheet reached the north ern 184 Tomasz Krzywicki slopes of the Hrodna Upland, relea sed small ice tongues into the Vistulian Gla ci ation) of south east ern Mazury, the southern part Neman and Hozhka River val leys, and reached the villages of of the Suwałki area and the Hrodna distri ct. The major objec - Tabola and Lozy. Be tween Skidel and Ostryna the ice sheet limits tive was to draw the ice sheet limits of the Vistulian Gla ci ation. of the Main and Świecie stadials ran along the same line. The main conclu sions are as follows: Geomorphological, morphogenetic and geo log i cal cri te ria 1. During the Vistulian Glaci ati on the ice sheet advance d were used for de limit ing the ex tent of the Main Stadial ice sheet. twice onto the area of eastern Mazury and Suwałki and Hrodna The most impo r tant were gla cial tunnel val leys with lakes dis tricts: dur ing the Mid dle Stadial (Świecie Stadial — appro- (Majdanowski, 1947). As sum ing the low est sed i men ta tion rates ximately 55–67 ka BP) and during the Upper Stadial (Main and slow contra cti on of the lakes (Więckowski, 1966) we can Stadial — approx i m ately 24–12 ka BP). The ice sheet extent suppose that the only lakes that could persis t unti l the Holo cene was greater during the Świecie Stadial; it advanced from a few were those which formed after 50 ka BP, i.e. during the reces sion to about 30 km further to the south than the Main Stadial ice of the Main Stadial ice sheet. In the vi cin ity of Grajewo there is sheet (Fig. 14). an outwash plain with a dis tinct outwash fan. This is the upper - 2. Results of petrographic compo siti on of gravels from tills most outwash plain level in that area, that is prob a bly as so ci ated (lithotypes B2, W2 and W1) tend to be highly conver gent in the with the max imum limit of the Main Stadial ice sheet. Of en tire Polish part of the study area. Only the tills of the Mid dle morphogenetic cri te ria, lead ing to the de ter mi na tion of the or i gin Stadial of the Vistulian Gla ci ation have a differ ent petrographic and dis tri buti on of gla cial forms, the occur rence of morai ne belts com po si tion (lithotypes B1 and B1bis). The result s of from the area be tween Pisa and Grajewo were con sid ered. The petrographic re search al lowed a stratigrap hic sep ara tion of the most im por tant geo log i cal cri te rion was the dis tri bu tion of till, high est tills. iden tified by pet ro graph ical stud ies. The ice sheet limits of the 3. The ice sheet limit of the Świecie Stadial is marked by Vistulian Gla ci ation are shown in Fig ure 13. fron tal mo raines, outwash fans, kames and, in di rectly, by sites Karabanov (1987) consid ered that the Hrodna Upland sep- of Eemian Inter gla cial sed im ents. In the east ern part of the re - arat ed two ice lobes during the Brandenburgian (Leszno) search area the Świecie Stadial ice sheet rested against the older Phase. To the west the Kursk Ice Lobe ad vanced from the Bal- uplands that extende d to the south. tic Sea area (from NW), while to the east the Riga Ice Lobe ad - 4. The ice sheet limit of the Main Stadial is de limited by vanced from the north. During the Frankfurti an and Pomer a - gla cial tun nel val leys and lakes (ex cept for a few small reser - nian phases, the Kursk Ice Lobe was sep arated into two parts in voirs lo cated outside this line). Gla cial sed iments of the Main the Szeskie Heights area: the west ern part cov ered Mazury, Stadial have often not been preserve d within outwash plains at whereas the east ern part formed an ice tongue reach ing as far its max im um extent line. The Main Stadial ice sheet ad vanced as the Švenčionys Up land in east ern Lith u a nia. onto the middle ba sin of the Biebrza Val ley. In the Suwałki The ice sheet limit of the last glaci ation was simi larly drawn Lakeland it only reached the northern end of the Augustów by Pachucki (1961). It ran from the vicin it y of Wisztyniec, Plain, and farther south it re leased a small ice tongue which de - across Hańcza Lake, Krasnopol, Kapčiamiestis, Merkine, in pos ited a thin till in the Augustów Plain. A simi lar si tuation the vicin ity of Vilnius, to Pabrade and Švenčionys. If such an might have oc curred in the Mazury-Kurpie, Dainava (Lith u a - eastern tongue could formed during the retre at of the Main nia) and Porechje, Aziory and Bershty (Belarus) outwash fans. Stadial ice sheet, it is prob able that it may have also ex isted ear - Gla cial sedi m ents of the Main Stadial have com monly not been lier, during the Świecie Stadial. The con sid er ations are based pre served in the area of its max imum limit. on char ac ter is tic petrographic co ef fi cients for the Świecie 5. “Till islands ”, emerging from beneat h the Stadial tills observ ed in the east (Augustów Plain, Upper afore-mentioned outwash fans, as well as the “is lands” between Biebrza Val ley), which are dif fer ent than those cal cu lated in the Augustów Plain and Biebrza Val ley, are composed of the Mazury. These char ac ter is tic petrographic co ef fi cients have re - Świecie Stadial tills, at least as re gards their up per parts. sulted in the sepa ra ti on of lithotype B1bis. Lith u a nian and Belarussian sci en tists claim that during the Therefore, it is highly proba ble that the Świecie Stadial ice Mid dle Stadial of the Vistulian Gla ci ation there was no ice sheet ad vanced onto eastern Mazury from N and NW, from sheet in the ter ri to ries of their coun tries. Nev er the less, these west ern Fin land, west ern Lat via and west ern Lith u a nia. The studies in di cate that the Middle Stadial till is repre sented prob a - Suwałki and Hrodna ar eas were trans gressed by the ice sheet bly by the highest till observe d in southwest ern Lithu a nia and advanc ing from the N, from Finland, Esto nia, eastern Latvia north west ern Belarus, in the area be tween the limits of the Mid - nad eastern Lith u ania. The area that sep arated both the ice dle Stadial and the Upper Stadial. The Gruda Stadial till of tongues were the Szeskie Heights (or rather a basem ent el eva - south west ern Lith u a nia, and the Ozerie Phase (of the Baltijskij tion lo cated west of Hańcza Lake and stretching to the south to- ho ri zon, Orshanskij IV Stadial) till of northwest ern Belarus, wards Suwałki), not the Hrodna Upland. prob a bly cor re spond to the Świecie Stadial till in Po land. On the ba sis of lithological sec tions of the Eemian Inter gla cial and the last gla ci ation de pos its in the Neman River val ley, the ice SUMMARY AND CONCLUSIONS sheet limit of the Świecie Stadial of the Vistulian Gla ci ation is postu lat ed to run 15 to 20 km to the south of its previ ously drawn lo ca tion. This paper sum marise s knowledge on the near-surface geo- logi cal structure (depos it s of the middle and younger part of the The maxi m um ice sheet limit of the Vistulian Glaci ation in northeast ern Po land and neighbour ing ar eas 185

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