The age of the old est Scan di na vian glaciations in mid-eastern Po land and south west ern Belarus
Leszek LINDNER, Barbara MARCINIAK, Al ex an der F. SANKO and Galina K. KHURSEVICH
Lindner L., Marciniak B., Sanko A. F. and Khursevich G. K. (2001) — The age of the old est Scan di na vian glaciations in mid-eastern Po - land and south west ern Belarus. Geol. Quart., 45 (4): 373–386. Warszawa.
Anal y sis of type lo cal i ties of Pleis to cene de pos its from mid-eastern Po land (Kozi Grzbiet, Łuków, Biała Podlaska and Wilczyn) and south west ern Belarus (Smolarka and Postolovo) has pro vided a new view on the age, lim its and cor re la tion of the old est Scan di na vian glaciations in the area. In te gra tion of palaeontological data with de ter mi na tion of the Brunhes/Matuyama bound ary (780 ka) at Kozi Grzbiet and Smolarka sug gests that the first gla ci ation (Narevian) pre ceded this bound ary and had a slightly smaller ex tent in SW Belarus than hith erto con sid ered. The sec ond gla ci ation (Nidanian) oc curred slightly above or at this palaeomagnetic bound ary. In Po land it is the first South Pol ish Gla ci ation, a till of which can be traced as far as the Holy Cross Mts. In SW Belarus it is rep re sented by a till to the south of Brest and Bereza, and con nected there with the old est gla ci ation.
Leszek Lindner, In sti tute of Ge ol ogy, War saw Uni ver sity, Żwirki i Wigury 93, PL-02-089 Warszawa, Po land; Barbara Marciniak, In sti - tute of Geo log i cal Sci ences, Pol ish Acad emy of Sci ences, Twarda 51/55, PL-00-818 Warszawa, Po land; Al ex an der F. Sanko, Galina K.
Khursevich, In sti tute of Geo log i cal Sci ences, Na tional Acad emy of Sci ences of Belarus, Kuprevich 7, 220141 Minsk, Belarus (re ceived:
No vem ber 22, 2000; ac cepted: Feb ru ary 7, 2001).
Key words: Po land, Belarus, Early Pleis to cene, Scan di na vian glaciations, strati graphic cor re la tion.
INTRODUCTION
We pro vide an analisis of the age of the two old est Scan di - na vian glaciations (Narevian and Nidanian?) in Po land and Belarus (Fig. 1). Halicki (1950) and Tsapenko and Makhnach (1959) iden ti fied the older of the two glaciations (Narevian) for the first time as be ing older than the Cracovian Gla ci ation (South Pol ish Gla ci ation, Elsterian and Mindelian). This gla ci - ation was at that time re ferred to as older than the Bialostockian (sensu Różycki, 1961), Przasnysznian (sensu Różycki, 1967) and Korchevian Inter gla cial (sensu Voznyachuk, 1961). It was re cog nised as the first one of the four then dis tin guished Scan - di na vian glaciations (Różycki, 1961; Mojski and Nowicki, 1964) and fi nally termed the Narevian Gla ci ation (Voznyachuk, 1961; Voznyachuk et al., 1977; Różycki, 1978).
The youn ger of the two glaciations (Nidanian) was iden ti - fied on the ba sis of Scan di na vian ma te rial pres ent be low the layer to gether with a fauna cor re lated with the Cromerian II (Westerhoven) in the Neth er lands, dis cov ered at the Kozi Grzbiet site near Kielce (Głazek et al., 1976). This gla ci ation is also rep re sented by one to two low er most tills to the north of
this site (Lindner, 1977). Palaeomagnetic data from Kozi Grzbiet in di cates that the Nidanian Gla ci ation oc curs around the Brunhes/Matuyama bound ary (Lindner, 1978; Różycki, 1978). Later on it was re cog nised as the first of the three South Pol ish Glaciations (Lindner, 1988a). It has not yet been re cog - nised in west ern Belarus (Lindner and Astapova, 2000).
The age and range of the Scan di na vian ice sheets dur ing these glaciations in Po land and Belarus are re con sid ered on the ba sis of new palaeomagnetic data from the Smolarka (S3) sec - tion near Bereza in Belarus (Fig. 1). Ac cord ing to these data, the old est till con nected with the Narevian Gla ci ation is youn ger than the Brunhes/Matuyama bound ary (Sanko and Moiseyev, 1996), de ter mined re cently at about 780 ka (Heller and Ev ans, 1995). Be sides Kozi Grzbiet (Głazek et al., 1977a), this bound - ary was also re cog nised in Po land at Witów near Kraków. It runs above preglacial grav els within silty-clayey de pos its (Nawrocki and Wójcik, 1990) that un der lie re sid ual till of the Sanian 2 Gla - ci ation (Lindner and Siennicka-Chmielewska, 1998).
Palaeomagnetic data from over ly ing de pos its sug gest that the till con sid ered as the equiv a lent of the Narevian Gla ci ation in the Kalejty sec tion near Augustów might cor re spond to the Gla cial A in the Neth er lands (Ber, 1997).
GEOLOGICAL SETTING
Against a ba sis of re cent cor re la tions of gla cial and inter - gla cial units be tween Po land and Belarus (Nazarov, 1995;
Velichkevich et al., 1996, 1997; Lindner and Yelovicheva, 1998; Lindner, 1999; Lindner and Astapova, 2000), we have reanalysed the geo log i cal set ting of the two main sites con tain - ing the Brunhes/Matuyama bound ary, i.e. Kozi Grzbiet and Smolarka, while con sid er ing links with the other four sites (Łuków, Biała Podlaska, Wilczyn and Postolovo) con tain ing the Older and Mid- Pleis to cene inter gla cial lake de pos its (Fig. 1). We aimed to throw some light on sev eral prob lems:
whether de pos its of the Narevian Gla ci ation are isochronous in Po land and Belarus, whether the Narevian Gla ci ation is youn - ger than the Brunhes/Matuyama bound ary and, if so, whether its strati graphic po si tion is the same as that of the Nidanian Gla - ci ation in Po land and in Belarus, and whether the ice limit of the Narevian Gla ci ation is smaller than sup posed so far, es pe - cially in Belarus.
KOZI GRZBIET NEAR KIELCE (FIGS. 1–4)
The Kozi Grzbiet sec tion, about 20 km to the west of Kielce, is rep re sented by de pos its in a cave within De vo nian lime stones (Głazek et al., 1976, 1977a, b). These de pos its
(Fig. 2) are up to 9 m thick and in their low er most part com prise grey-yel low clays with cal car e ous con cre tions rep re sent ing a pre-Pleis to cene (?) or even a Neo gene lime stone re sid uum.
Cherry-red in col our, quartzose clayey and poorly sorted sands with in ter ca la tions and lenses of clays and lime stone de bris and cal car e ous con cre tions oc cur above. The sands are 3 m thick and are char ac ter ised by ir reg u lar bed ding.
The sands con tain up to 30% of clay, sev eral per cent of silt and 60–70% of fine sand. Their heavy min er als in clude abun - dant zir con, ap a tite, rutile and tour ma line, and smaller quan ti - ties of gar net, epidote, bi o tite, am phi bole and pyroxene.
Be sides the do minant quartz, the light frac tion con tains small quan ti ties of feld spar and si li ceous rock frag ments. The clays are com posed mainly of kaolinite with small quan ti ties of illite and smectite. The cherry-red col our is due to hae ma tite. Con - sid er able ad mix ture of eas ily weatherable heavy min er als sug - gests a sig nif i cant gla cial component.
The sands are over lain by 1.5 m of “brecciated” cherry-red clay with cal car e ous con cre tions and grains of am phi bole and pyroxene. The clay is com posed mainly of kaolinite, haematite and ver mic u lite. Palaeomagnetic in ves ti ga tions have re vealed the Brunhes/Matuyama bound ary in its up per part (Figs. 2 and 3; Głazek et al.,1977a).
A ca. 1 m thick layer of sandy, brown-yellowish clays with bone frag ments and snail shells (Kowalski, 1975; Młynarski, 1977; Stworzewicz, 1981; Szyndlar, 1981; Sanchiz and
Fig. 1. Lo ca tion sketch-map of mid-eastern Po land and south west ern Belarus
Ice sheet lim its: 1 — older, 2 — youn ger; 3 — sites with lake de pos its dis cussed in the pa per; 4 — sites with inter gla cial de pos its cited in the pa per
Szyndlar, 1984), frag ments of sta lac tites, cal car e ous tufa and frag ments and blocks of lime stone (Głazek et al., 1977b) oc - curs above. The snails in clude Helicigona banatica, Soosia diodonta, Isognomostoma personatum, Zenobiella vicina, Cochlodina laminata, C. orthostoma, Lacinaria cana, Ruthenica filograna, Clausilia cruciata, Iphigena latestriata, I.
tumida and Acanthinula aculeata, rep re sent ing a warm and hu - mid for est as sem blage.
The am phib ian and rep tile bone frag ments re cog nised are dom i nated by Natrix cf. natrix and Triturus cf. cristatus, forms typ i cal of hu mid de cid u ous for ests. The pres ence of such mam - mals as Lemmus lemmus and Dicrostonyx simplicior points to a rather cold cli mate, while Cas tor fi ber, Clethrionomys cf.
glareolus, Sus scrofa, Alces sp. and Pliomys lenki are typ i cal of a hu mid for est. Among the nu mer ous mam mals there are Ursus deningeri, Sus cf. scrofa, Alces sp., Beremendia fissidens, Citellus polonicus, Dicrostonyx simplicior, Lemmus lemmus, Pliomys lenki, Cas tor fi ber, Mimomys savini, Clethrionomys cf. glareolus, Pliomys episcopalis, Pitymys gregaloides and Pitymys arvaloides.
Flu vio gla cial fine-grained sands with Scan di na vian ma te - rial (Fig. 2) cover the clays. This fact and the co-oc cur rence of Pliomys lenki, Mimomys savini, Dicrostonyx simplicior, Ursus deningeri, Pliobatrachus Langhae and Bombina cf. bombina in the clays, sug gest ing an Older Pleis to cene (Late Biharian) fau nal as sem blage, are cru cial to the age de ter mi na tion. The over ly ing sands are TL-dated to over 400 ka (Prószyński, pers.
comm.) whereas FCI/P-age de ter mi na tions of bones in di cate 700–550 ka, mak ing the cave de pos its at Kozi Grzbiet cor re - spond to the Cromerian II (Westerhoven) in the Neth er lands.
Anal y ses of col la gen loss in bones sug gest the cool est cli mate oc curred dur ing the de po si tion of the low er most cave clays, fol lowed by two warm ep i sodes sep a rated by a cool in ter val (Głazek et al., 1976, 1977a, b).
The cave de pos its thus typ ify the cli ma tic con di tions of the Kozi Grzbiet Inter gla cial, cor re lated with the Jasionka sec tion near Rzeszów (Dąbrowski, 1967; Laskowska-Wysoczańska, 1967), later named the Malopolanian Inter gla cial by Różycki (1978). Heavy min er als (am phi bole and pyroxene) de rived from weath ered crystalline (Scan di na vian) rocks, pre served at Kozi Grzbiet (def i nitely older than this inter gla cial), are con sid ered to be the traces of the Nidanian Gla ci ation along with the old est tills oc cur ring north of this site (Fig. 4). The sands cov er ing the cave clays within the site, as well as the youn ger tills oc cur ring in the area, cor re spond to the Sanian Gla ci ation (Lindner, 1982), sub di vided into the Sanian 1 and Sanian 2 (Fig. 4) and sep a rated else where by the Ferdynandovian Inter gla cial (Lindner, 1988a).
ŁUKÓW CROSS-SECTION (FIG. 5)
The cross-sec tion shown of the Qua ter nary de pos its in Łuków (Fig. 5) con sti tutes the north east ern part of the cross-sec tion of Rühle (1969). It is sup ple mented by the Ł-105 bore hole, the or ganic de pos its of which (peats and gyttja) were sub jected to palynological anal y sis (Sobolewska, 1969) and are taken into ac count in the new strati graphic in ter pre ta tion.
The bed rock of the Qua ter nary de pos its (that are 40–100 m thick) is com posed of Plio cene clays, un der lain by the Mio cene sands with in ter ca la tions of silt and brown coal, un der lain by
Fig. 2. Pro file, FCI/P age and palaeomagnetic data of cave de pos its from Kozi Grzbiet near Kielce (af ter Głazek et al., 1977a)
Sanian 1 and Sanian 2 Glaciations: 1 — fine-grained sands with Scan di - na vian ma te rial, structureless in their up per part, lam i nated in their lower part, with frag ments of sta lac tites and calc tufa as well as with lime stone blocks and de bris; Malopolanian Inter gla cial: 2 — brown-yellow sandy clays, with bone frag ments and snail shells as well as frag ments of sta lac - tites, calc tufa and lime stone blocks; Nidanian Gla ci ation: 3 —
“brecciated” clay com posed of pieces of lam i nated clay, cherry-red in col - our, with car bon ate con cre tions and grains of am phi boles and py rox enes;
pre-Pleistocene (?): 4 — cherry-red clayey sand, with de bris of lime stone and car bon ate con cre tions, 5 — poorly sorted sand with clayey lenses and de bris of lime stone and car bon ate con cre tions and with lenses of yel low to cherry-red clay, 6 — yel low-brown clay with car bon ate con cre tions, 7 — lime stone de bris and small car bon ate con cre tions, 8 — bone re mains, 9 — larger lime stone blocks in cave de pos its, 10 — snail shells
Oligocene sand with gravel, Eocene clay and silt with sand and Paleocene sandy marl and the low er most Cre ta ceous marl and lime stone. The old est Qua ter nary is rep re sented by the pre-Pleistocene (Pp) i.e. preglacial sands with gravel with out Scan di na vian ma te rial, and by poorly sorted, lo cally silty, sand.
The Pleis to cene se quence be gins with flu vio gla cial sands with gravel con tain ing Scan di na vian ma te rial to gether with a thin till in and around a gla cial-eroded de pres sion. These de - pos its rep re sent the old est gla cial ho ri zon in the area, are 5–10 m thick and cor re spond to the Narevian Gla ci ation (N) (Fig. 5), for merly named the lower stadial of the South Pol ish Gla ci ation (Rühle, 1969), and later, the Podlasian Gla ci ation (Ruszczyńska-Szenajch, 1976). Sands with gravel, prob a bly of flu vial or i gin, re late to the old est inter gla cial named the Podlasian Inter gla cial (Po) or Augustovian (?), and lie above the till of this gla ci ation. The sands are 3–6 m thick and are cov - ered by an al most con tin u ous layer of a sec ond till, 3–5 m thick.
This sec ond till prob a bly rep re sents the Nidanian Gla ci ation (Ni), and was for merly con sid ered as the equiv a lent of the up - per stadial of the South Pol ish Gla ci ation (Rühle, 1969) or as the older unit of gla cial de pos its of the Cracovian Gla ci ation (Ruszczyńska-Szenajch, 1976). The till cor re sponds to the Nidanian Gla ci ation of north east ern Po land (Kenig, 1998).
These de pos its and also the Oligocene de pos its in the bore - hole Ł-105 (Fig. 5), are over lain by up to 70 m of fine-grained silty sand with in ter ca la tions and lenses of gravel, clay and silt.
Rühle (1969) and Ruszczyńska-Szenajch (1976) in ter preted these a multi-cy clic flu vial suc ces sion of the Great Inter gla cial (Mazovian sensu lato). They are cov ered by a third till and youn ger sands as well as by peat and gyttja of the Ferdynandovian Inter gla cial (Cromerian? ac cord ing to Sobolewska, 1969), and thus cor re late with the older i.e.
Małopolanian Inter gla cial (Ma) (Fig. 5). There fore, the till youn ger than this inter gla cial can not rep re sent the Mid dle Pol - ish Gla ci ation (glaciations) as hith erto con sid ered (Rühle, 1969; Ruszczyńska-Szenajch, 1976), and cor re sponds rather to the Sanian 1 Gla ci ation (S1), as in the strati graphic scheme of north east ern Po land (Kenig, 1998).
Ac cord ing to Sobolewska (1969) the peat and gyttja ex am - ined in bore hole Ł-105, con tain an inter gla cial for est flora from a cli ma tic op ti mum, with out any ini tial and ter mi nal phases.
She sug gests that, dur ing this inter gla cial, el e va tions were over grown by oak-pine for ests with abun dant ha zel in the un - der growth, while hu mid hab i tats within de pres sions com prised al der, elm and ash for ests with ma ple, spruce and wil low. This spec trum cor re sponds well with the fos sil flora from Ferdynandów, at pres ent con sid ered to be the type lo cal ity of the Ferdynandovian Inter gla cial (F) (Janczyk-Kopikowa et al., 1981; Rzechowski, 1996).
The youn ger Qua ter nary de pos its near Łuków com prise two tills, the lower one of which prob a bly rep re sents the Sanian 2 Gla ci ation (S2) or Wilgian, while the up per cor re sponds to the Odranian Gla ci ation (Wartanian?) and is lo cally bi par tite. The lower till is 2–15 m thick and is the best-de vel oped gla cial unit in the sec tion. The youn ger till con tains in ter ca la tions of gravel and sand, and is lo cally over 20 m thick. Flu vio gla cial sands with gravel and/or flu vial grav els and sands of the Great Inter gla cial (Mazovian sensu lato — M) un der lie it. De pos its of the Odranian (Wartanian?) Gla ci ation (O) or (W?) in Łuków are eroded and a palaeovalley is filled with gravel and flu vial sand of the Lubavian Inter gla cial (Lu). Dur ing the Wartanian (?) Gla ci ation (W?) the re gion oc cu pied an extraglacial en vi ron ment.
Sandy-silty-gravely elluvial and al lu vial sed i ments formed be - tween the Eemian Inter gla cial and the Ho lo cene (E+V+H) oc cur above these de pos its and on the sur round ing tills.
BIAłA PODLASKA-WILCZYN CROSS-SECTION (FIG. 6)
The pre-Quaternary bed rock be tween Biała Podlaska and Wilczyn is rep re sented by Oligocene sand and gravel with glauconite, clay and silt. The old est Qua ter nary de pos its in - clude tills (sub di vided mainly on the ba sis of geo mor phol ogy) in bed rock de pres sions. Tills are over 10 m thick and rep re sent the old est of the four gla cial suc ces sion be low or ganic de pos its of the Mazovian Inter gla cial. They seem to cor re spond to the Narevian Gla ci ation (N) (Lindner, 1988b; Nitychoruk, 1994) and the Narevian in ter val in the strati graphic scheme of north - east ern Po land (Kenig, 1998). In the Biała Podlaska re gion a till is cut by an an cient river val ley, over 15 m deep, infilled with gravel and sands of the Podlasian Inter gla cial (Po). The val ley se ries is over lain with silt and lo cally bi par tite till of the sec ond
Fig. 3. Re sults of palaeomagnetic anal y ses of the youn ger cave de pos its from Kozi Grzbiet near Kielce (af ter Głazek et al., 1977a)
Pre-Pleistocene: 1 — poorly sorted sands with lenses of clay and de bris of lime stones and car bon ate con cre tions; Nidanian Gla ci ation: 2 —
“brecciated” clay com posed of pieces of lam i nated clay, cherry-red in col - our, with car bon ate con cre tions and grains of am phi bole and pyroxene;
Malopolanian Inter gla cial: 3 — yel low-brown sandy clay, with nu mer - ous bone re mains, 4 — yel low-brown sandy clay with bone re mains and snail shells; Sanian 1 and Sanian 2 Glaciations, 5 — fine-grained sand with Scan di na vian ma te rial
gla cial suc ces sion, con nected with the Nidanian Gla ci ation (Ni). The till is 5–8 m thick, and oc curs in de pres sions within the pre-Quaternary bed rock. It cor re sponds to the Nidanian in - ter vals in the strati graphic scheme of north east ern Po land (Kenig, 1998).
In the re gion of Biała Podlaska this till is cut by a youn ger an - cient val ley filled with gravel-sandy de pos its, to 20 m thick and in many cases com prised of two sub se quent gravel-sand-silty com plexes. They rep re sent al lu via of the Malopolanian Inter gla - cial (Ma) of a palaeovalley run ning south-east. Flu vio gla cial sands and a youn ger till of the third gla cial com plex spread widely across the whole (Fig. 6) val ley. This till is 6–10 m thick, con tains Scan di na vian ma te rial along with a large ad - mix ture of frag ments and peb bles of lo cal Cre ta ceous marls and lime stones. It is as cribed to the Sanian 1 Gla ci ation (S1). In the Biała Podlaska re gion the till is cut by a rather shal low (up to 5 m deep) an cient val ley filled with flu vial gravel and sand up to 4 m thick, con tain ing many boul ders. Up wards, these de - pos its pass into an al most con tin u ous ho ri zon of sand, 5–10 m thick, rep re sent ing the fourth gla cial suc ces sion along with the over ly ing till. The till is lo cally up to 20 m thick and con tains much Scan di na vian ma te rial, and is con sid er ably decalcified and plas tic in the up per most part. It was de pos ited by an ice sheet whose dy nam ics fa voured the de vel op ment of ex ten sive and deep glaciotectonic de for ma tion. This ice sheet was con - nected with the Sanian 2 Gla ci ation (S2), be cause its de pos its are di rectly over lain by palaeontologically-dated (palynology, macrofauna and di a toms) lake de pos its of the Mazovian Inter - gla cial (M) in the sec tions Biała Podlaska 2/84 (Krupiński et al., 1988; Marciniak and Lindner, 1995; Marciniak, 1998) and Wilczyn WL 1/92 (Bińka et al., 1997).
The low est palaeoflora at Biała Podlaska rep re sents bo real for ests, suc ceeded by mixed for est dur ing the inter gla cial cli ma - tic op ti mum, with a slight cool ing (PAZ–BP–F — Pinus — Picea — Alnus) in the older part of this op ti mum (Krupiński, 1988). The pre-op ti mal part of the inter gla cial was pre dom i nated by nu mer ous periphytic di a toms within the macrophytes and on the lake bot tom (Fragilaria lapponica, Cymbella diluviana, Am - phora pediculus and Navicula scutelloides), fol lowed by Fragilaria spp. and Cyclotella spp. (Marciniak, 1998). The op ti - mum was marked by a dom i nance of the plank tonic di a toms Aulacoseira (mainly A. ambigua) in di cat ing a rise of wa ter level and lake eutrophication, fol lowed by periphytic, alkaliphilous di - a toms (Fragilaria construens var. venter and F. construens var.
binodis), typ i cal of a lit to ral zone. The post-op ti mal part of the inter gla cial was char ac ter ised by the di a toms Stauroneis, Pinnularia, Neidium and Navicula, tes ti fy ing to shallowing and over grow ing of the lake. Higher flora of the cli ma tic op ti mum in Wilczyn is char ac ter ised by nu mer ous exotics (Parrotia type, Celtis, Buxus, Vitis), with a cli ma tic trend from oce anic to con ti - nen tal con di tions (Bińka et al., 1997).
Some of the for mer deep de pres sions in the Biała Podlaska re gion were later partly filled by sand from extraglacial rivers dur ing the Liviecian Gla ci ation (L). The sands are 10 m thick and lo cally con tain in ter ca la tions of soliflucted tills from nearby morainic pla teaux (Fig. 6). At the foot of such an edge near Biała Podlaska a youn ger lake ba sin was formed, gradually filled with silts, most prob a bly of the Zbójnian Inter gla cial (Z).
In the Biała Podlaska re gion the inter gla cial val ley, lake de - pos its and the an cient morainic pla teau from the Sanian 2 Gla - ci ation are cov ered by up to 15 m of glaciofluvial and ice-dammed de pos its rep re sented by sand, sand and silt, over - lain by till of the Odranian (Wartanian?) Gla ci ation (O or W?).
The till is rather thin (3–6 m), and it has been lo cally re moved by en er getic glaciofluvial flow dur ing the ice sheet re treat. Vast sandur plains and val ley sandurs formed at the ice sheet mar gin that stopped to the north in the vi cin ity of Konstantynów, Komarno and Klonowica (Lindner, 1996, 1997). Some val ley or dead-ice de pres sions were later in cor po rated within the youn ger val ley net work, which in flu enced ac cu mu la tion of sands, silts, peat and or ganic mud from the Lubavian Inter gla - cial to the Ho lo cene (Lu-H).
SMOLARKA PROFILE AND CROSS-SECTION (FIGS. 7 AND 8)
In the vi cin ity of Smolarka near Bereza the pre-Qua ter nary bed rock com prises Neo gene (Ne) sandy de pos its with in ter ca - la tions of brown coal, over lain by clay with in ter ca la tions of sand or with Older Paleogene (Pa) sands on the Cre ta ceous (Cr) marls and lime stones (Fig. 7).
The old est Qua ter nary de pos its in clude clays with ad mix - tures or in ter ca la tions of sand up to 20 m thick, these rep re sent - ing the Varyazhskian cold (vr) (Sanko and Moiseyev, 1996).
Palynological and macrofaunal in ves ti ga tions (Yakubovskaya and Rylova, 1992) showed three pol len phases, typ i cal of a cooler for est de void veg e ta tion, part of the pre-Pleis to cene (Eopleistocene of the Belarussian sci en tists). The low er most pol len phase in cludes cold cli ma tic flora with Selaginella selaginoides, S. helvetica, Potamogeton vaginatus and Betula cf. humilis. In the up per phases, the flora pres ents rather a warmer cli mate with Az ol la interglacialis, Scirpus kreczetoviczii and Stratiotes intermedius. In the sec tion Smolarka-3 (S-3 on Figs. 7 and 8) these de pos its show re versed mag netic po lar ity, thus are lo cated within the Matuyama ep och (Sanko and Moiseyev, 1996).
Fig. 4. Gla cial and glaciofluvial ac cu mu la tion in the west ern part of the Holy Cross Mts. (af ter Głazek et al., 1977a)
These de pos its are cov ered by clay with sand in ter ca la tions and by sand with gravel and over ly ing blue-grey clay with pos - i tive po lar ity typ i cal of the Brunhes ep och, there fore con strain - ing the po si tion of the Brunhes/Matuyama bound ary (Sanko and Moiseyev, 1996). They are up to 6 m in thick (Fig. 7). Ac - cord ing to Belarussian sci en tists they rep re sent the Ruzhanskian warm (rz), de spite the pres ence of varved clays (Velichkevich et al., 1993), in di cat ing de po si tion some dis - tance from the ice sheet. Yakubovskaya and Nazarov (1993) con nect these de pos its with the Smorgonian cool ing (sm?) that is the up per part of the Brest ho ri zon of the Eopleistocene.
According to Sanko and Moiseyev (1996) they are lo cally over
30 m thick and rep re sent the anaglacial (preglacial) part of the Narevian Gla ci ation (Fig. 8). In the Smolarka-3 sec tion they are cov ered by sands with gravel, and higher with sand and till of the Narevian Gla ci ation (nr). The till is from sev eral to over 40 m thick and oc curs at bot tom of a gla cial de pres sion as well as cov er ing an cient morainic pla teaux, though lo cally it has been re moved by youn ger ero sion.
In the sec tion Smolarka-3 the till is char ac ter ised by pos i - tive po lar ity, and is cov ered by clayey silts of the Korchevian Inter gla cial (kch) (Sanko and Moiseyev, 1996). The silts are over lain by a till of the Yaseldinian Gla ci ation (yas), like wise char ac ter ised by pos i tive po lar ity, and up to 20 m thick. In the
Fig. 5. Geo log i cal cross-section in the vi cin ity of Łuków, Siedlce Pla teau (af ter Rühle, 1969), sec tion Ł-105 with palynological data (af ter Sobolewska, 1969), age in ter pre ta tion and strati graphic sym bols (af ter Lindner, 1992)
Cr — Cre ta ceous, Pa — Paleocene, E — Eocene, Ol — Oligocene, Mi — Mio cene, Pl — Plio cene, Pp — pre-Pleistocene, N — Narevian Gla ci ation, Po — Podlasian Inter gla cial, Ni — Nidanian Gla ci ation, Ma — Malopolanian Inter gla cial, S1 — Sanian 1 Gla ci ation, F — Ferdynandovian Inter gla cial, S2 — Sanian 2 Gla ci ation, M — Mazovian Inter gla cial, O (W?) — Odranian (Wartanian?) Gla ci ation, Lu — Lubavian Inter gla cial, E+V+H — Eemian Inter gla - cial + Vistulian Gla ci ation + Ho lo cene; 1 — marl and lime stone, 2 — sandy marl, 3 — clay and silt with sand, 4 — sand with gravel, 5 — sand with in ter ca - la tions of silt and brown coal, 6 — clay, 7 — poorly sorted sand, par tially silty sand, 8 — till with boul ders and peb bles, 9 — fine-grained and silty sand with lenses of gravel, clay and silt, 10 — till with lenses of sands and gravel, 11 — peat and gyttja, 12 — gravel and sand, 13 — sandy tills with lenses of gravel and sand, 14 — fine- and me dium-grained and poorly sorted sand
sec tions Smolarka-3 and Smolarka-13 there are grav els with sands and lake de pos its up to 10 m thick. On the ba sis of palynologic data the low er most part of the lac us trine de pos its in the Smolarka sec tion has been pre vi ously re ferred to the Korchevian Inter gla cial (Makhnach and Rylova, 1986;
Velichkevich et al., 1993). In the light of new palaeobotanic data the fol low ing in ter vals have been dis tin guished in the Smolarka-3 sec tion: Byelovezhian Inter gla cial sensu lato, at pres ent sub di vided into the Byelovezhian Inter gla cial sensu stricto (bl), a small Nizhinian Gla ci ation (nz) and the Mogilevian Inter gla cial (mh) (Sanko and Moiseyev, 1996;
Velichkevich et al., 1997). These de pos its are cov ered by a till of the Berezinian Gla ci ation (br) and by youn ger glaciofluvial sands (Figs. 7 and 8).
POSTOLOVO CROSS-SECTION (FIG. 9)
In the vi cin ity of Postolovo near Bereza (Fig. 1), the pre-Qua ter nary bed rock com prises Cre ta ceous (Cr) marls and lime stones, cov ered lo cally by Palaeogene (Pa) clay, sand and sand with gravel, and Neo gene (Ne) sand with gravel, sand and sand stone as well as clay and mud (Fig. 9).
The old est Qua ter nary de pos its in clude sand and silt with sand and over ly ing gyttja and peat with sand, up to 20 m thick.
Flora from gyttja and peat con tains Late Plio cene taxa
(Potamogeton perforatus, P. praemaackianus, P. pseudorutilus, P. cf. felixi, P. cf. parvulus, Caulinia palaeotenuissima, Scirpus atroviroides), taxa linked with the be gin ning of the Pleis to cene (Eleocharis praemaximoviczii, Carex paucifloroides, Hypericum pleistocenicum), as well as taxa of ex otic flora, thus cor re lat ing the or ganic de pos its to the Korchevian Inter gla cial (kch) (Velichkevich et al., 1993).
The youn ger Qua ter nary de pos its in the Postolovo re gion in - clude three tills sep a rated by sands (Fig. 9). They are to 50–60 m thick, and ac cord ing to Velichkevich et al. (1993) rep re sent the Lower Qua ter nary (gQ1) with the Yaseldinian Gla ci ation (yas) in cluded. The lower till, 10 m thick, fills a gla cial de pres sion. It lies di rectly on the Cre ta ceous rocks and is cov ered by sands 15 m thick. The mid dle till is also pre served within the same de - pres sion, as well as ly ing on the Neo gene de pos its in the north - ern part of the cross-sec tion (Fig. 9). The cov er ing sands are 40–80 m thick. On the north ern slope of the de pres sion, the up - per most till is un der lain by clays 6 m thick. The till is up to 20 m thick and oc curs in all bore holes of the cross-sec tion (Fig. 9), most deeply within the de pres sion and more shal lowly in the north ern part where it con tains a clay xe no lith.
Lo cally in the north ern part of the de pres sion there are silts with sands above the till, while in the re main ing area the till is cov ered by up to 70 m of sand, in the re gion with a till to 18 m thick and reach ing the sur face (Fig. 9). The up per part of this
Fig. 6. Geo log i cal cross-section in the vi cin ity of Biała Podlaska (af ter Lindner and Marciniak, 1998), sec tion 2/84 of the Mazovian Inter gla cial de pos its with palynological data of Krupiński (Krupiński et al., 1988) and di a tom data of Marciniak (1998), sec tion WL 1/92 of the Mazovian Inter gla cial de pos its with palynological data of Bińka (Bińka et al., 1996)
Ol (?) — Oligocene, N — Narevian Gla ci ation, Po — Podlasian Inter gla cial, Ni — Nidanian Gla ci ation, Ma — Malopolanian Inter gla cial, S1 — Sanian 1 Gla ci ation, F — Ferdynandovian Inter gla cial, S2 — Sanian 2 Gla ci ation, M — Mazovian Inter gla cial, L — Liviecian (?) Gla ci ation, Z — Zbójnian (?) Gla ci ation, O (W?) — Odranian (Wartanian?) Gla ci ation, Lu-H — Lubavian Inter gla cial-Holocene; 1 — sand and gravel with glauconite as well as clay and silt, 2 — tills (older), 3 — gravel and sand (flu vial), 4 — flu vial and glacifluvial sand, 5 — glacifluvial sand, gravel and silt, 6 — clays and silts, 7 — lake marl and gyttja, 8 — silts, 9 — bi tu mi nous silt and shale, 10 — sand and silt, 11 — till (youn ger), 12 — sand and silt, peat and or ganic mud
suc ces sion shows two lenses of lake marl and peat, 4–6 m thick, in the cen tral and north ern part of the cross-sec tion. The or ganic de pos its yield flora (i.e. Picea, Larix, Pinus silvestris, Abies alba, Juniperus communis, Betula alba, B. humilis, Alnus cf. glutinosa, Carpinus cf. betulus, Sambucus racemosa), which along with re mains of ex otic flora sug gest cor re la tion of these de pos its to the Al ex an drian Inter gla cial (al) (Velichkevich et al., 1993). There fore, the cov er ing sands of the up per most part of the se ries seem to rep re sent flu vio gla cial de po si tion of the fol low ing gla ci ation (Dnieperian?).
COMPARISON REMARKS
The data pre sented and re cent cor re la tion of the Pleis to cene de pos its in Po land and Belarus (Lindner and Yelovicheva, 1998; Lindner and Astapova, 2000) sug gest biostratigraphical
cor re la tion of the lake de pos its of the Mazovian and Al ex an - drian interglacials. In the area stud ied this is par tic u larly the case for the closely spaced sites of Biała Podlaska and Gvoznitsa (Fig. 1), es pe cially on the ba sis of palynological data (Krupiński, 1995).
Com par a tive di a tom in ves ti ga tions of Po land car ried out in sites with lake de pos its from the Mazovian Inter gla cial (Marciniak, 1998) and the Al ex an drian Inter gla cial of Belarus (Khursevich and Fedenya, 1998) re vealed sig nif i cant di ver sity, re sulting from in flu ence of cli ma tic and eco log i cal changes dur ing this inter gla cial. All sites yield char ac ter is tic di a tom taxa (i.e. Cyclotella comta var. lichvinensis, C. vorticosa) that are in di ca tors of both the Mazovian and the Al ex an drian interglacials. In both cases the lake de pos its are youn ger than tills from the Sanian 2 (=Berezinian) Gla ci ation.
In the area ana lysed tills of this gla ci ation cover older, sim i - larly correlable lake de pos its of the Ferdynandovian and the Byelovezhian Inter gla cial (sensu lato). In mid-east ern Po land,
Fig. 7. Geo log i cal cross-section in the vi cin ity of Smolarka near Bereza (af ter Sanko and Moiseyev, 1996), sup ple mented by S-3 and S-13 sec tions with palaeobotanical data
Cr — Cre ta ceous, Pa — Paleogene, Ne — Neo gene, vr — Varyazhskian cold, rz — Ruzhanskian warm, sm — Smorgonian cold (Narevian preglacial), nr
— Narevian Gla ci ation, kch — Korchevian Inter gla cial, yas — Yaseldinian Gla ci ation, bl — Byelovezhian Inter gla cial, nz — Nizhinian cool ing (Gla ci - ation?), mh — Mogilevian Inter gla cial, br — Berezinian Gla ci ation; 1 — brown coal (Ne), 2 — peat, 3 — silty gyttja, 4 — peaty gyttja, 5 — fine-grained sand, 6 — poorly sorted sand with gravel, 7 — silt, 8 — clayey silt, 9 — till, 10 — clay with sandy in ter ca la tions, 11 — clay with sand, 12 — clay, 13 — marl and lime stone
apart from sec tion Ł-5 from the Łuków re gion (Figs. 1 and 5), de pos its of the Ferdynandovian Inter gla cial have been de - scribed from Ferdynandów, Podlodów and Falęcice (Fig. 1).
The pol len suc ces sion of the Ferdynandów Inter gla cial is char - ac ter ised by small amounts of spruce. Oak and elm pre vail at first dur ing the op ti mum, fol lowed by a dom i na tion of ha zel, along with small quan ti ties of lin den, and spo radic oc cur rence of horn beam and yew, while fir plays a cru cial role. The sec ond warm ing in the up per part of the type sec tion at Ferdynandów re sulted in the de vel op ment of a de cid u ous for est with horn - beam (Janczyk-Kopikowa, 1963, 1991).
Di a tom anal y sis from the type sec tions of the Ferdynandovian Inter gla cial from Ferdynandów and the Byelovezhian Inter gla cial from Krasnaya Dubrova (SE Belarus) car ried out in tan dem with the palynological sub di vi sion in di - cated the pres ence of a rich di a tom flora from the two cli ma tic op tima at Krasnaya Dubrova and a lack of di a toms in the up per, youn ger cli ma tic op ti mum at Ferdynandów. The sim i lar tax o - nomic com po si tion of the dom i nant di a tom spe cies, the high con tent of shared taxa (ca. 80%) and oc cur rence of ex tinct taxa in both sec tions (i.e. Cyclotella reczickiae, C. reczickiae var.
diversa, Stephanodiscus peculiaris, S. niagarae var. insuetus),
Fig. 8. Sec tion S-3 and palaeomagnetic data at Smolarka near Bereza (af ter Sanko and Moiseyev, 1996)
D° — dec li na tion, I° — in cli na tion; 1–12 ex pla na tion see Figure 7, 13 — mag netic po lar ity (a — nor mal, b — vari able, c — re versed)
typ i cal for the Byelovezhian and Ferdynandovian interglacials, in di cate that the microflora are of the same age (Khursevich et al., 1990). In lake de pos its from Podlodów and Falęcice, di a - toms have been sim i larly noted only in the lower, older cli ma tic op ti mum of the Ferdynandovian Inter gla cial (Marciniak, 1991;
Lindner et al., 1991). Palynological and di a tom stud ies at these sites sug gest (Janczyk-Kopikowa, 1963, 1991; Khursevich et al., 1990; Marciniak, 1991; Lindner et al., 1991) that the lake de pos its are of the same age as de pos its of the Byelovezhian Inter gla cial sensu lato at Smolarka in west ern Belarus (Fig. 1) where di a toms are ab sent.
Palynological data from Borki (Fig. 1) sug gest the lac us - trine inter gla cial de pos its there be long to the Byelovezhian Inter gla cial sensu stricto (Bogomolova et al., 1985). Di a toms from Borki in clude Cyclotella reczickiae et var. diversa, C.
comta (C. radiosa) var. pliocaenica et var. lichvinensis (Yakubovskaya et al., 1991, Velichkievich et al., 1997), found also in the lower part of the sec tion at Krasnaya Dubrova which cor re sponds to the Byelovezhian Inter gla cial.
From a biostratigraphical point of view, the three main parts of this inter gla cial (lower op ti mum, cool ing and up per op ti - mum) are re ferred in Belarus (Makhnach et al., 1982; Nazarov, 1995; Velichkevich et al., 1996; Velichkevich et al., 1997) to the Byelovezhian Inter gla cial sensu stricto, the Nizhninian
cool ing (mi nor gla ci ation) and the Mogilevian Inter gla cial, re - spec tively (Fig. 10). The lake de pos its of the Ferdynandovian = Byelovezhian Inter gla cial sensu lato, are youn ger than tills of the Sanian 1 (=Yaseldinian) Gla ci ation.
Biostratigraphical cor re la tion of the lake de pos its of the Mazovian Inter gla cial in Po land with the lake de pos its of the Al ex an drian Inter gla cial in Belarus and cor re la tion of de pos its of the Ferdynandovian Inter gla cial in Po land with de pos its of the Byelovezhian Inter gla cial sensu lato in Belarus sug gest that the un der ly ing gla cial de pos its are of the same age. There fore, the two youn ger South Pol ish Glaciations (Sanian 2 and Sanian 1) should cor re spond in Belarus to the Berezinian Glaciations sensu lato (Berezinian sensu stricto and Yaseldinian re spec tively).
De ter mi na tion of the strati graphic po si tion of the older inter gla cial and gla cial de pos its of the gla cial Pleis to cene in Po - land and Belarus is more com pli cated. Thus, flo ral suc ces sion from lake de pos its at Przasnysz (Fig. 1) may be re garded as sim i lar to the suc ces sion in the Mazovian Inter gla cial or in Inter gla cial IV of the Cromerian com plex in the Neth er lands, while flora from Przasnysz in Po land and Korchevo in Belarus can not in di cate the same strati graphic set ting (Mamakowa, 1998). Based on these as sump tions and on anal y ses from Kozi Grzbiet in Po land and Postolovo in Belarus, the Korchevian
Fig. 9. Geo log i cal cross-section in the vi cin ity of Postolovo near Bereza (af ter Velichkevich et al., 1993)
Cr — Cre ta ceous, Pa — Paleogene, Ne — Neo gene, kch — Korchevian Inter gla cial, yas — Yaseldinian Gla ci ation, br — Berezinian Gla ci ation, al — Al - ex an drian Inter gla cial; 1 — marl and lime stone, 2 — clay with sand, 3 — sand and sand stone, 4 — clay, 5 — silt with sand, 6 — till, 7 — lake marl, 8 — gyttja and peat, 9 — sand with gravel, 10 — sand
Inter gla cial in Belarus should be re garded as an equiv a lent of the Malopolanian Inter gla cial in Po land. This in ter pre ta tion is sup ported by sim i lar fau nal re mains in de pos its of the Korchevian Inter gla cial in Belarus (Motuzko, 1985) and the Malopolanian Inter gla cial in Po land, as pointed out by Nazarov (1995).
Older still is the Nidanian Gla ci ation in Po land, re garded as the first South Pol ish Gla ci ation, which is cor re lated on the ba - sis of palaeomagnetic data with the Gla cial A in the Neth er - lands (Lindner, 1991). In the Smolarka-3 sec tion in Belarus (Fig. 7) silts of the Korchevian Inter gla cial (Sanko and Moiseyev, 1996) and in the Smolarka-13 sec tion (Fig. 7) sand at depth 38.4–42.0 m are un der lain by a till, palaeomagnetically youn ger than the Brunhes/Matuyama bound ary. This may cor - re late with the Narevian Gla ci ation (Sanko and Moiseyev, 1996). In the nearby site of Postolovo, this till is bi par tite and fills a gla cial de pres sion. There fore, only the lower ho ri zon of this till pos si bly rep re sents the Narevian Gla ci ation, while the up per one cor re sponds to the till from Smolarka which, youn - ger than the Brunhes/Matuyama bound ary, may cor re late with the Nidianian Gla ci ation in Po land.
In Po land the till of the Narevian (=Linge? or Menapian) Gla ci ation (Lindner and Siennicka-Chmielewska, 1998) is sep - a rated from the till of the Nidanian Gla ci ation by inter gla cial de pos its from Kijewice near Przasnysz (Bałuk, 1991). Or ganic de pos its from Ceteń (Fig. 1), oc cur ring be yond the limit of the Narevian Gla ci ation, may be re garded as its equiv a lent, which, ac cord ing to Lindner (1992), rep re sents the Podlasian Inter gla - cial (Fig. 10) along with the de pos its from Kijewice. Or ganic de pos its con tain ing the re cently dis cov ered Augustovian flo ral
suc ces sion (Janczyk-Kopikowa, 1996; Ber et al., 1998) may also oc cupy the same strati graphic po si tion. The age of this suc - ces sion cor re sponds ei ther to the Bavelian Inter gla cial (Leerdam) or to the Cromerian II (Westerhoven) al though such cor re la tion is ten ta tive (Ber, 2000; Marks, 2000). So far, this suc ces sion has not been noted in Belarus.
CONCLUSIONS
The data pre sented and is sues dis cussed show that age de ter - mi na tion of the old est Scan di na vian glaciations in mid-eastern Po land and west ern Belarus re quires fur ther biostratigraphic and palaeomagnetic in ves ti ga tions of the preglacial and Pleis to cene de pos its. Cor re la tions have been es tab lished only for the two youn ger South Pol ish Glaciations (Sanian 2 = Berezinian sensu stricto and Sanian 1 = Yaseldinian) and the Ferdynandovian (=Byelovezhian) Inter gla cial which sep a rates them. Dating of the older South Pol ish Gla ci ation (Nidanian), of the old est gla ci - ation (Narevian) and of the pre ced ing inter gla cial re quires fur - ther stud ies in the gla ci ated and the extraglacial area, in clud ing de tailed palaeomagnetic re search of thick Pleis to cene de pos its in NE Po land and NW Belarus in the for mer and of loess sec tions in SE Po land and NW Belarus in the lat ter.
Nev er the less, we con sider that the Nidanian Gla ci ation was a dis tinct (first) South Pol ish Gla ci ation, and that it oc curred slightly above or at the Brunhes/Matuyama bound ary (780 ka), cor re spond ing to Gla cial A in the Neth er lands. There fore, the youn ger inter gla cial should cor re spond to the Cromerian II
Fig. 10. Ten ta tive cor re la tion of gla cial and inter gla cial units of the older Pleis to cene in cen tral-eastern Po land and south west ern Belarus 1 — till, 2 — sites with inter gla cial de pos its, 3 — flo ral re mains, 4 — fau nal re mains
(Westerhoven = Małopolanian = Korchevian), Cromerian III (Rosmalen = lower op ti mum of the Ferdynandovian = Byelovezhian sensu stricto) and Cromerian IV (Noordbergum
= up per op ti mum of the Ferdynandovian = Mogilevian) of the Dutch re search ers (Zagwijn, 1989, 1996). Fur ther more, we do not ex clude that the hith erto as sumed range of the Scan di na - vian ice sheet dur ing the old est (Narevian) gla ci ation in west ern Belarus may be iden ti fied as the Nidanian Gla ci ation. The range of the old est gla ci ation (Narevian) was smaller there, re - stricted prac ti cally to the pres ent-day interfluve of Narew and Yaselda (Fig. 1). It should be sep a rated from the South Pol ish glaciations by the Cromerian I (Wardenburg) Inter gla cial, de - pos its of which, along with the Bavelian com plex, oc cur be low the Brunhes/Matuyama bound ary (Zagwijn, 1996) and dis play neg a tive mag netic po lar ity. An other pos si bil ity sug gests that dur ing the old est (Narevian) gla ci ation, the Scan di na vian ice
sheet ad vanced into mid-east ern Po land and south west ern Belarus in sev eral dis tinct lobes, and so its range and sed i ments may be re stricted to an cient gla cial de pres sions, mainly of ero - sional or i gin. The anal y sis of sev eral tens of cores and geo logic cross-sec tions through the Pleis to cene de pos its in mid-east ern Po land and south west ern Belarus (Lindner and Astapova, 2000) re veals that tills of the Nidanian Gla ci ation typ i cally rep - re sent the old est gla cial ho ri zon out side these de pres sions i.e.
on bur ied mor pho log i cal el e va tions.
Ac knowl edge ment. This work formed part of pro ject BW-1484/6 “Stra tig ra phy of the Qua ter nary in mid-eastern Eu - rope” (L. Lindner) and of the Pol ish-Belarussian In ter gov ern - men tal Pro ject “Bio- and lithostratigraphy of Qua ter nary de pos its of cen tral and east ern Po land and west ern Belarus” (B.
Marciniak, G. K. Khursevich and A. F. Sanko).
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