Early Vistulian vegetation history and climate change at Gutów (Wielkopolska Lowland) from pollen analysis

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Early Vistulian veg e ta tion his tory and cli mate change at Gutów (Wielkopolska Low land) from pol len anal y sis

Małgorzata MALKIEWICZ

Malkiewicz M. (2010) – Early Vistulian Veg e ta tion his tory and cli mate change at Gutów (Wielkopolska Low land) from pol len anal y sis.

Geol. Quart., 54 (3): 357–366. Warszawa.

Pol len as sem blages in peat and silt de pos its from a core drilled at Gutów, Wielkopolska Low land, have been ana lysed, enabling char ac - ter iza tion of the de vel op ment of veg e ta tion and of palaeoenviromental change. The pol len anal y sis shows phases with for est and open veg e ta tion com mu ni ties al ter nat ing in re sponse to cli mate changes. The age of the suc ces sion can be re lated to the stadials and interstadials of the Early Vistulian.

Małgorzata Malkiewicz, De part ment of Palaeobotany, In sti tute of Geo log i cal Sci ences, Uni ver sity of Wrocław, Cybulskiego 34, PL-50-205 Wrocław, Po land, e-mail: malgorzata.malkiewicz@ing.uni.wroc.pl (re ceived: May 20, 2010; ac cepted: Sep tem ber 29, 2010).

Key words: Wielkopolska Low land, Early Vistulian, pol len anal y sis, his tory of veg e ta tion, cli mate changes.

INTRODUCTION

The be gin ning of the Last Gla cial (the Early Weichselian) and the end of the Eemian Inter gla cial are in ter vals of spe cial in ter est, show ing the de vel op ment of plant com mu ni ties and of cli ma te change with out in flu ence by hu man ac tiv ity. In ves ti ga - tions of ice cores from Green land and of sea floor sed i ments from the North At lan tic have occasioned con tro versy con cern - ing the palaeoclimatic de vel op ment of the last gla cial-inter gla - cial cy cle (Dansgaard et al., 1993; Grootes et al., 1993; Tay lor et al., 1993; McManus et al., 1994). Palaeobotanical and iso - tope in ves ti ga tions in Ger many (Litt et al., 1996) sug gest that the Eemian Inter gla cial was rel a tively sta ble with marked cli - mate os cil la tions only dur ing the Last Gla cial (the Early Weichselian). Most palynological in ves ti ga tions from Eu rope sug gest that the last inter gla cial was an un in ter rupted warm in - ter val with a ma jor oscillation in win ter tem per a tures dur ing the mesocratic part of the inter gla cial (Menke and Tynni, 1984;

Frenzel, 1991; Zagwijn, 1996).

Palynological data from Early Vistulian Gla ci ation time in the Wielkopolska Low land is scanty. 14 sites are known in this area of Po land, of which the ma jor ity rep re sent an in com plete Early Vistulian suc ces sion (Tołpa, 1952; Janczyk-Kopikowa, 1965; Kuszell, 1980; Kozarski et al., 1980; Klatkowa, 1990;

Tobolski, 1991; Klatkowa and Załoba, 1991; Malkiewicz,

2002; Fig. 1). Only two sites from the Konin area (Tobolski, 1991; Stankowski and Nita, 2004) rep re sent the full Early Vistulian suc ces sion pre ceded by a con tin u ous Eemian suc ces - sion. In the neigh bour hood of the Wielkopolska Low land there are 9 fur ther sites, of which only 4 rep re sent all stadial and interstadial pe ri ods of the Early Vistulian (Jastrzębska- Mamełka, 1985; Mamakowa, 1989; Balwierz, 2003). How - ever, in the sites in Domasłów (Rotnicki and Tobolski, 1965), Wołów (Kuszell, 1980), Zofiówka (Kuszell, 1997), Dziadowa Kłoda and Szklarka (Kuszell and Malkiewicz, 1999; Kuszell et al., 2007) an in com plete suc ces sion of cold and warm phases of the Early Vistulian has been doc u mented.

At the be gin ning of the 21st cen tury sub se quent sites were de scribed which, ex cept for the Eemian Inter gla cial, com prise a sig nif i cant part of the Last Gla cial (Weichselian) (Balwierz, 2003; Granoszewski, 2003; Kupryjanowicz, 2005, 2008).

How ever, there are still few sites with a con tin u ous Eemian-Vistulian suc ces sion, and each is im por tant for un der - stand ing the de vel op ment of veg e ta tion, cli mate and stra tig ra - phy of the Late Pleistocene.

Dur ing field work car ried out in the early 1990’s for the De - tailed Geo log i cal Map of Po land (1:50 000 scale, Skalmierzyce sheet) sev eral cores of biogenic de pos its were ob tained (Boniecki and Jeziorski, 2000). The age of these was paly no logi cal ly es ti mated as rep re sent ing the Eemian Inter gla - cial and the Early Vistulian (Balwierz, 1993; Kuszell and

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Sadowska, 1994; Noryśkiewicz, 1995; Malkiewicz, 2002, 2003, 2008).

Es pe cially in ter est ing was the pro file from Gutów, with 5.7 m-thick inter gla cial de pos its, over lain by 2 m of Vistulian (Weichselian) Gla ci ation de pos its (Kuszell and Sadowska, 1994). Due to the in com plete sam pling no at tempt was made at de tailed biostratigraphic anal y sis of this suc ces sion. In 2006, though, palynological anal y sis of the Eemian Inter gla cial de - pos its from Gutów was car ried out (Malkiewicz, 2008). This showed not only the full inter gla cial suc ces sion, but also the de clin ing part of the Mid dle Pol ish Glaciations (Saalian). At the same time, palynological and biostratigraphical re search of the over ly ing Weichselian de pos its began. The re search aimed to in crease knowl edge of the palaeoenvironmental and cli ma tic con di tions of the im me di ate fore land at the max i mum limit of the Vistulian (Weichselian) Gla ci ation ice sheet.

In this pa per are described the re sults of palynological stud - ies of the biogenic de pos its rep re sent ing the fi nal phase of the Eemian Inter gla cial and the Early Vistulian, and com par i son of those with de pos its of the same age from adjacent areas.

THE AREA INVESTIGATED:

GEOLOGY

The site of Gutów (N 51°45’42”, E 17°52’10”) is lo cated on the Kalisz Up land in the south ern part of the Wielkopolska Low land (Kondracki, 2001), about 20 km to the west of Kalisz (Fig. 1).

In the area in ves ti gated, the Pleis to cene de pos its rep re sent sev eral gla ci ation pe ri ods. De pos its of the South Pol ish Gla ci - ation (Elsterian) are the old est Pleis to cene de pos its in the area (Boniecki and Jeziorski, 2000). They are found in de pres sions in the Neo gene de pos its near Miedzianówka, Czekanów, Czachor and Czechel. Lo cally they di rectly over lie Lower Neo - gene strata (Fig. 2). No de pos its rep re sent ing the Mazovian Inter gla cial (Holsteinian) were found in the area in ves ti gated.

De pos its of the Mid dle Pol ish Glaciations (Saalian): Krznanian and Odranian with Warta Stadial (for merly Odranian and Wartanian Glatiation) (cf. Lindner and Marks, 1999; Lindner, 2005; Ber et al., 2007) are pre served lo cally as flu vio gla cial de - pos its and till. The till thick ness var ies from 2 m be tween Macewo and Kucharki to over 30 m in the vi cin ity of

358 Małgorzata Malkiewicz

Fig. 1. Sites of the Early Vistulian Gla ci ation flo ras in Wielkopolska Low land and in the vi cin ity (Łódź Up land, Lower Silesia) 1 – Gutów (Malkiewicz, 2008), 2 – Grudzielec Nowy (Malkiewicz, 2002), 3 – Kalisz (Tołpa, 1952), 4 – Kazimierz (Tobolski, 1991), 5 – Jóźwin (Tobolski, 1991), 6 – Mikorzyn (Stankowski and Nita, 2004), 7 – Władysławów (Tobolski, 1991), 8 – Kaliska (Janczyk-Kopikowa, 1965), 9 – Emilianów (Klatkowa and Załoba, 1991), 10 – Zagajew (Klatkowa, 1990), 11 – Ustków (Klatkowa and Załoba, 1991), 12 – Raki (Kuszell, 1980), 13 – Lechitów (Malkiewicz, 2002), 14 – Stare Kurowo (Kozarski et al., 1980), 15 – Zofiówka (Kuszell, 1997), 16 – Imbramowice (Mamakowa, 1989), 17 – Wołów (Kuszell, 1980), 18 – Dziadowa Kłoda (Kuszell and Malkiewicz, 1999; Kuszell et al., 2007), 19 – Szklarka (Kuszell and Malkiewicz, 1999), 20 – Domasłów (Rotnicki and Tobolski, 1965), 21 – Kuców (Balwierz, 2003), 22 – Zgierz-Rudunki (Jastrzębska-Mamełka, 1985), 23 – Łanięta (Balwierz, 2003)

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Czekanów. The Eemian Inter gla cial is rep re sented by up to 13 m of sands and lac us trine silt near Czekanów, as well as silt, peat and gyttja doc u mented from a subglacial trough in the area of Grudzielec Nowy–Bieganin and from hol lows formed by melted dead-ice scat tered across the up land. The hol lows are up to sev eral dozen metres in di am e ter and 10 m deep (Gutów and Kwiatków). When the re gion in ves ti gated was a prox i mal part of the gla cier fore land dur ing the Vistulian (Weichselian) Gla ci ation, flu vio gla cial sed i ments up to 25 m-thick were de - pos ited. Silt that fills the subglacial trough to the west of the site in ves ti gated and some of the de pres sions on the up land is of the same age. The Ho lo cene de pos its com prise mainly flu vial sand and gravel of flood plains and peat to 0.5 m-thick in the river val leys.

The palaeolake in Gutów, from which the ana lysed pro file was taken, is lo cated a few metres to the east of the geo log i cal sec tion Sobótka–Gutów–Miedzianówek (Boniecki and Jeziorski, 2000; Fig. 2). The ba sin was small and with out out - flow. It formed as a re sult of dead-ice melt ing dur ing the Warta Stadial – the fi nal stadial of the Odranian (Late Saalian) Gla ci - ation (for merly Wartanian Glatiation; cf. Lindner and Marks, 1999; Lindner 2005; Ber et al., 2007). The depth of the ba sin was about 10 metres.

A core for pol len anal y sis, mea sur ing 8.5 m, was ob tained, com pris ing peat and, or ganic and min eral silt (Ta ble 1). These sed i ments are un der lain by clayey silts and boul der clay of the

Warta Stadial – the stadial of the Odranian (Saalian) Gla ci ation (cf. Lindner and Marks, 1999; Lindner, 2005; Ber et al., 2007).

The top of the pro file com prises fine sands with gravel and clayey sands, dat ing from the Vistulian (Weichselian) Gla ci - ation. The de pos its from the depths from 10.70 to 5.40 m were pre vi ously the fo cus of palynological anal y sis (Malkiewicz, 2008). This pa per pres ents the re sults of pol len anal y sis of peat and silt from the depth in ter val 2.20 to 5.30 m.

MATERIAL AND METHODS

56 sam ples were col lected for palynological anal y sis. Peat and or ganic silts were boiled in 10% KOH, while sam ples with a con sid er able con tent of min eral ma te rial (silt and sand) were treated with con cen trated hy dro flu oric acid for 24 hours. Sub - se quently the ma te rial was mac er ated us ing Erdtman’s acetolysis (1960). Pol len spec tra were counted on two or three slides. On av er age a to tal of 800–1000 sporomorphs was found in each sam ple. The re sults of pol len anal y sis are shown on the pol len di a gram (Fig. 3). The per cent age cal cu la tions are based on the to tal sum (AP + NAP), which in clude trees, shrubs (AP) and her ba ceous plants (NAP). Aquatic, swampy plants and spore plants were ex cluded from the to tal sum. POLPAL palynological soft ware was used to make the per cent age pol len di a gram (Nalepka and Walanus, 2003).

Fig. 2. Geo log i cal cross-sec tion NW–SE in the vi cin ity of the Gutów site (from Boniecki and Jeziorski, 2000)

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RESULTS

The re sults of pol len anal y sis from Gutów are shown in a pol len di a gram (Fig. 3). In this, nine lo cal pol len as sem blage zones (L PAZ) were dis tin guished ac cord ing to cri te ria sub mit - ted by Janczyk-Kopikowa (1987). A de scrip tion of each zone is given in Ta ble 2.

The pol len spec tra of the se quence from Gutów are cor re - lated with chronostratigraphic units dis tin guished for Po land by Mamakowa (1989), for the Konin re gion by Tobolski (1991) and for north west ern Eu rope by Behre (1989) (Ta ble 3).

VEGETATION HISTORY AND CHRONOSTRATIGRAPHY

Lo cal pol len zone GUT 1, rep re sented by two sam ples, is char ac ter ized by a dense pine for est with birch (Betula).

Among trees an im por tant role is played also by spruce (Picea) and al der (Alnus). Trees and shrubs char ac ter is tic of warmer inter gla cial zones oc cur in slight amounts. The sig nif i cant pres - ence of her ba ceous plants (above 20.0%) as well as the ap pear - ance of Betula nana and Juniperus in di cate de te ri o ra tion of the cli mate and the be gin ning of the veg e ta tion changes in the area in ves ti gated. This veg e ta tion suc ces sion can be cor re lated with the his tory of the end of Eemian Inter gla cial. Zone GUT 1 cor - re sponds to re gional pol len zone E 7 by Mamakowa (1989) and the Pinus zone by Tobolski (1991). The up per bound ary of the GUT 1 Pinus L PAZ represents the Eemian–Vistulian Gla ci - ation bound ary. The cri te ria of this bound ary def i ni tion match those ap plied by Andersen (1961), Zagwijn (1961) and Mamakowa (1988). It is placed where a rise in the herb pol len val ues in di cates the de cline of dense for est and the for ma tion of more open com mu ni ties with a fairly marked pro por tion of dif - fer ent heliophytes.

The veg e ta tion in pol len zones GUT 2 and GUT 3 in di cates a se vere cli mate cool ing. Peat sed i men ta tion con tin ued in the lake ba sin, but the min eral frac tion value was in creased. In zone GUT 2 a with drawal of for est com mu ni ties can be ob - served. The high per cent age of heliophytes shows the spread of open com mu ni ties. This is particulary vis i ble in the 50th sam - ple, where the herb plants per cent age ex ceed 65%. The heliophytic com mu ni ties were rep re sented mostly by Ar te mi - sia, Chenopodiaceae, Helianthemum, Caryophyllaceae, and

Rumex. The high pro por tion of Poaceae pol len points to a spread of grass com mu ni ties. Damp hab i tats were cov ered by Ranunculaceae, Asteraceae, Apiaceae, Thalicrtum, Galium, Equisetum, Polypodiaceae and shrub com mu ni ties with dwarf birch and shrub wil low. The plant com mu ni ties of that time were very poor in trees. Sin gle pines (Pinus) and birch trees (Betula) could build up sparse groups with the oc ca sional ap - pear ance of larch (Larix). The pol len pic ture of zone GUT 3 in - di cates a small change in the veg e ta tion of the ba sin. The in - crease in val ues of Betula pol len and slight de crease in the her - ba ceous plants may re sult from the de vel op ment of sparse for - ests. The ex pan sion of birch in the fi nal stage of this cold pe riod was doc u mented also at a near by site, Zgierz-Rudunki (Jastrzębska-Mamełka, 1985) and at many other sites. It is a re - sult of a more tem per ate cli mate and pre cedes other changes in the plant com mu ni ties. These zones doc u ment a tree less stadial phase and cor re spond to re gional pol len zones EV 1 (Mamakowa, 1989) and Ar te mi sia–NAP (Tobolski, 1991).

These zones rep re sent the Herning Stadial in the strati graphic scheme of north west ern Eu rope (Behre, 1989).

In pol len zones GUT 4 and GUT 5 cli mate warm ing and in - creased hu mid ity is fol lowed by a more con ti nen tal cli mate. In the lake ba sin in ves ti gated peat ac cu mu la tion was con tin ued, but the ad di tion of min eral frac tions was much lower. In zone GUT 4 the de vel op ment of dense birch for est with ad di tion of pine and larch was ob served. The de cline in herb plant pol len shows the scar city of open hab i tats. Shrub com mu ni ties with Betula nana, Juniperus and Salix as well as heliophytic com - mu ni ties with Ar te mi sia, Chenopodiaceae, Helianthemum and Rumex were still pres ent. How ever, their area was very lim ited.

Within zone GUT 4, at a depth of 3.90–3.95 m, a brief cli mate cool ing was ob served. The de crease in val ues of Betula and a higher per cent age of Ar te mi sia, Juniperus and Betula nana in - di cates the ter mi na tion of birch for est ex pan sion and a de vel op - ment of open hab i tat com mu ni ties. Af ter this short ep i sode the cli mate ameliorated, which al lowed the next ex pan sion of birch and also pine at the end of this zone. At the bor der of zone GUT 5 the de vel op ment of birch-pine for ests with an ad di tion of larch was ob served, which later yielded to pine for ests with an ad di tion of birch, larch, spruce and ha zel. The small con tent of herb plants indicates the ex is tence of dense for est com mu ni - ties at that time, with few open hab i tats. In the zone GUT 5 de - cline, peat sed i men ta tion was in ter rupted. Peats grad u ally be - come peaty silts, and subsequently silts with progressively lower or ganic con tents. Increase of the groundwa ter level prob - a bly caused moor un der cut and flood ing, and as a con se quence the sed i ment change oc curred. Lo cal pol len zones GUT 4 and GUT 5 are cor re lated with EV 2 (Mamakowa, 1989) and V-I (Tobolski, 1991). Two main phases can be dis tin guished in the suc ces sion of this interstadial at Gutów. The first (GUT 4) is the dom i nance of birch for est. The sec ond phase (GUT 5) is char - ac ter ized by the de vel op ment and spread of pine for est. The birch phase of the interstadial has been cor re lated by Kupryanowicz (2008) with the Amersfoort Interstadial and the pine phase with the Brörup sensu stricto. Behre and Lade (1986), Behre (1989) and other au thors from Po land (Stankowski et al., 1999; Balwierz, 2003; Kuszell et al., 2007) cor re late both the older and youn ger parts of the interstadial with the Brörup sensu lato.

T a b l e 1 Lithological de scrip tion of the Gutów pro file

Depth [m] Li thol ogy

2.20–2.65 silt

2.65–2.97 silty peat

2.97–7.65 peat

7.65–8.15 peaty silt

8.15–9.15 com pressed silt, brown ish-grey 9.15–9.75 com pressed silt, pale grey 9.75–10.70 loose silt, grey and pale grey

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In zones GUT 6 and GUT 7, as a re sult of con tin u ous cli - mate cool ing and wet ting, re peated re con struc tion of the Gutów area veg e ta tion oc curred. At that time, for est re treated and the land scape opened, with NAP in creas ing to over 70%.

Prob a bly, tun dra with the ad di tion of dwarf birch, ju ni per and shrub wil lows de vel oped in the area. Sand and ex posed hab i - tats were dom i nated by heliophytic com mu ni ties, with an im -

por tant role of Poaceae, Ar te mi sia, Chenopodiaceae, Helianthemum and Caryophyllaceae. An in crease in pol len from thermophilous plants is as cribed to in creased trans port ero sion, and sug gests marked de for es ta tion. The tree less stadial phase (lo cal pol len zones GUT 6 and GUT 7) cor re spond to re - gional pol len zones EV 3 (Mamakowa, 1989) and NAP

morf mar g aid ne lloP .3 .giFwótuG

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(Tobolski, 1991) and rep re sent the Redestall Stadial in the strati graphic scheme of north west ern Eu rope (Behre, 1989).

The veg e ta tion in pol len zones GUT 8 and GUT 9 in di cates subsequent cli mate warm ing. At this time the silt sed i men ta tion was tak ing place in the lake ba sin. Cli mate warm ing en abled the for est com mu ni ties to re-ex pand. In zone GUT 8 the birch

for est of park-tun dra type de vel oped, whereas in zone GUT 9 bo real pine for ests with the ad di tion of birch dom i nated. The im por tant el e ments of these for ests were larch and spruce. A sig nif i cant her ba ceous plant value (45%) sug gest open plant communities in the area.

T a b l e 3 Cor re la tion of the lo cal pol len as sem blage zones from Gutów with the re gional pol len as sem blage zones

of the Eemian Inter gla cial and the Early Vistulian Gla ci ation

Re gional pol len zones from Po land (R PAZ) Mamakowa (1989)

Lo cal pol len zones (L PAZ)

Gutów

Re gional pol len zones (R PAZ) Konin re gion Tobolski (1991)

Chronostratigraphy NW Eu rope Behre (1989)

EV 4 GUT 9 – Pinus–Betula–NAP

GUT 8 – Betula-NAP V-II Odderade Interstadial

Early Vistulian Gla ci ation EV 3 GUT 7 – NAP–Betula nana–Juniperus

GUT 6 – NAP–Pinus NAP Rederstall Stadial

EV 2 GUT 5 – Pinus–Betula

GUT 4 – Betula–Pinus V-I Brörup Interstadial

EV 1 GUT 3 – NAP–Betula–Juniperus–Betula nana

GUT 2 – NAP–Juniperus–Betula nana Ar te mi sia–NAP Herning Stadial

E 7 GUT 1 – Pinus E-III Pinus Eemian Inter gla cial

T a b l e 2 De scrip tion of the lo cal pol len as sem blage zones from the Gutów sec tion

Lo cal pol len as sem blage zones

L PAZ Depth

[m] De scrip tion of L PAZ

GUT 9 – Pinus–Betula–NAP 2.40–2.20

AP dominantes, with the max i mum shares of Pinus 39.0% and Betula 13.0%.

Juniperus reaches 1.0%, Larix and Salix 0.8% and Betula nana 0.5%. Ulmus, Quercus, Corylus, Alnus, Carpinus and Tilia pres ent. Picea in crease to 2.5%.

In the NAP group, the high est pro por tions are those of Cyperaceae (16.5%), Poaceae (14.5%) and Ar te mi sia (8.0%).

GUT 8 – Betula–NAP 2.50–2.45

Betula pol len (34.0%) is dom i nant. The fol low ing pol len of other trees oc curs:

Pinus (max. 25.0%), Picea (2.0%), Carpinus (1.4%), Corylus (1.3%) and Larix (0.8%). There are sin gle pol len grain of Betula nana, Salix

and Juniperus. Val ues of NAP de crease to av er age 37.9%.

GUT 7 – NAP–Betula nana–Juniperus 2.70–2.55

The val ues of NAP reach 75.2%, the high est pro por tions be ing those of Cyperaceae (38.0%), Poaceae (28.0%) and Ar te mi sia (7.5%). The max i mum val ues are reached by Betula nana 2.5% and Juniperus 2.1%. Of AP the high est

val ues are those of Betula (17.0%) and Pinus (14.5%).

GUT 6 – NAP–Pinus 2.90 A marked in crease in the NAP val ues takes place (max. 61.4%). Ar te mi sia, Poaceae and Cyperaceae are dom i nant. The fol low ing of Pinus pol len (20.5%)

and Betula pol len (13.5%) oc curs.

GUT 5 – Pinus–Betula 3.30–2.95 The AP fre quency are high, reach ing av er age 84.4%. Pinus shows a dis tinct in crease while Betula falls. Countinuous pres ence of Juniperus, Betula nana, Salix

and Larix. Val ues of NAP reaches a max i mum of 34.9%.

GUT 4 – Betula–Pinus 4.30–3.35 Betula pol len dom i nates (75.0%), Pinus reach ing 36.0%. Betula nana, Juniperus and Larix pol len less 2.5%. NAP in crease to 33.7%.

GUT 3 – NAP–Betula–Juniperus–Betula nana 4.55–4.40 NAP val ues decrese to av er age 46.8% and in crease value of Betula to 38.0%.

The con tin u ous curves of Betula nana (max. 6.0%) and Juniperus (max. 3.8%) be gin. Pol len of Corylus, Ulmus and Quercus are rarely found.

GUT 2 – NAP–Juniperus–Betula nana 5.10–4.60

NAP val ues in crease to 65.3%. The high est pol len shares are those of Poaceae (to 37.0%), Cyperaceae (to 26.0%) and Ar te mi sia (to 12.0%). Both Juniperus (max. 5.3%), Salix (max. 1.3%) and Betula nana (max. 2.8%) have rel a tively high

val ues. Pinus os cil lates from 6.1 to 28.0% and Betula from 11.0 to 23.5%.

Of other trees, Alnus reaches av er age 4.3% and Picea 2.0%.

Larix, Hippophae and Populus are noted.

GUT 1 – Pinus 5.30–5.20

Pinus pol len dom i nates ab so lutely, reach ing a max i mum of 64.0%. The fol low ing pol len of other trees oc curs: Betula (max. 8.5%), Alnus (max. 3.4%) and Picea

(max. 2.3%). Juniperus, Betula nana, Salix and Larix are pres ent. The up per bound ary of the zone the NAP pro por tion in creases, to 42.0%.

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These zones cor re spond to the suc ces sion of an interstadial char ac ter. This is the youn ger interstadial of the early gla cial of the Vistulian Gla ci ation, rep re sent ing the Odderade Interstadial (Behre, 1989) and EV 4 (Mamakowa, 1989), V-II (Tobolski, 1991).

DISCUSSION

Gutów is the third site in the Wielkopolska Low land, where the full re cord of an Early Vistulian suc ces sion pre ceded by a con tin uous Eemian suc ces sion can be found. Two pre vi - ously-de scribed sites are in the Konin area (Tobolski, 1991;

Stankowski and Nita, 2004). In the neigh bour hood of the Wielkopolska Low land there are 9 fur ther sites, of which only 4 rep re sent all stadial and interstadial pe ri ods of the Early Vistulian (Jastrzębska-Mamełka, 1985; Mamakowa, 1989;

Balwierz, 2003).

For est com mu ni ties of the end of the Eemian Inter gla cial at Gutów were char ac ter ized by the pres ence of horn beam (Carpinus), oak (Quercus), ha zel (Corylus) and lime (Tilia).

They sur vived prob a bly in all of south west ern Po land un til the be gin ning the Early Vistulian. Their pres ence has also been con firmed in other sites in the Wielkopolska Low land (Tobolski, 1991; Kuszell, 1997; Malkiewicz, 2002, 2008;

Stankowski and Nita, 2004), Lódź Up land (Jastrzębska- Mamełka, 1985; Klatkowa and Win ter, 1990; Załoba and Jastrzębska-Mamełka, 1990a, b), Lower Silesia (Kuszell, 1980; Mamakowa, 1989) and West ern Pomerania (Urbański and Win ter, 2005; Win ter et al., 2008). Val ues of Alnus and Picea pol len sug gest that spruce and al der were pres ent in the area in ves ti gated dur ing the fi nal part of the Eemian Inter gla - cial. Alnus was prob a bly build ing al der for est com mu ni ties, still grow ing in the near by Prosna val ley. Spruce is sup posed to ap pear in drier as well as wetter hab i tats. A sim i lar veg e ta - tion land scape has been re corded also in other sites in south - west ern Po land (Kuszell, 1980, 1997; Mamakowa, 1986, 1989; Tobolski, 1991; Malkiewicz, 2002, 2003, 2008;

Stankowski and Nita, 2004).

The pres ent in ves ti ga tions show that there is no doubt about the with draw al of dense for est from the cen tral part of the Wielkopolska Low land dur ing the Herning Stadial. Nev er the - less it is de bat able whether or not pine and birch trees with drew from this area com pletely. The per cent age of AP in Gutów, fluc tu at ing be tween 40 and 58%, con sists al most ex clu sively of Pinus and Betula pol len. The 10% share of pine pol len may mostly re sult from long-distance trans por ta tion, how ever the per cent age of Betula pol len, reach ing 30%, may be ev i dence of isolated birch trees. Even if pines did not grow in the area, they may have been pres ent in the near neigh bour hood. The pres - ence of pine in the early stage of the Herning Stadial in the area of Mikorzyn was not ex cluded by Nita (Stankowski et al., 1999). Tobolski (1991), how ever, doc u mented the pres ence of steppe in the Konin area. The higher sig nif i cance of Pinus and Betula in plant com mu ni ties of that time was doc u mented in sites lo cated south of Gutów (Mamakowa, 1989; Malkiewicz, 2002; Kuszell et al., 2007). It is pos si ble that a part of the pol len in GUT 2 and GUT 3 co mes from redeposition, which is also

in di cated by the sig nif i cant pres ence of Picea and Alnus as well as the other pol len of thermophilous trees. The up land na ture of the site and the low wa ter level in the littoral zone of the lake could have con trib uted to extensive ero sion of the sed i ments de pos ited dur ing the Eemian Inter gla cial. On the other hand, the pres ence of Larix at this time in di cates the ex is tence of the open and well-lit hab i tats. Larch is one of the most light-de - mand ing tree spe cies in the mod er ate cli mate zone. For nor mal growth it re quires a full top light and a good side light (Olaczek, 1986). The vegetation of this stadial, doc u mented in the Gutów spec trum as well as in other spec tra from Cen tral Po land (Jastrzębska- Mamełka, 1985; Tobolski, 1991; Malkiewicz, 2002; Stankowski and Nita, 2004) and south west ern Po land (Malkiewicz, 2002; Kuszell et al., 2007) al lows one to as sume that the cli mate was sub arc tic with some con ti nen tal fea tures.

In Cen tral Po land the av er age July tem per a ture might have varied be tween 8 and 10°C dur ing this pe riod. In sites lo cated more to the west, the av er age tem per a ture of the cold est month de creased per haps to –12°C (Aalbersberg and Litt, 1998).

The pres ent in ves ti ga tions in di cate a short break in the birch for est ex pan sion within the Brörup Interstadial shown by a de - crease in val ues of birch and a slight in crease of NAP. This cold os cil la tion has been re corded in only few pol len di a grams from Po land. So far it has been doc u mented in the Wielkopolska Low land only in the re cord from Mikorzyn (Stankowski et al., 1999), and from the ad ja cent ar eas only in in di vid ual records from the Lódź Up land (Jastrzębska-Mamełka, 1985; Balwierz, 2003) and Lower Silesia (Mamakowa, 1989). This cold cli mate fluc tu a tion has also been re corded from East ern Po land (Kupryanowicz, 1991, 2008; Granoszewski, 2003). This phe - nom e non does not ap pear to be lo cal, be cause it has also been doc u mented in some pro files from West ern Eu rope (Robertsson, 1988; Behre, 1989; Reille et al., 1992; Müller et al., 2003). Dur ing the Brörup, in al most all of Po land, a significant tem per a ture in crease took place, prob a bly to 15°C (Tobolski, 1991; Aalbersberg and Litt, 1998; Granoszewski, 2003). Flora of this in ter val in di cates that the cli mate of Cen tral Po land was bo real, more humid dur ing the first half of the interstadial, and more con ti nen tal dur ing the sec ond. Pine oc - cur rence may sug gest the warm est month mean tem per a ture was above 12°C (Granoszewski, 2003). On the other hand, the occurence of Typha latifolia shows that the July mean tem per a - ture was not lower than 14°C (Tobolski, 1991). This value may even have been higher, if we con sider the pres ence of Larix.

The min i mum July tem per a ture for Larix decidua is 17°C (Granoszewski, 2003). The pol len of Betula nana seem to point to better cli ma tic con di tions and may suggest the ces sa tion of con ti nen tal in flu ence in this zone (Tobolski, 1986). Win ter tem per a tures were still low, at ap prox i mately –13°C in East ern Ger many and West ern Po land. The oc cur rence of Calluna and Larix in most pro files in north west ern Eu rope in di cates that min i mum Jan u ary tem per a tures were around this value and in - di cates pre cip i ta tion was about 400–600 mm (Aalbersberg and Litt, 1998). Only in Great Brit ain the tem per a ture seemed to be higher, up to –6°C. Fol low ing the birch pe riod (depth 3.90–3.95 m) a re turn of open com mu ni ties is ob served. The higher val ues of Ar te mi sia, Poaceae and Chenopodiaceae, as well as the in crease of Betula nana and Juniperus, de pict worse

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con di tions and more con ti nen tal fea tures of the cli mate. In this pe riod the mean July tem per a ture did not fall be low 10°C (Granoszewski, 2003).

The per cent age of NAP ex ceed ing 70% in di cate very marked land scape open ing and non-for est tun dra de vel op ment in the Redestal Stadial. A sim i lar land scape was de tected at Mikorzyn (Stankowski et al., 1999) and Łanięta (Balwierz, 2003). In sites lo cated fur ther south of Gutów (Mamakowa, 1989; Kuszell et al., 2007) the im por tance of her ba ceous plant was lesser. As in the Redestall Stadial, the ab sence of for ests in - di cates that the mean sum mer tem per a tures were around 10°C.

In this stadial the for est com mu ni ties were re placed by her ba - ceous plants. The de vel op ment of a shrub tun dra and the in - crease in val ues of Betula nana in di cate cli mate de te ri o ra tion in the Gutów re gion. The shrub tun dra com mu ni ties with Betula nana in di cate milder con ti nen tal cli mate con di tions (Tobolski, 1986; Bińka and Nitychoruk, 1996). The value be tween 8–12°C in di cated by bee tles for north west ern Eu rope is a good match with the sug gested July tem per a ture of 10°C (Aalbersberg and Litt, 1998).

The palynological in ves ti ga tions of the Gutów sed i ments in di cate the some what dif fer ent char ac ter is tics of the Odderade Interstadial as com par ed to the Brörup and the ex is tence of a short birch ep i sode within it. The Odderade Interstadial, char - ac ter ized by open pine for est dom i na tion, was prob a bly pre - ceded by a short pe riod of open birch park-like for est dom i na - tion. This short birch ep i sode is not eas ily vis i ble in most pol len di a grams. In the Wielkopolska Low land it has been known so far only from one sam ple from Mikorzyn (Stankowski et al., 1999). It is sim i larly de vel oped in Kuców and Łanięta in the Lódź Up land (Balwierz, 2003) and in the Podlasie re gion (Kupryanowicz, 2008). It ap pears that it has also been re corded in one sam ple from Zgierz-Rudunki, but the au thor in cluded this seg ment in the Redestall Stadial (Jastrzębska-Mamełka, 1985). The birch ep i sode is very well doc u mented in Horoszki in Podlasie (Granoszewski, 2003), where mac ro scopic frag - ments in di cate the pres ence of birch for ests at that time. It has also been found in many di a grams from Cen tral Eu rope (Erd, 1973; Menke and Tynni, 1984; Behre and Lade, 1986;

Caspers, 1997). The phe nom e non is not likely to be lim ited only to the area of Po land. The re turn of birch and pine-birch for est in the Odderade Interstadial is an ev i dence of in creas ing

warm est-month tem per a tures to around 15°C. Tak ing into ac - count the pres ence of Typha latifolia and Nymphaea alba, the July tem per a ture may have been 12 to 14°C (Huijzer and Isarin, 1997). The pres ence of larch could in di cate the sum mer tem - per a tures up to 17°C, sim i lar to the Brörup Interstadial con di - tions. The min i mum mean Jan u ary tem per a tures are com pa ra - ble to those of the Brörup Interstadial also (Aalbersberg and Litt, 1998). The high est tem per a ture of the cold est month def i - nitely did not ex ceed 0°C. These con di tions are sug gested by the pres ence of Betula nana. The conterporary range of dwarf birch matches the range of max i mum Jan u ary tem per a ture up to 0°C (Granoszewski, 2003).

CONCLUSIONS

The Gutów pro file com prises one of the lon ger Up per Pleis to cene inter gla cial-gla cial suc ces sions in the Wielkopolska Low land. These in ves ti ga tions con trib ute to the gen eral knowl edge of the nat u ral en vi ron ment of stadial and interstadial pe ri ods of the Early Vistulian in the cen tral part of the Wielkopolska Lowland.

1. The de pos its from Gutów a re cord four cli mate fluc tu a - tions of the Early Vistulian, two stadials – Herning and Redestall – and two interstadials – Brörup and Odderade.

2. Four cli mate changes fol low ing the Eemian Inter gla cial were re corded – from the sub arc tic, con ti nen tal cli mate, through bo real, again sub arc tic, up to again bo real. This in di - cates a tran si tion from a sub arc tic steppe, through for est com - mu ni ties of bo real cli mate to tun dra veg e ta tion, and then again to boreal forest communities.

3. In the Brörup Interstadial a cool ing event has been re - corded.

4. A dif fer ent char ac ter of the Odderade Interstadial com - pared to the Brörup Interstadial was no ticed.

5. The birch phase of the Odderade Interstadial was shorter than the birch phase of the Brörup Interstadial and may sug gest a gen er ally greater continentality of the cli mate.

Ac knowl edg ments. I would like to ex press my grat i tude to Dr A. Szynkiewicz for geo log i cal dis cus sion, Ms J. Maj for lin - guis tic help and Mr K. Moskwa for graphic as sis tance.

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