Geological Quarterly, 2000,44 (2): 187-197
The age and geological setting of Pleistocene glacigenic beds around the border between Poland and Belarus
Lazek LINDNER and Svetlana D. ASTAPOVA
Lindncr L. and Astapova S. D. (2000) -The age and geological setting of Pleistocene glacigenic bcds around the bordcr betwccn Poland and Bclam. Geol. Quart, 44 (2): 187-1 97. Warszawa.
Plcistocenc glacigcnic sdiments around the Polish-Bciarussian bordcr arc corrclatd. Tills of thc Narcvian Glaciation arc present in both countries, arc thosc in PoIand possibly being ordcr. Within the oIder South Polish Glaciations (Elstcrian) thcrc is no dcfinite evidence o f de- posits of thc Nidanian Glaciation in Bclarus, though the younger ofthcse glaciations (Sanian 1 and 2), sccm to correspond to the Bcrczin~an Glaciation sensu Into (Yaseldinian and Beminian sensrr s ~ c i o ) . During the oldcr Middlc Polish Glaciations (Saalian), compris~ng two glaciations (Liviccinn, Krmanian), thc Scandinavian icc shccts occupicd Polish territory only. Till of lhc Odnnian + Wartanian Glaciation In Poland is corrclatcd with till of thc Dnicpcrlan Glaciation in Belarus. Thcn: arc sirnilardcposits of the VistulianGlaciation (Poozerian) in both countries.
L w c k Lind~ier, Jtrsiiiirte of Geology, Warsaw Uniwmity, ~ i i r k i i W&rv 93, PL02-089 Warszawa, Poland; Svetiona D. Astapova, Insti- nrte ofGeologica1 Sciencm, Natio~rol Academy ofScimcm ofBelams, Kuprevidi 7.2201 4 1 Mitrsk, Belar~s (received: Nave~>iber 9,1999:
accepted: Decembs 13, 1999).
Key words: Poland, Belarus, PIcistocene, tills, stratigraphic correlation.
INTRODUCTION
This paper discusses the age, location and correlation of the Pleistocene; glacial sediments (mainly tilIs) around the border between Poland and BeIarus, considered in the context of inter- glacial deposits in this region.
Studies of the Pleistocene in both countries have hitherto used different methodological approaches as regards lithological description and bioslratipphical analyses, inter- pretation and conclusions. This paper attempts to overcome some of these differences. Four schematic geological cross-sections of the Pleistocene deposi~ in this area are given (Figs, 1-5). The different density of boreholes in each cross-section necessitated a varying horizontal scale. Two set;
tions run meridionally: one cuts northeastern Poland f b m Aug1st6w in the north to Biala Podlaska in the south (A-B at Flgs. 1 and 2) and the othw cuts western Belarus h m Gozha in the north to Gvoznitsa in the south (G-H at Figs. 1 and 51, These sections are joined by two whch sun westeast, one from Bialystok to Grodno
(GD
at Figs. 1 and 31, the other from Biala Podlaska to Malorita(EF
at Figs. 1 and 4). All sections were constructed on the same basis as previously publishednorth-south and west-east geological sections of the Quaternary diments in Poland (cf: Lindner et aL, 1995).
The presented sections m based on a single exposure and 99 boreholes, most reaching pre-Quaternary strata. Some bore- holes, ~ c u I a f l y the very deep ones around BiaIystok and S o k h , were drilled more than 30 years ago and hence their lithological description was often oversimplified. The Pleisto- cene sediments in this area range from about 280 m thick near Grodno and 220-240 m near Sokbika, to about 80 m near Biab Podlaska and 3 0 4 0 m near Malorita, Commonly
they
containinterglacial organic deposits.
The pattern of interbedding of tills and glaciofluvial depos- its comprised the basis to identify and date h e main glacigenic beds in this area. The stratigraphy of these beds in Poland in- volved the subdivision of the Pleistocene into 8 main glaciations separated by 7 interglaciaIs (Lindner, 1988a, b, 199 1;
Baraniecka, 1990; Lindmr and Marks, 1 994, 1999; Lisicki, 1997; Lindner and Marciniak, 1998). The glacigenic deposits in BeIams were meanwhile assigned to 5 glaciations separated by 4 interglacials (Astapova, 1983, 1993; Astapova and Monkevicb, 1990; Velichkevich et al., 1996, 1997). Here we show that the Bmezjnian Glaciation sensu lafo in Belarus equates with three South Polish Glaciations (Nidanian, Sanian
188 Leszck Lindner and Svetlana D. Astapova
Fig. 1. Area studied in amund he Poland-Belarus border
1
-
bowholcs and cxposurw: Ga - Gawrych-Ruda, S - Szczcbra, A -Augustbw, Sz - Sztabin, So - Sokblka, K5 - Kruszyniany 5, Og -
Ogrodniki,N -Narcw, Mi-Miclnik, Za-Zarzcczc, H - Horoszki, Wi
-
WiInyn, F - Easty, K1- Kruszyniany 1 , KR - Kolodczhny Rov, BP- Biala Podlaska, Wo - Woskmcnicc, G - Gvoznitsa, P -
hincrnanskaya, Sv-Svisloch,Ne-Nevbovichi,R-Borki,U-UgIany, Pod- Podosyc; 2 - schematic gmlogical sections (Figs. 2-5)
1, Sanian 2) and that the Scandinavian ice sheets did not reach Belarus during the older Middle Polish Glaciations (Liviecian, b a n i a n ) .
GEOLOGICAL SETTING
GEOLOGICAL CROSS-SECTION AUGUST~W-BIALA PODLASKA
This cross-section contains the most identified glacigenic units. The oldest is a till assigned to the Nardan Glaciation- Na (= nr). It occurs in several boreholes at depth of 150-1 60 m in the vicinity of AugustBw per, 1996), is up to 20 m thick and is underlain by Tertiary (PaIeogene?) sands and marls. This till is overlain by later Narevian sibs and sands at Szczbra (S at Figs. 1 and 2) andor by interglacial organic sediments showing
two climatic optima, assigned to the Augustovinn Interglacial (Janczyk-Kopikowa, 1996; Ber et al,, 1998), which correlates with the Podlasian Interglacial in earlier schemes (Lindner and Yelovicheva, 1998).
Tills of the Narevian Glaciation
-
Na (= nr) contain morecarbonate clasts than crystalline ones, and include abundant dolomites and local rocks (to 32.2%), with pmographic coeffi- cients: K/W = 0.86,
O K
= 1.23, A/B = 1.2 and DpNJp = 0.46 at Szczebrapa,
1996) and K/W = 1.27, OIK = 0.94 and All3 =0.76 at Krzykwo in which 0 are sedimentary rocks, K- crys- talline rocks and q u m , W - carbonate rccks, A - rocks non-resistant to weathering and B - resistant to weathering (Kenig, 11998), to the west of the cross-section. Among heavy minerals there are abundant garnets and amphiboles (Ber et al.,
1998).
Around Sokdka this till forms the basal part of the Pleisto- cene succession and occurs at a depth 200-220 rn (So at Fig. 2).
It is 5-10 m thick and underlain by Tertiq sands. At Kruszyniany 5 (K5) it fills a glacigenic depression, resting on Cretaceous deposits (Fig. 2). Further to the south it occurs at a depth of 60-80 m and forms isolated patches, either on buried elevations (between Narew md Mjelnik) or within glacigenic depressions (near Biala Podlaska). This ti11 has generally been assigned to the older stadia1 of the South Polish Glaciation (Nowicki, 1965, 1969; Ber, 1970), and only Rbkycki (1961,
1967), followed by Nowak (1931), correlated it with the Podlasian Glaciation (= Narevian).
A younger glacigenic unit in this a m , correlated with the Nidanian Glaciation - Ni (the first South Polish Glaciation), is best recognised near Augustbw (A at Fig. 2), where it occurs at a depth of 120-140 m per, 1946) and is represented by a till un- derlain by glaciofluvial sands with gravel. Tlus till, underlain by sediments of the Podlasian Interglacial - Po (= Aug~stovian - A), contains more crystalline rock fragments than carbonate ones, with a content of local rocks of to 4.9-5.8%.(Ber, 1996).
At Szczebra, petrographic coefficients of this till are: OIK = 1.70, W W - 0.61 andA/13= 1.58 (Kenig 1998). Among heavy minerah there are sIightly more garnets and less amphiboles tRan in the older till but no biotite occurs (Ber ef a[., 1 W8).
Further to the south there is a relatively continuous bed of this till. At hszyniany 5 it is at its deepest, thus resting on bur- ied dluvium of the Podlasian Interglacial - Po (= Augustovian -A) and it is preserved in a similar setling near Biah Pdlaska (Fig. 2). In both these regions it has h e n bated previously as a representative of a stadial of the South Polish Glaciation (Nowicki, 1969; Nowak, 1971), latterly assigned to the Nidanian Glaciation, particularly in papers on the geology of Biah Podlaska (Lindner, I9g8b; Nitychoruk, 1994).
TilIs of the younger South Polish GIaciations (Sanian 1- S 1, Sanian 2 - S2 = Wilgian), previously assigned to stadials of the South Polish Glaciation (Nowicki, 1965, 1969; Ber, 1970; Nowak, 1971), are preserved at S o k h at a depth of 150-1 70 m, in the Narew-Mielnik and Miehik-Biaki Podlaska regions at a depth of 30-40 m (Fig. 2). Near Biala Podlaska petrographic coefficients of the Iower till are equal to: O K =
1.54, K/W = 0.76 and
AIB
= 1.09 (bnig, 1998). l'hese tills and the accompanying glaciofluvial sands and gravels, and p d c u - larly the younger till, are covered by silty glaciolacustrine de- posits, widespread in nostheastern Poland and northwesternThe agc and geological setting of Plcistoccnc glacigcnic bcds around tbc bordcr betwcen Poland and Belarus 189
Belarus (Marks and Pavlovskaya, 1998). At Gawrych-Ruda (Ga) near Augustbw and at Wilcqm (Wi) near Biala Podlaska, these silts and sands are overlain by organic sediments of the Mazovian Interglacial -M (=Alexandrian - al) with its char- acteristic floristic succession (Janczyk-Kopikowa in: Ber, 1996;
Bihka et al., 1997).
The younger glacigenic unit in this cmss-section comprises deposits ofthe Liviecian Glaciation-L (Fig. 2) which, accord- ing to Lindner and Marks (1 999), is the fnit of the three Middle Polish Glaciations. Near Augustbw a till of this glaciation is up to 12 m thck and is presenred at depths 0f80-120 m, overlain by silts (Ber, 1996). Petrographic coefficients of this till are:
KsW= I.23,OK=0.83,AIB= 1.18 andDp/Wp=0.33,andit contains up tol2.8% of locaI Paleogene rocks (other local rocks:
2.3%). At Gawrych-Ruda it is overlain by organic sediments, presumably of the Zb6jnian Interglacial - 2. Near Sokhtka, a till of the Liviccian Glaciation - L forms a buried elevation and seems to occur as far as the Narew river valley Fig. 21, therefore indicating a limit of the Scandinavian ice sheet during this glaci- ation.
A till of the K m n i a n Glaciation- KIZ (Fig. 2) is, accord- ing to Lindner and Marks (1 999), an equivalent of the second Middle Polish Glaciation. Th~s till is preserved at depths of 80-1 00 m near Augustbw where it is a dozen metres thick, and at depths of 20-80 m between Sok6llca and Biata Podlaska. At its southernmost limit the till does not cross the Lower Krma river valley, indicating the maxim~un extent of the Scandina- vian ice sheet. Previously this till was connected with the older
@-maximum or maximum) stadal of the Middle Polish Gla- ciation (Nowicki, 1965, 1969; Ber, 1970; Nowak, 1971). At Narew (N at Fig. 2) this till is overlain by sands containing or- ganic material, presumably of the Lubavian? Interglacial
-
Lu? (Kupryjanowicz ef al., 1 999).
The third Middle Polish Glaciation, at present treated as the Warcanian Glaciation with its maximum, the Odranian Stadia1 (Lidner and Marks, 1999), is represented in t h s area by a lo- cally bipartite till (0 -1- W = dn at Fig. 2). At Szczebra near Aup~stbw this is the yo~mgest till, with the petrographic coeffi- cients WW = 1.47,OK= 0.82, hlB = 1.36 andDpIWp =0.28, indicating a predominance of crystalline over carbonate rocks (Ber, 1996). At Krzyzewo to the west of Augustbw, petrographic coefficients of this till are O/K = 1.96, WW = 0.54 and AiE = 1.89 (Kenig, 1998). In the middle part of the section there are distinctly less garnets, accompanied by more amphi- boles, whilebiotite is abscnt(Ber etab, 1998). According to Ber (1996), this till represents the Odranian Glaciation, and i t oocuts at depths of 12-30m.
The bipartite nature of this till near Mielnik and SokXka (Fig. 2), and its occurrence at surface outcrop between Szktbin (Sz) in the north to Biala Podlaska in the south, suggests oscilla- tions during ice sheet retreat, expressed in this part of Poland by at least two or three distinct stadial advances. Thick glaciofluvial sediments beneath this till at Kruszyrlimy 5 (Fig.
2) and Zarzecze (2 at Fig. 2) indicate meltwater erosion, lead- ing to the development of deep glacigenic channeEljke depres- sions.
The youngest glacigenic bed is relates to t h ~ Vistdian Gla- ciation - V (= Poozerian- pz) and is preserved in the vicinity of Augusthw only (Fig. 2) where it delimits a maximum extent of the Scandinavian ice sheet. A till, several metres thick, repre- smk it together with underlying and overlying glaciofluvial sediments. At zubrynek near Gawrych-Ruda to the north-west of Augustbw (outside the cross-section shown), petrographic coefficients of this till are O K = 2.14 K/W = 0.53 and All3 = 1.87 (Kenig, 1998).
GEOLOGICAL CROSS-SECTION RIALYSTOKGRODNO
A ti11 of the Narevian Glaciation - Na (= nr), noted neat Bialystok at depths of 170-220m is the oldest glacigenic bed in this cross-section (Fig. 3). It is up to 10 m thick and fills the bot- toms of deep glacigenic dep~ssions eroded in the Tertiary sands or in Cretaceous rocks. This till has been generally corre- Iated with the older stadial of the South Polish Glaciation (Nowiclu, 1969), named the Podlasian (RbQcki, 1961) and then the Narevian Glaciation (Rbkycki, 1978). Only Tsapenko and Makhnxh (1959) assigned it to the older glaciation. At Kruszyniany 5 (Figs. 1 and3), this till is overlain by alluvium of the Podlasian Interglacial - Po (= Augustovian - A).
A till ofthe Narevian Glaciation- nr (= Na) was noted also in the vicinity of Gmdno. Together with the accompanying glaciofluvial sands and gravels it occurs at depths of 1 15-220 m (Fig. 3). This ti11 is up to 90 m thick and overlies Jurassic lime- stones in a deep glacial depression and Cretaceous rocks in a shallower depression eroded by meltwaters (possibly a subglacial tunnel vaIley).
The
depressions are ikagmmts of two systems (Sopotskinskovo and Losenskovo), formed dctring the earliest ice sheet advances. Lineaments on satellitary photos (Azhgirevich et al., 1990) indicate that the former depression runs NE-SW (fiom Vilnius to Druskeninkai) and h e other NW-SE (from Grodno to Mosty).In the vicinity of Gnsdno a ti11 of the Nmvian Glaciation - nr (= Na) contains a characteristic set of heavy minerals, con- tents of hornblende, garnets, ilmenite, glaumnite, epidote, zir- con, leucoxene, pyrite, tourmaline each exceeding 10%
(Astapova, 1989). The coeficient of Scandinavian rocks is < 1, calculated as the ratio of Scandinavian minerals (hornblende, biotite, pyroxen~) to local minerals klauconite, siderite, pyrite, dolomite, phosphates) in the Itaction 0.25-0.1 mm. The heavy mineral composition of this ti11 can be denoted by the symbol HEGIP (hornblende, epidote, garnet, ilmenite and pyrite). The coefficient of crystalline rocks content is e q ~ ~ a l to 0.3-0.5, based on examination of the 3-5,5-7 and 7-10 mm fractions. This co- efficient is a ratio of the total of crystalline rock fragments (granite, etc.) to the total of sedimentary rock fragments (sand- stones, dolomites, limestones and others).
ln the vicinity of Bialystok these deposits are overlain by 3 younger glacigenic units, corresponding to the South Polish Glaciations (Nidanian - Ni, Sanian 1
-
S 1, Sanian 2 - S2).Each is represented by a single bed, commonly separated from the others by sands with gravels or by silts (Fig. 3). Only at
The age and geological sctting of Plcistmene glacigenic beds around the bordcr bctwccn Poland and Belarus 191
Kruszyniany 5 are there buried alIuvial deposits o f the Malopolanian Interglacial - Ma (= Korchevian - kch) sepa- rating the glacial deposits Nidanian-Ni and Sanian l- S l. In totaI, the three glacigenic wits of the South Polish Glaciations (Berezinian sensu iato) are about 100 rn thick and occur at depths of 50-140 m. All units in this complex were correlated previously with stadials of the South Polish Glaciation (Nowicki, 1965, 1969).
In the vicinity of Grodno there is a similar gIacigenic corn- plex of thc, Berezinian Glaciation semt laro - br s.[. (= Sanian 1 -I- Sanian 2 - S1+ S2). It i s composed of 3 4 ( ? ) largely amal- gamated tills, accompanied by sands and gravels (Fig. 3). These deposits are also to about 100 m thick and occur at depths of 50-140 m. At Krt~szyniany 1 (K1 ) there is also a buried alluvial unit, set in the upper part of the Bwezinian complex, and repre- senting a palamvalley of the Ferdynandovian Interglacial - F (= ByeIovezhian - bI),
Deposits of the Beminian Glaciation senm lato- br s. I. (=
Sanian 1
+
Sanisln 2-
S1-k S2) near Grodno contain abundant amphiboles (17-25%), hornblende, actinolite and tremolite, and also pyroxenes (2-3%). Among local minerals (3 1.6%) in tills there are: glauconite, dolomite, pynte, phosphates and sid- erite. From a mineralogical-petrographical point of view these tills are similar to the till efthe Narevian Glaciation- nr (= Na).The Belarussian authors denoted them with the symbol HGIE (hornblende, garnet, iImenite and epidotes) and BGIF (hornblende, garnet, ilmenite and phosphate). The coefficient of Scandmavianrocks inthese tills is equal to 1. In the Grodno area these tills contain commonly clasts of SiIurian limestones with brachiopods, and also traces of numerous glacicdynamic and glacioteetonic deformations. The age of these tills was deter- mined by reference to the overlying organic deposits of the Al- exandrian lnterglacial - a1 (= Mazovian -
M)
for example in the Kolodezhny Rov exposure (Figs. 1 and 3) (Yakubovskaya,1976).
The youngest bed in the vicinity of Bialystok and G m h o is represented by a till at the land surface accompanied by sands and gravels of the Odranian t- Wartanim Glaciation - 0 -t W (= Dnieperian Glaciation - dn), This tin is 5-40 rn thick ('Fig.
3). In the Grodno area it contains some local material (to 1 PA), and the coefficient of crystalline rock content is over 2. Heavy minerals are predominantly hornblende, garnets and ilmenite (in total 6690%). Boulders in end moraina of the Dnieperian Glaciation
- dn (= Odranian +-
Wartanian - 0 +
in this
area are dominated by material from central Scandinavia,
particularly h r n northern and central Sweden, the h a n d Is- Iands and the bottom of the Baltic Sea (Astapova, 198 1).
GEOLOGICAL CROSS-SECTION BIALA PODLASKA-MALQRITA
In the vicinity of Biaia PodIaska a till of the Narevian Glaci- ation - nr (= Na) r e p e n t s the oldest glacigenic bed. It occurs at depths of 75-> 82 m (Fig. 4). Tertiary (Oligocene) sands in a glacial depression underlie the till. This till is dissected by a bur- ied river valley of the Podlasian Interglacial - Po (=
kugustovian
-
A) and overlain by a glacige~c bed of the Nidanian Glaciation - Ni comprising sands, silts and till. The till occurs at depths of 50-60 m, is 4 1 6 m thick and locally di- rectly tmderlain by Tertiary sands.In this area the overlying glacigenic bed is represented by a till of the Sanian 1 Glaciation - S 1, to 8 m thick and occurring at depths of 4 6 5 0 m pig. 4). This ti11 is locally dssccted by buried valleys of the Ferdynandovian Interglacial - F (=
Byelovezhian - bl) and overlain by the succeeding glacigenic unit, of the Sanian 2 Glaciation - S2 (= Berezinian serrstr
stn'cto - br s.x). Tbis unit is dominated by a tiI1, sevaal to 30 m thick. Near Biah Podlaska the top of this ti11 occurs at depths from several to over 30 m. Its stratigraphical setting is con- strained by organic deposits oithe Mazovian InterglaciaI - M (= Alexandrian - a!), with palynological (Ktupihski et al., 198s) and diatomological (h4arcinia3E and Lindner, 1995;
Marciniak, 1998) analyses at Biala Podlaska (BP at Figs. 1 and 4), and detailed palaeobotanical analyses at Woskrzenice (Wo at Figs. 1 and 4; Bdca and Nitychomk, 1995).
The youngest glacigenic bed in the vicinity of Biah Podaska corresponds to the Odranian
+
Wartanian Glaciation - 0 -I- W (= D~ieperiaII - dn). It is represented by a relatively thin (to 3 4 m) discontinuous till and by accompanied silts and sands and glaciofluvial m d s with gravels (Fig. 4; Lindner, 1996). In the Bug river valley these deposits are dissected to the Tertiary and the incision is filled with Late Pleistocene and He locene alluwium.Around Malorita here are two Pleistocene glacigenic beds only (Fig. 4). The older is represented by a till of the Berezinian Glaciation sensu strict0 -brs.s. I(= Sanian 2 - S2). This till, in spite of its mosaic preservation, is to 25 rn thick and occurs at depths of 30-50 m, directly on Cretaceous rocks (Fig. 4). Dur- ing this glaciation (glaciations?) a deep and narrow glacigenic
Fig. 2. S~hcmatic gcological cross-soction A-B of thc Quaternary scdimcnts and thcir substrate from Auystbw to Bida Podlaska; by L. Lindncr b a s d on data
of Ruhlc and Zwica (1961), Nowicki (1969), Bcr (1970, 1996), Nowak (1971). Lindncr (19886, I996), Nivchotuk (19!M}, Bcr et a!. (1997), Bitika ef ol.
(1 997) and Rupryj~nowicz ct aI. ( 1 999)
Litholow: 1 -organic dcposits, 2- plant dctrihs, J -humus,4- santlr;,5-sands withgravcls, 6-gravel and boulders, 7- sandysilt, 8-claycysilt, 9 -silt, 10- diatornaccous siIt, 11 -sandy till, 12- till, 13 - clay, 14- claystones, 15 --sandstones, 16 -marl, 17 -chaIk, 18 - limcslone, 19 -
gIauconitc; o r i ~ n of sands and gravels: f- fluvial, gf- glaciofluvial; age: Cr- Crctacoous, T- Tertiary, Na (= nr) - Narcvian Glaciation, Po (=A) -
Podlasian Intcglacial (= Augustovinn), Ni - Nidaninn Glaciation, Ma (= kch) - Malopolanian Intcrglacial (= Korchcvian), S 1 - Sanian I Glacialion, F {=
bl) - Fcrdynandovian Intcrglacial (= Byclovczhian), S2 - Sanian 2 Glaciation, M (= al) - Mazovian Intcrglacial (= Alcxandrian), L- 1,iviccian Glaciation, Z - Zbbjnian Intcrglacial, Krz- Kn;nanian Glaciation, Lu? - Lubavian Interglacial?, O
+
W (= dn) Odranran + Wartanian Glaciation (= Dnicpcrian), E (=mu) -Ecminn Intcrglacial [= Mumvian). V (= pz) - Vislul ian Glaciation (= Poozerian); top of: 1 -Tertiary, 2 -South Polish Glaciations @crczinian.~ensri lato), 3 -Middle Polish GIaciations (Dnicpcrian); explanations of borcholc symbols scc Fig. 1
192 Lcszck Lindner and Svctlana D. Astapova
KRYNKI
Fig. 3. Schcmaiic geological cross-section C-D of the Quaternary sdmcnts and their subshate from Bialystok to Gmdno; by L. Lindncr for Poland, bascd on
data o f Nowicki (1969), and by S. D. Astapova for Belarus
J -Juressic, nr (= Na)- Narcvian Glaciation, br s.L (= SI
+
S2)-Bcrczinian Glaciation s ~ t s u fato (= Snnian I + Sanian 21, br-dn - Bcrczinian s m u lato-Dnicperian Glaciations, al (= M)- Alexandrian IntergIncial(= Mazovian), dn (= O+ W) - Dnicperian Glaciation (= Qdtanian+
Wartanian), pz (= V)- Poozerian Glaciation (= Vistulian): for olher explanations scc Figs. 1 and 2The age and geological setting o f Pleistocene glacigenic bcds around the bmdcr behvccn Poland and Belarus 193
BREST
Fig. 4. Schmatic geological cross-section E-F o f thc Quaternary srdimentr and their substrate from Biala Podlaska to Malorita; by L. Lindncr for Poland, bascdon dataofRiihle(l952),Now& (1971),Lindncr(1988b, 1996),Nitychonik(1994),Bi6kamdNitychoruk (1 995),Lindncr andMarciniak(1997,1998), and by S. D. Astapova €or Bclarus
bt s-s. (= $2) - B d n i a n Glaciation sensu srricro (= Sanian 2); for other explanations sec Figs. 1-3
fmnel-like depression was formed, noted at Gvoznitsa (G at Rgs. 1 and 4) and filled with sands, silts and clays. It was occu- pied by a Iake, with the deposition of diatomaceous silts whch contain a typical floristic succession of the Alexandrian Inter- glacial
-
a1 (= Mazovian - M) (Cruzman etal, 1935). A deep palamvalley near Bresl, incised in to Tertiary (Oligocene?) sands, is presumably of the same age.This valley and the interglacial Iake sdments ate overlain by the youngest glacigenic bed of the Dnieperian Glaciation - dn (= Odrian
-+
Wartanian - 0 1- W), represented by a till, locally at the Iand d a c e and up to 25 m thick, and by ice-dammed silts and glaciofluvial sands. The deposits in end moraines the Dnleperian Glaciation and emtics on a land sur- face near Malorita, contain abundant flint, phosphorites and or- ganic limestones in addition to crystalline material (Astapova, 1987). They were deposited by an ice sheet which advanced mainly from northwestern Finland, the kand Islands and the Baltic Basin and to a smaller degree (to 13% of she material), from northern and centraI Sweden,GEOL.QGICAL CROSS-SECTION GOZI-IA-GVOZNITSA
Near Gozha (to the north of Grodne) the oldest glacigenic bed is represented by patches of till of the Narevian- nr (= Na) Glaciation, up to 30 m thick and occurrjng at depths of 1 80-210
m on the southern slope of a glacial depression (Fig. 5). The Iat- ter reaches Grodno and is part of a more general depression of the base of the Quaternary, running NW-SE from Grodno to Mosty (Azhgirevich et a!., 1990). The base of this depression is incised through Tertiary sands in to Cretaceous rocks.
Further to the south, a glacigenic unit of the Narevian Glaci- ation-nr (= Na) is preserved between the Svislochriver valley andBorki (I3 at Figs. 1 and 5), where it is represwted by silts and sands with gravel and by a till. These deposits are preserved mainly on a glacigenic elevation, composed of Tertiary sands underlain by the Cretacmusrockr. The till is 12-25 m thick and occurs at depths of 80-1 60 m (Pig. 5). Near Borki this till and the locally underlying silts are up to 40 m thick and occur at
GOZHA GRODNO BORKl BEREZ A KOBRIN GVOZNITSA
Thc agc and gcolo~ical scttjng of Pleistocene glacigeni c beds around the bordcr between Poland and Bclarus 195
depths of 140-2 1 0 m, They fill a ghcigenic depression, gener- ally corresponding to the present valley of the Upper Narew river.
Further to the sou& a glacigenic unit of the Narevian Glaci- ation-nr (= Na) is composed of sands and silts overlain by till.
Between B~erki and Bmm these deposits are 20-40 m thick and occur at depths of30-90 m Only at Podosye (Pod at Figs. 1 and 5) silts (about 100 m thick) underlie these deposits, presumably inside a deep and narrow meltwater depression, the base of which occurs at depths of about I50 m. In the same section this glacigenic unit is overlain by organic deposits of the Byelovezhian Interglacid - bl (= Ferdynandovian - F).
Borehole data indicate that the Scandinavian ice sheet of the Narevian Glaciation advanced to the Kobryin area (Figs. 1 and 5). In the Narew and Yaselda waterfluve the coefficient of the Scandinavian rocks in the tilI is < 1 and there is asignificant con- tent of pynte, dolomite and siderite. The mineralogy is denoted by the symbol GRIS (garnet, mfile, ihenite and siderite).
h younger glacigenic unit is composed of deposits of the Berezinian Glaciation sensu Iato - br s.l. (= Sanian 1 -I- Sanian 2 - S1 f S2). In thenorthernmostpart ofthe sectition near Gozha they are 30-90 n thick and occur at depths of 50-1 50 m, filling a gfacigenic depression with glacial rafk of Cretaceous rocks.
Near
Grodno a till is 40-130 rn thick with traces of bi- or tripartity due to the presence of intertill sands and clays which may total 20 m or more. Organic deposits of the Alexandrian Interglacial - a1 (= Mazovian - M) at the top of the youngest till at Prinemanskaya (P at Figs. 1 and 5), determine the age of the underlying tills.Further to the south a till of the Berezinian Glaciation sensu lato - br s.1. (= Sanian 1 "r Sanian 2 - S 1 -k S2) is comjdmbly thinner (to about 10 m) at Nevbovichi (Ne at Figs. 1 and 5), thickening near Borki. At Borki (Figs. E and 5) the till is divided by organic deposits of the Byelovezhian Interglacial - bl (=
Ferdynandovian - F). Therefore, the older part of this glaci- ation can be distinguished as a separate Yaseldinian Glaciation - yas, correlated with the Nidanian - Ni or Sanian 1 Glaci- ation - S 1 (Nazarov, 1995). Further to the south, deposits of the- Byelovezhian InterglaciaI underlie the younger ti11 of the Berezinian Glaciation senm stntdo - br as., both near Bereza at Podosye (Pod at Figs. 1 and 5) and near Gvomitsa.
The succeeding glacigenic unit in western Belarus is com- posed of 1-2 tills, in total 540 m thlck, of the Dnieperian Glaci- ation - dn (= Odrian
+
Wartanian - 0+
W), in the northern and central part of the section. Between b d n o in the north and Gvomitsa in the south, these tilIs are mostly exposed at: the land surface or covered by thick (20-30 m) glaciofl uvial sands and graveIs. The age setting ofthese tilIs is constrained by the under- lying organic deposits of the Alexandrian Interglacial - a1 (=Mazovian - M), noted at Nevbovichi (Ne at Figs. 1 and 51, Borki (I3 at Figs. 1 and 5), Uglany (U at Figs. 1 and 5) and Gvomitsa (G at Figs. 1 and 5). In many pIaces these deposits are accompanied by interglacial alluvium, composed of sands with sthodinate silts and clays, which aIso underline tiHs of the Dnieperian Glaciation - dn in western Belarus.
The youngest glacigenic unit in this section is represented by deposits of the Poozerian GIaciation - pz (= VistuIian - V). They outcrop in the north near Gozha, where they form a separate tilI, 2-7 m thick, overlain by sands and underlain by
Pig. 6. Attempted correlation of Pleistmcne glacigcnic beds (hatched) around thc border between Poland and Bclams
glaciofluvial sands (Fig. 5). These deposits are up to 20 m thick The till contains much calcite and dolomites in the gravel h c - tion and aIso hornblende, pyroxene and biotite.
FINAL REMARKS
This paper attempts an initial spatial correlation of the PIeis- tocene deposits around the border between PoIand and Belarus.
The sening and age of the two youngest glacigenic units, as- signed to the Vistulian (= Poozerian) and Odranian
+
Wartanian(= hieperian) glaciations, was most easiIy determined (Fig. 6).
These deposits m u r at outmp in Poland and Belarus, and their geology and geomorphology has been studied for many years.
The age and correlation of the deeper glacigenic beds, accesi- ble mostly in theboreholes only, was more difficult to ascertain.
Starting h m the top, in western Belarus there are no depos- its that couId correspond to the glacigenic deposits of the b a n i a n and Liviecian glaciations, as well as to the Lubavian and Zbbjnian interglacials in Poland. The Scandinavian ice sheets duringthese glaciations prescunably only reached PoIand and land to the north of Belarus. Such a conc'tr~sion is supported by recent studies in Lithuania p a l m s , 1995; Kondratienk, 1996; Ber et al., 1997; Lisicki, 1998) and Russia (Bolikhovskaya and Sudakova, 1996).
The glacigenic deposits cemlated in Poland with the South Polish Glaciations (Nidanian, Sanian I, Sanian 2 = Wilgian) seem to have their equivalents in two gIaciations i.e. Berezinian senm lato (= Sanian 2) and Yaseldinian (= Sanian 1). The ice
196 L e m k Lindner and Swtlana D. Astapova
sheet of the Nidanian Glaciation therefore eithm did not reach Poland the Podlasian Interglacial (= Augustovi an), we conclude Belarus or its deposits have not
been
identified there yet. This that the oldest of Pleistocene glacigenic unit in both counkies probIem is relatedto that of the mutual age relations of the three seems referable to the Narevian Glaciation. But, it is also possi- oldest interglaciaIs in PoIand and Belarus (Korchevian, ble that the Narevian Glaciation in Belarus corresponds to the Podlasian = Augustovian, Malopolanian). Assuming thatin
Nidanian Glaciation in Poland (Lindner and Yelovicheva, Belarusthe
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!["Antoni Sygietyński. Estetyk i krytyk", Jan Detko, indeks zestwiła Lucyna Michalska, Warszawa 1971, Państwowy Instytut Wydawniczy, ss. 356 : [recenzja]](data:image/gif;base64,R0lGODlhAQABAIAAAP///wAAACH5BAEAAAAALAAAAAABAAEAAAICRAEAOw==)