Up per Pleis to cene palaeoenvironmental changes at the Zwierzyniec site, cen tral Po land
Edyta KALIÑSKA-NARTIŠA1, *, Jan DZIER¯EK2, Krzysztof BIÑKA2, Andrzej BORKOWSKI2, Pawe³ RYDELEK2 and Piotr ZAWRZYKRAJ2
1 Lund Uni ver sity, De part ment of Ge ol ogy, Sölvegatan 12, Lund 223 62, Swe den
2 Uni ver sity of War saw, Fac ulty of Ge ol ogy, ¯wirki i Wigury 93, 02-089 Warszawa, Po land
Kaliñska-Nartiša, E., Dzier¿ek, J., Biñka, K., Borkowski, A., Rydelek, P., Zawrzykraj, P., 2016. Up per Pleis to cene palaeoenvironmental changes at the Zwierzyniec site, cen tral Po land. Geo log i cal Quar terly, 60 (3): 610–623, doi:
10.7306/gq.1280
The pa per pres ents the data on an Eemian–Late Gla cial sed i men tary se quence from the Zwierzyniec site, cen tral Po land. A num ber of bore holes doc u ment one or two or ganic lay ers that oc cur be neath one or two ho ri zons of clayey and silty de pos its of ice-dammed lakes. This study dem on strates to which ex tent the Zwierzyniec site can con trib ute to a better un der stand ing of the palaeoenvironmental changes dur ing the Eemian–Vistulian time-frame in cen tral Po land. To study it, a multi-proxy ap - proach was ap plied, in volv ing: palynological and plant macrofossil anal y sis, study of round ing of quartz grains and mor phol - ogy of their sur face, and in ves ti ga tions of sand min er al ogy and till pe trog ra phy. The re sults show that a till bed is over lain by a sandy se ries cor re spond ing to the gla cial-inter gla cial tran si tion. Ei ther one or two dis tinct peaks of or ganic ac cu mu la tion are ev i denced by peat ho ri zons. The lower ho ri zon re cords spec tra with ha zel and horn beam, and did, there fore, ac cu mu late in the Eemian. Ob served only in some bore holes, the up per peat ho ri zon marks the BrÝrup (or the lower part of the Rederstall stadial) rep re sented by for est-steppe con di tions with patchy mo sa ics of larch and fur ther tran si tion into sedges and her ba - ceous taxa. Lo cal ized in be tween the two peat se quences, the sandy ho ri zon marks a long-last ing ae olian trans for ma tion with weath er ing by frost in the Early Vistulian. Again, sig nif i cant changes of the palaeoenvironmental re gime oc curred, and are man i fested in the one or two ho ri zons of the glaciolacustrine sed i ments. This cor re sponded to the last gla ci ation in the re - gion, when the ice-dammed lakes formed dur ing the Main Stadial.
Key words: pol len, plant macrofossils, glaciolacustrine, Eemian–Vistulian se quence, palaeoenvironment, cen tral Po land.
INTRODUCTION
A se ries of sed i ments of var i ous or i gins and ages oc cur in the War saw re gion, cen tral Po land. The area was cov ered by ice sheets sev eral times dur ing the Qua ter nary. The Wartanian ( MIS 6) ice sheet was the last one (Marks, 2002, 2005a; Marks et al., 2006) and it was fol lowed by the Eemian (MIS 5e) warm - ing. The lat ter re sulted in de po si tion or ganic sed i ments that have been found through out the re gion (Karaszewski, 1972;
Kenig, 1985; Krupiñski, 1986). Al though the area of cen tral Po - land was ice-free dur ing the next Vistulian cold stage (MIS 5d-2), a num ber of cooler-warmer ep i sodes took place (Klatkowa, 1997). Among these ep i sodes, the de vel op ment of an ice-dammed lake in the hypsometrically lower parts of cen - tral Po land (i.e. the War saw Ba sin) are of great palaeoenvironmental sig nif i cance. This mor pho log i cal de pres - sion is an im por tant hy dro graphic junc tion of the ma jor rivers of the Pol ish Low lands, thus fa vour ing lake de vel op ment (Marks,
2005b). Vast flat ar eas typ i cal for ice-dammed lakes pre vail both west and east of War saw (Fig. 1).
Among sed i men tary ho ri zons in cen tral Po land, some of them have a well-es tab lished age con trol and palaeoenviron - mental re con struc tions (cf. Weckwerth et al., 2011;
Dzieduszyñska et al., 2014; Kaliñska-Nartiša and Nartišs, 2016a). Oth ers, in con trast, lack of suf fi cient in ves ti ga tion. To fill the ex ist ing knowl edge gap, we pres ent a new data on the Zwierzyniec se quence doc u mented by a num ber of bore holes drilled in the vi cin ity of Radzymin, 30 km north-east of War saw, dur ing a rou tine geo log i cal sur vey. There fore, this study aims to dis tin guish the sed i men tary-en vi ron men tal sig na ture of the Zwierzyniec se quence and of fers a better un der stand ing of the palaeoenvironmental changes of the re gion. A com bi na tion of two peat ho ri zons sep a rated by fine-grained sands and su per - im posed by varved clay-sandy al ter na tions makes the Zwierzyniec area ideal for a new study on en vi ron men tal his - tory. The pro files span warmer and colder pe ri ods and pro vide a po ten tial in sight into palaeoclimatic changes of the re gion dur - ing the Late Pleis to cene. The lat ter is syn chro nous with the North-Pol ish com plex (MIS 5e-2; Lindner et al., 2013). In our study, we ap ply a multi-proxy meth od olog i cal ap proach in volv - ing palynological and plant macrofossil anal y sis, study of round - ing of quartz grains and mor phol ogy of their sur face, and in ves - ti ga tions of sand min er al ogy and till pe trog ra phy.
* Corresponding author, e-mail: edyta.kalinska-nartisa@geol.lu.se Received: October 15, 2015; accepted: January 20, 2016; first published online: February 22, 2016
THE UPPER PLEISTOCENE SEDIMENTS IN CENTRAL POLAND
Gla cial de pos its of Wartanian (MIS 6) age cover vast ar eas of cen tral Po land and form the higher el e va tions and top o - graph i cally dis tinct morainic pla teaux (Marks et al., 2006). Gla - cial re ces sion re sulted in deg ra da tion of sed i ments (Lindner and Marks, 2012), and fur ther de vel op ment of lo cal ice-dammed lakes. This is doc u mented at nu mer ous sites, i.e.
at Mochty, ca. 40 km north-west of War saw (Marks et al., 1996) and at Plecewice, ca. 50 km west of War saw (Kaliñska, 2015).
In the post-Wartanian land scape, small-sized lakes or/and peatlands pre vailed, where or ganic ac cu mu la tion took place dur ing the Eemian. In cen tral Po land, sev eral sec tions of Eemian or ganic de pos its were paly no logi cal ly doc u mented, i.e.
at Ossów (Sarnacka, 1992), ca. 10 km south of Zwierzyniec (Fig. 2), Komorów (Krupiñski, 1986), Pass (Janczyk-Kopikowa, 1974; Karaszewski, 1974), and at the ¯oliborz subglacial tun nel val ley in War saw (Morawski, 1980; Pietrzykowski, 2011). The Eemian–Vistulian tran si tion with a full re cord of sed i ments rep - re sent ing the Amersfoort, BrÝrup (MIS 5c) and Odderade (MIS 5a) interstadials is doc u mented by the pro files at the Zgierz–Rudunki (Jastrzêbska-Mame³ka, 1985), Kub³owo (Ro - man and Balwierz, 2010) and Ustków (Ko³aczek et al., 2012) sites, all of them lo cated west of War saw (Fig. 1). It is also well es tab lished that dur ing the Eemian–Vistulian tran si tion the periglacial pro cesses dom i nated in the higher el e va tions, with lim ited ac cu mu la tion of the sed i ments in the val leys and in - creased slope-driven pro cesses (Ro man et al., 2014). Sim i larly, a sig nif i cant ice ad vance (MIS 4) in north ern Po land (Wysota, 2002; Dzier¿ek, 2009; Marks, 2012; Dzier¿ek and Szymanek, 2013) in ten si fied periglacial pro cesses in the extraglacial area of Po land (Dzier¿ek and Stañczuk, 2006; Ro man et al., 2014).
Dur ing the Last Gla cial Max i mum (LGM), the ice sheet blocked river val leys and the War saw ice-dammed lake de vel oped (Marks, 2012). Af ter the fi nal drain age of the ice-dammed lake,
Fig. 1. Location map showing the main glacial limits during the Late Vistulian in Poland and adjacent areas (adopted from Marks, 2012)
Ga – Gardno Phase; Le – Leszno Phase, Pz – Poznañ Phase, Pm – Pom er a nian Phase, Main Vistulian ice-dammed lakes (grey) and lo ca tion of se lected Eemian and Vistulian or ganic pro files (af ter Bruj and Ro man, 2007): B – B³onie, G – Go³ków, H – Horoszki, I – I³ów, K – Kub³owo, O – Ossów, P – Piaseczno, U – Ustków, Z – Zakroczym, ZR – Zgierz-Rudunki; black square – area shown in Fig ure 2
Fig. 2. Geomorphology of the eastern Warsaw Basin
a few Vistula River ter races formed, largely cov ered by Late Gla cial dunes (Ró¿ycki, 1967; Baraniecka and Konecka-Bet - ley, 1987; Starkel et al., 2015).
THE WARSAW ICE-DAMMED LAKE
The Zwierzyniec site is lo cated on a vast glaciolacustrine plain named the Radzymin–Marki level. Varved clays of the ice-dammed lake are cov ered by a thin sandy ho ri zon (Fig. 2).
A sim i lar sandy layer cov ers the B³onie level, west of War saw (Kaliñska, 2012). The varved clays of the War saw ice-dammed lake, as es tab lished by Halicki (1933), oc cur also north of War - saw in the Zakroczym area, as well as in Piaseczno and Go³ków, south of War saw (Fig. 1). The up per most ho ri zon of the varved clays is hipsometrically roughly uni form and the varvograms re veal a sim i lar pat tern.
Orig i nally, the War saw ice-dammed lake was po si tioned in the north ern part of the War saw Ba sin (Samsonowicz, 1922).
The spa tial range of the ice-dammed lake var ied from 25 to 130 km in its wid est place, with a com plex shore line and nar row bays stretch ing into the val leys of the trib u tar ies of the Vistula and Narew rivers (Fig. 1). Its de vel op ment was cor re lated with the Mid dle Pol ish Gla ci ation (MIS 6; Lencewicz, 1927; Halicki, 1933; Ró¿ycki, 1967).
The dis cov ery of peat ho ri zons in ter ca lated with sands at the B³onie site (Janczyk-Kopikowa, 1974; Karaszewski, 1974) and sands with organics at the Ossów site (Sarnacka, 1982) changed the ice-dammed lake age-model rad i cally. This or - ganic se quence oc curs di rectly be neath the varved sed i ments and ap peared to be of Eemian age. Such in ter pre ta tion po si - tioned the ice-dammed lake in the Vistulian Gla ci ation.
As yet, very few di rect age de ter mi na tion of the ice-dammed lake ex ists. A very early thermoluminescence (TL) study yielded an age of 44 ka (Prószyñska-Bordas et al., 1988). This placed the War saw ice-dammed lake in the mid dle part of the last (Vistulian) Gla ci ation (Baraniecka and Konecka-Bet ley, 1987), and con tra dicted the gen eral palaeo geo graphi cal out - line, be cause no di rect re cord of the gla ci ation have been found in cen tral Po land at that time. Only the P³ock lobe of the Vistulian ice sheet, cor re lated with the Poznañ Phase at 19–20 ka (Marks, 2012) and lo cated ca. 100 km west of War - saw, could dam up the wa ter. If it is true, the War saw ice-dammed lake de vel oped at 19–20 ka. A sim i lar large ice-dammed lake oc curred also in the vi cin ity of Grodno (Belarus) in a sim i lar palaeogeographic po si tion (Fig. 1), and was linked by Marks and Pavlovskaya (2007) with the max i - mum ad vance of the Late Vistulian ice sheet.
Giv ing con fi dence to the above-men tioned in ter pre ta tions, the varved de pos its from bore holes and out crops in the vicintity of War saw do not rep re sent one glaciolacustrine depositional event in one ice-dammed lake as stated pre vi ously. The tec - toni cally af fected de pres sion-like area of the War saw Ba sin fa - voured, there fore, sev eral gla cially-controled ice-dammed lakes. An ac cu rate de ter mi na tion of the age and dis tri bu tion of the War saw ice-dammed lake re mains, how ever, de bat able.
METHODS
To de ter mine the palaeoenvironmental re cord, 10–20 m long sed i ment cores and a few tens of metres apart from each other were ac quired in the Radzymin area. The H-15 50 cm drill with a 9 cm in ner tube di am e ter cham ber as sem bled on a UAZ452 chas sis was used. Ad di tion ally, drillings were also per -
formed with a hand au ger. This al lowed rec og ni tion of one to two peat in ter vals, as well as one or two glaciolacustrine ho ri - zons. The elec tri cal re sis tiv ity tomograph (ERT) was tested across the pro file and de tails can be found in Kowalczyk et al.
(2015).
The four bore hole logs (Zw 1–4) were ex am ined for (1) palynological and plant macrofossil ev i dence in peats and gyttjas, (2) round ing of quartz grains and char ac ter of their sur - face to gether with their min eral con tent in sands, and, fi nally, (3) pe trog ra phy of grav elly frac tions in the tills. The de tails on those are given in the fol low ing sub-chap ters.
ORGANIC SEDIMENTS
Plant pol len and macrofossil data can be used to re con - struct cli mate vari a tions dur ing de po si tion of peat (cf. Kalnina et al., 2015) and, there fore, were em ployed in our study. A to tal of 25 sam ples of ca. 3 cm thick and 5 cm in di am e ter were avail - able for palaeobotanical sur vey: 1 for the gyttja layer (960 cm) in the Zw-1 bore hole, 3 for peats (1000–1030 cm), and 3 for the gyttja layer (1160–1190 cm) in the Zw-2 log, 5 for the up per peat layer (415–430 cm), and 11 for the lower peat layer (815–855 cm) in the Zw-3 log (Ta ble 1), and fi nally 2 for or ganic mat ter (560 and 1730 cm) in the Zw-4 bore hole. In ev ery pol len sam ple, hy dro flu oric acid and the stan dard Erdtman acetolysis were ap plied. Ap prox i mately 1000 pol len grains per sam ple were counted. Prior to the macrofossil anal y sis, the sam ples were boiled in 10% KOH so lu tion. Oc ca sion ally, boil ing had to be re peated due to a high de gree of peat com pac tion pre vent - ing sam ple dis so lu tion. Plant macrofossils were also ex tracted by wet siev ing on a 200 µm mesh screen.
CLASTIC SEDIMENTS
Quartz is ubiq ui tous in nearly all clastic sed i ments and its grain round ing and char ac ter of its sur face are of great im por - tance in de ter mi na tion of the en vi ron ment in which the grain has been trans ported and pre served (Vos et al., 2014). Sim i larly, the min eral com po si tion of clastic sed i ments can be a pow er ful tool in as cer tain ing i.e. min er al og i cal ma tu rity and sed i ment sources (Muhs et al., 2013). Hav ing two clastic (fine me dium-grained sand) ho ri zons, we can clas sify round ing of quartz grains and char ac ter of their sur face and de ter mine their min eral com po si - tion. Pre lim i nar ily, two sandy sam ples from depths of 6.7 and 10 m (Zw-3) in two grain-size frac tions (0.5–0.8 and 0.8–1.0 mm) were ana lysed. The clas si fi ca tion of the grain shape and the sur - face char ac ter was done ac cord ing to the Cailleux (1942) method mod i fied by Mycielska-Dowgia³³o and Woronko (1998) and ac com pa nied with depositional en vi ron ments ac cord ing to Woronko et al. (2015). Six groups of grains were de ter mined: (1) RM – well-rounded frosted (long-term abra sion in ae olian en vi - ron ment), (2) EM/RM – par tially-rounded and frosted (short-term abra sion in ae olian en vi ron ment), (3) EL – well-rounded shiny (long-term trans for ma tion in flu vial/beach en vi ron ment), (4) EL/EM – par tially-rounded and shiny grains (short-term trans for - ma tion in flu vial/beach en vi ron ment), (5) C – bro ken with at least 30% of the orig i nal grain sur faces (crush ing in all types of en vi - ron ments), and (6) NU – fresh, an gu lar. Within the lat ter, the fol - low ing sub groups were dis tin guished: (i) NU/L shiny grains with sharp edges that re sult from crush ing and abra sion in a gla cial en vi ron ment (Woronko et al., 2015), and (ii) NU/M – out wardly frosted grains with sharp edges with out ef fect of trans port. The NU/M grains could cor re spond with “other” group as es tab lished
by Woronko et al. (2015) and ex posed to, e.g., a periglacial en vi - ron ment. How ever, in our stud ies these grains are only of non-rounded out line and are, there fore, sim i lar to quartz grains ob served by Kaliñska-Nartiša et al. (2015) in ae olian set tings of Lith u a nia. Sub se quently, min eral-petrographic com po si tion was de ter mined from both the 0.5–0.8 and 0.8–1.0 mm frac tions, as the amount of quartz in creases in the de pos its due to nu mer ous redeposition events (Mycielska-Dowgia³³o, 2007). A ran dom se - lec tion of 200–250 grains was made and four groups were dis tin - guished: quartz, feld spars, par ti cles of crys tal line rocks, and micaeous min er als.
MORAINIC TILL
Morainic till was found in sev eral bore holes at a depth of 17–18.5 m (Fig. 3). Two till sam ples were taken for petrographic anal y sis from the Zw-2 and Zw-3 bore holes. Be cause of the low fre quency of gravel, we took ad di tional sam ples from other nearby bore holes (Zw-com bine). Be cause the petrographic anal y sis al lows a prompt ex am i na tion of the ver ti cal petrographic differenation of tills (WoŸniak and Czubla, 2015), we con sider it as an ad e quate tech nique in our study. The de - pos its were wet-sieved to ob tain only the 5–10 mm gravel frac - tion. The num ber of grav els var ied be tween 64 and 345 (Ta - ble 2). The re la tion of crys tal line rocks, Pa leo zoic lime stones, dolomites, quartzites, quartz) was used for cal cu la tion of the petrographic in di ces (O/K, K/W, A/B), where: O – to tal of sed i - men tary rocks, K – to tal of lithic frag ments and quartz, W – to tal of car bon ate rocks, A – to tal of non-re sis tant rocks, B – to tal of re sis tant rocks (Ta ble 2). Ad di tion ally, the re la tion be tween Pa - leo zoic limestons and dolomites (Wp/Dp) was also counted.
De tails of the meth od ol ogy can be found, e.g., in WoŸniak and Czubla (2015). The val ues of petrographic in di ces have been ana lysed with re gard to re gional char ac ter is tics (lithotype) of the tills (Lisicki, 2003).
RESULTS
LITHOLOGY
At Zwierzyniec the fol low ing units can be clas si fied in the bore - holes (Fig. 3). The fine-grained 0.4–1.0 m thick sands lie di rectly un der the pres ent-day soil ho ri zon. Sands are un der lain by one (in the Zw-1, Zw-2 and Zw-3) or two (in the Zw-4) glaciolacustrine ho - ri zons: brown-grey varved clays sep a rated by a thin sandy layer, or a sandy silt layer on top of varved clays. Varves rep re sent nu - mer ous al ter na tions be tween the dark grey to brown and light grey laminae to wards the top of the pro file. The thick ness of a sin gle varve lamina var ies be tween 0.1 and 1.5 cm, how ever, no di rect cor re la tion be tween col our and thick ness was ob served. Lo cally, the brown laminae in ter ca lates with the dark grey laminae. Deeper in the pro file, un der the glaciolacustrine se quence, one (in the Zw-2) or two (in the Zw-1 and Zw-3, Zw-4) peat ho ri zons oc cur.
The up per peat layer is 0.9–1.4 m thick and is doc u mented in the Zw-1 and Zw-3. Sands with or ganic frag ments oc cur in the Zw-4.
Be neath the up per peat layer, there is a thick (up to 4 m) grey fine-grained sandy layer. The lower layer of peat is 2–3 m thick. In the Zw-4 pro file, an ad di tional peat layer was doc u mented be - tween a 13.0–14.5 m depth, un der lain by 4.5 m thick gyttja (Fig. 3).
Thin lay ers of gyttja be neath the peat lay ers were also drilled in the Zw-1 and Zw-2. The or ganic-rich sed i ments are un der lain ei ther by me dium-grained sands (Zw-4) or grey morainic till (Zw-2 and Zw-3).
PALAEOBOTANICAL STUDIES OF ORGANIC SEDIMENTS IN THE ZW-3
Three lo cal pol len as sem blage zones (LPAZ) and five lo cal macrofossil zones (LMZ) were dis tin guished in the Zw-3 pro file based on vi sual eval u a tion.
LOCAL POLLEN ASSEMBLAGE ZONES
In the lower part of peat (sam ples 6–16; 814–854 cm depth), LPAZ Z-1 was dis tin guished (Fig. 4 and Ta ble 1). This zone is char ac ter ized by the high num ber of pol len grains, that de creases slightly to wards its top. The pol len of pine and, to a lesser ex tent, birches be come com mon among trees. The lower sam ples from the zone re veal the oc cur rence of Picea, Alnus and Calluna vulgaris as well as sin gle pol len of de cid u ous trees. Ad di tion ally, pol len grains of Buxus are noted within the lower part of the pro file. How ever, Betula nana pol len is pres ent at the top of the zone (Fig. 4)
LPAZ Z-2 is dis tin guished in the up per peat of the Zw-3 pro - file (sam ples 3–5; 420–430 cm depth). In this zone, the pol len fre quency in di cates the ex is tence of for est patches. The ar bo - real pol len (AP) is dom i nated by pine and, to a lesser ex tent, by birch and larch. A high and in creas ing amount of the non-ar bo - real pol len (NAP) is caused by the sedges (Cyperaceae).
These rep re sent lo cal veg e ta tion.
The up per peat of the Zw-3 pro file at a depth of 414–420 cm (sam ples 1–2) rep re sents the LPAZ Z-3 zone, in which the pol - len re veals a rel a tively low fre quency. The AP, dom i nated by birch and pine, falls rap idly to about 50%. There is a scant re - cord of Larix, Juniperus and Salix. Among the NAP, grasses and sedges are abun dant. In part, how ever, they are un doubt - edly lo cal in or i gin. Ar te mi sia, Chenopodiaceae and a large num ber of her ba ceous taxa are also dis tinc tive for this zone.
POLLEN ANALYSIS OF THE OTHER SAMPLES
Sam ple from a depth of 560 cm from sand with or ganic mat - ter in the Zw-4 pro file (Figs. 3 and 5) shows a tree less phase (some what sim i lar to that of LPAZ Z-3 in the Zw-3 pro file;
Fig. 4). How ever, a ho ri zon with a pol len spec trum abun dant in Quercus, Corylus and Pinus pol len is found in gyttjas at a depth of 1730 cm in the same pro file. Sam ples taken from the peat layer in the Zw-2 pro file (Fig. 5) show that the pol len spec tra from a depth of 1000–1020 cm are dom i nated by horn beam, and from a depth of 1030 cm by ha zel with an ad mix ture of horn beam (R 2 LPAZ). In gyttja at depths of 1160, 1180, 1190 cm we have doc u mented the pres ence of ha zel pol len with a low amount of Tilia and Alnus (R 1 LPAZ). Fi nally, sam ple from gyttja at a depth of 960 cm in the Zw-1 pro file (Fig. 5) shows a high fre quency of horn beam pol len. The horn beam and oak lev els, noted in the three above-men tioned pro files, rep re sent part of the widely re cog nised cli ma tic op ti mum, in which pol len of plants with a more south erly pres ent-day range have the great est fre quency in the se quence (Biñka and Nitychoruk, 2011).
LOCAL MACROFOSSIL ZONES
The MZ-1 from the Zw-3 pro file (sam ples 10–16;
830–854 cm depth; Fig. 6) shows a low fre quency of Andromeda polifolia, Scheuchzeria palustris, Oxycoccus, Triglochin palustre, Potentilla palustre, Menyanthes tri foli ata, Carex riparia, Cicuta virosa; all of them ei ther in habit raised and tran si tional bogs or form microhabitats in raised bogs (Fig. 6).
Fig. 3. Details on the boreholes of the Zwierzyniec and Ossów area
Macroremains of pine and tree birches as well as plants from dry hab i tats (Arctostaphylos uva-ursi and Rumex acetosella) oc cur reg u larly.
The MZ-2 (sam ples 8–9; 822–826 cm depth) shows a lower va ri ety of taxa than the MZ-1. Betula nana, as well as Andromeda polifolia and Potentilla palustre oc cur abun dantly.
The MZ-3 (sam ples 6–7; 814–818 cm depth) re veals a de - cline of Betula nana (Fig. 7) and Andromeda, and gen er ally has less fre quent re mains than as com pared to the MZ-2. Abun dant pine wood frag ments are noted to wards the top of the zone (Ta - ble 1).
In the MZ-4 (sam ples 3–5; 42–430 cm depth), nu mer ous types of Carex nuts pre vail in the spec tra. Other plants from sub aque ous hab i tats are rare. Only Menyanthes, Potentilla palustre ap pear sin gly. The re mains of pine and tree birches are pres ent in small num bers.
Lastly, in the MZ-5 (sam ples 1–2; 414–418 cm depth), nee - dles of larch, nuts of Betula sect. Albae, Carex rostrata and Stellaria palustris are the most abun dant re mains. Frag mented wood of wil low is sig nif i cant to wards the top of the zone (Ta ble 1).
CLASTIC SEDIMENTS
The num ber of well-rounded frosted (RM) grains var ies be - tween 27 and 32% in the 0.5–0.8 mm frac tion, and 24–38% in the coarser frac tion. This is fol lowed by par tially-rounded frosted (EM/RM) grains that ac count for 18–29% and 23–25%
in the 0.5–0.8 and 0.8–1.0 mm frac tions, re spec tively. The in - ves ti gated sed i ments are, there fore, characterized by abun - dantly ae olian-trans ported quartz grains which both have the high est round ness (RM), and with the signs of ae olian ac tiv ity vis i ble on the edges and cor ners of the grains (EM/RM).
High-en ergy sub aque ous grains reach as high as 4–7%
(well-rounded shiny EL grains), and 11–13% (par tially-rounded shiny EM/EL grains) in the 0.8–1.0 mm frac tion, as well as ca.
8% (EL), and 12–17% (EM/EL) in the 0.5–0.8 mm frac tion. The num ber of bro ken (C) grains, formed from break age of the EL, EM/EL, RM and EM/RM types, is rel a tively high – ca. 16–18%
in both of the frac tions. Both the fresh (NU/L) and weath ered (NU/M) grains oc cur sparsely. How ever, the sam ple from a depth of 10 m con tains ca. 10% of fresh grains (NU/L).
Li thol ogy Sam ple
num ber Depth [cm] Ma te rial LPAZ LMZ
Up per peat 1 2
414 418
4Th (radic.)/2 [trunki et rami salici/II]
4Th (radic.)/2 Z-3 MZ-5
3 4 5
422 426 430
2Th (Sphagn.)/2, 2Th(radic.)/2 4Th (Sphagn.)/2 4Th (Sphagn.)/1
Z-2 MZ-4
Lower peat 6 7
814 818
4Dg [stripes pini]
4Th (radic.)/1 [trunki et rami]
Z-1
MZ-3 8
9
822 826
3Dg, 1Th (radic.)2 [trunki et rami]
2Th (Sphagn.)/2, 2Th (radic.)/1 MZ-2
10 11 12 13 14 15 16
830 834 838 842 846 850 854
2Th (radic.)/1, 2Dg 2Th (radic.)/1, 1Th (Sphagn.)/1,1Dg 3Th (radic.)/1, 1Th (brown mosses,Sphagn.)/1
2Th (Sphagn.)/1, 1Th(radic.)/1, 1Dg 3Th (radic.)/1, 1Dg
4Th (Sphagn.)/1 4Th (Sphagn.)/1
MZ-1
LPAZ – Lo cal pol len as sem blage zones; LMZ – Lo cal macrofossil zones
T a b l e 1 Li thol ogy of peats fol low ing the Tröels-Smith (1955) clas si fi ca tion and the lo cal palaeobotanical
zones in the Zw-3 pro file
Pro file Depth [m] Num ber
of grav els O/K K/W A/B Wp/Dp
Zw-2 17.5–18.0 189 0.49 2.59 0.40 1.33
Zw-3 17.0–17.5 64 0.88 1.36 1.21 0.78
Zw-com bine 17.5–18.5 345 0.67 1.72 0.54 1.61
O – sed i men tary rocks, K – lithic frag ments, W – lime stones (Wp) and dolomites (Dp), A – me chan i cally non-re sis tant rocks, B – me chan i cally re sis - tant rocks
T a b l e 2 Pe trog ra phy of tills at Zwierzyniec
morf margaid nelloP .4 .giFceinyzreiwZ( 3-wZ) morf margaid nelloP .5 .giFceinyzreiwZ( 4-wZ ,1-wZ ,2-wZ)
The high est con tent of quartz (92%) is found in the 0.5–0.8 mm frac tion of the sam ple from a depth of 6.7 m. The 0.8–1.0 mm frac tion and the sam ple from a depth of 10 m seem to be de pleted in quartz con - tent, which var ies from 74 to 80%. Si mul ta neously, a rel a tively high con tent of both rounded feld spars (4–8%) and lithic frag ments (11–20%) are ob served.
No micaceous min er als are found.
THE PETROGRAPHIC CHARACTERISTICS OF TILL
The com po si tion of gravel in all sam ples is dom i - nated by lithic frag ments. The K/W in dex of 2.59 for the Zw-2 pro file (Ta ble 2) is very high and is not com - pat i ble with any tills in the re gion. The low fre quency of lime stones in the fine-gravely frac tion of till can be ex plained by strong weath er ing. The lat ter is sup - ported by the pres ence of Pa leo zoic lime stones and dolomites (Ta ble 2). A high con tent of do lo mite is typ i - cal of the Wartanian tills in cen tral Po land. How ever, the low fre quency of lime stones in tills, which build the bot tom of lakes, is very com mon (D. Ga³¹zka, pers.
comm.).
DISCUSSION
PALAEOENVIRONMENTAL INTERPRETATION OF POLLEN AND MACROFOSSIL DATA
At least two peat lay ers have been dis tin guished in the geo log i cal cross-sec tion in the Zwierzyniec area (Kowalczyk et al., 2015). How ever, the up per peat layer is not pre served in the Zw-2 and Zw-4 bore holes. It was pre sum ably eroded and re placed by fine sand with the high con tent of or ganic ma te rial that could rep re sent an other sed i ment fa cies of the same age (Fig. 3). The lower or ganic layer is rep re - sented by peat and gyttja, which over lie the sandy layer.
Pol len spec tra from the three fragmentarily ana - lysed pro files in di cate the pres ence of pine-oak for est (gyttja at 1730 cm in the Zw-4), for est com mu ni ties dom i nant by ha zel (gyttja at 1160–1190 cm in the Zw-2) and, fi nally, by horn beam (gyttja at 960 cm in the Zw-1).
The LPAZ Z-1 (Zw-3 pro file) pol len con cen tra tion and the low con tent of her ba ceous taxa (ex clud ing lo - cal el e ments) sug gest dense bo real pine for ests that ex isted un til the end of the zone; a wood of pine was iden ti fied in the top most sam ple. There fore, we ob - serve a grad ual de cline of inter gla cial con di tion. This is ex pressed by rare Buxus that re quires more mar i - time cli mate, and sin gle pol len of de cid u ous trees in the lower sam ples (Fig. 4). In the Eemian, Buxus oc - curred in a horn beam zone and per sisted un til the end with Picea, and the be gin ning of the pine phase (Biñka and Nitychoruk, 2011; Biñka et al., 2011;
Mamakowa, 1989; Zagwijn, 2000). More abun dant re mains of Betula nana (Fig. 6) in di cate a pro gres sive de crease in tem per a ture at the end of the zone.
Lo cally, the MZ-1 rep re sents ini tially a veg e ta tion of raised or tran si tional bog over grow ing by Sphag - num moss (Ta ble 1). The more de mand ing plants dom i nate in the hol lows or in small per ma nent and .6 .giFlissoforcaMmorf margaid ceinyzreiwZ( 3-wZ) – h ;sriah – rhedohtadyh ;tiurf– rf ;sf– n2 ;sdees – s ;elcillof – f ;enoc – c ;seldeen – n ;sevael – l ;selacs tiurf– lamgits-owt– n3 ;stun lamgits-eerht ;stun sdioprics– xeraCpuorg seiceps ro suneg ot dengissa-non
tem po rary wa ter bod ies, in clud ing Triglochin, Carex riparia, Menyanthes, Cicuta virosa and Potentilla palustris, as re vealed at a depth of 850–855 cm in the Zw-3. It was rap idly fol lowed by a peat bog with sedge com mu ni ties and of lower wa ter level, be cause the re mains of pine and tree birches were found in situ.
The MZ-2 (820–830 cm in the Zw-3 pro file) rep re sents a suc - ces sive re treat of trees from the bogs, the abun dance of dwarf birch, and its fur ther dis ap pear ance in the next zone (Fig. 6). A sim i lar pat tern is ob served in the Linie rel ict bog in north ern Po - land (Ejankowski and Kunz, 2006), wherein the dwarf birch oc - curs in the dwarf shrub com mu ni ties Ledo-Sphagnetum magellanici, and fur ther re treats. This is caused by a low ground wa ter level, that could po ten tially be trig gered by waterlogging of the ground, as ob served by Ejankowski (2004, 2008). The dwarf birch de cline is re corded at a depth of 815–820 cm in the Zw-3 pro file. A sat is fac tory ex pla na tion of this can not be found at the pres ent stage of re search. Of sig nif i - cance, some plants such as Carex riparia can in di cate an even higher wa ter level. Si mul ta neously, a well-de com posed peat layer with par ti cles of wood sug gests a pe riod of drought.
Through out the pe riod of sed i men ta tion of the up per peat layer, for est rep re sents the iso lated type only in the LPAZ Z-2, where pine dom i nates in com mu ni ties. The lower pol len fre - quency and abun dant her ba ceous plants, es pe cially Ar te mi sia, as so ci ated with steppe veg e ta tion mark open con di tions in the LPAZ Z-3. The pres ence of re mains of tree birches and abun - dant nee dles of larch, how ever, shows the ex is tence of for est. It seems that the veg e ta tion was for est-steppe with patchy mo sa - ics of larch. Abun dant re mains of larch and low per cent ages of its pol len also at tract at ten tion. A very sim i lar pat tern is known from the neigh bour ing Eemian se quence at Horoszki (Fig. 1;
Granoszewski, 2003). Ob ser va tions of mod ern pol len of larch in the Altai Moun tains (Pelánková and Chytrý, 2009) sup port these dis crep an cies and show that the cor re spon dence be - tween Larix pol len in the mod ern spec tra and real tree abun - dance was of ten ten u ous.
The up per or ganic level (MZ-4 and MZ-5) also be gins with a Sphag num peat bog (Ta ble 1), be fore be ing rap idly re placed by tran si tional or minerotrophic mires with many spe cies of sedges, Potentilla palustris, Menyanthes, Stellaria palustris and Carex rostrata. Abun dant larch nee dles and a higher de gree of peat de com po si tion in di cate fre quent ep i sodes when the bog dried up in sum mer.
PRESUMABLE AGE OF THE DEPOSITS
The for ma tion of the lower peat layer and the gyttjas at Zwierzyniec may have started dur ing the Eemian. This is sup - ported by the pres ence of spec tra with ha zel (at a depth of 1160–1190 cm; Zw-2), oak, pine and ha zel (at a depth of 1730 cm; Zw-4) as well as of pol len spec tra dom i nated by horn - beam at a depth of 1000–1030 cm (Zw-2) and at 960 m (Zw-1) rep re sent ing the Carpinus zone (Fig. 5). In the Zw-3 pro file, the lower peat layer (LPAZ Z-1) rep re sents prob a bly part of the fi nal zone of the Eemian. This is sup ported by the oc cur rence of Buxus, low curve of Picea and rare pol len of de cid u ous trees.
The same pat tern has been ob served re gion ally in the nu mer - ous Eemian pol len di a grams in Po land (Granoszewski, 2003;
Kupryjanowicz, 2008; Biñka and Nitychoruk, 2011; Biñka et al., 2011). This pe riod lasted from ca. 1500 to 2000 years (Caspers et al., 2002).
Fol low ing the su per po si tion, the up per peat layer in the Zw-3 pro file at a depth of 414-430 cm (Fig. 4), and the fine ma - te rial with organics in the Zw-4 pro file at a depth of 560 cm (Fig. 5) rep re sent the up per or lower part of the BrÝrup interstadial (LPAZ Z-2 zone), and the first part of the Rederstall stadial (LPAZ Z-3) or the lower part of the BrÝrup and a part of a part of intra-interstadial cold fluc tu a tion.
PALAEOENVIRONMENTAL IDENTIFICATION OF QUARTZ GRAINS
The quartz grain mor phol ogy re lates to the mode of trans - por ta tion, dis tance from source, and tim ing, but it is equally a func tion of the orig i nal grain shape in the par ent rock (Mahaney et al., 2001; Kleesment, 2009; Costa et al., 2013; Kaliñska and Nartišs, 2014; Vos et al., 2014). In this study, a pre lim i nary anal - y sis of the round ness of quartz sand grains and the char ac ter of their sur face com bined with min er al og i cal com po si tion open up great op por tu ni ties for fu ture work at higher res o lu tion. So far, two sed i ment sam ples re vealed a great vari abil ity of grain types, rep re sent ing not only ae olian (RM and EM/RM) and flu - vial (EM/EL) sed i men tary en vi ron ments, but also cracked grains (C) and to tally fresh grains with no traces of trans por ta - tion (NU/L). How ever, the pre dom i nance of matt grains with per fectly spher i cal shapes was noted in par tic u lar in the up per part of the pro file (sam ple taken from a depth of 6.7 m). These grains rep re sent the long-last ing ae olian trans for ma tion. Si mul - ta neously, the abun dance of shiny (EM/EL+EL) quartz grains is at trib uted to flu vial en vi ron ments (Krinsley and Doornkamp, 1973), and such de pos its could be typ i cal of river floodplains (Marks et al., 2014). It is ac knowl edged that a rel a tively high (>5%) num ber of grains with well-rounded out lines ob served in the sed i ments re fer ei ther to the un der ly ing de pos its (Woronko, Fig. 7. Macrofossils from Zwierzyniec (Zw-3)
A – leaf of Betula nana (depth 826 cm in Table 1); B–D – Scheuchzeria palustris: B – ends of leaves with hydathodes (depth
854 cm), C – follicle (depth 846 cm), D – seed (depth 830 cm)
2001) or re sults from the long-last ing flu vial cy cles (Weckwerth et al., 2011). Sim i larly, the high con tent of cracked grains (C) in - di cates the post-sed i men tary weath er ing due to freeze-thaw (Woronko and Hoch, 2011; Woronko, 2012) and have been re - ported from the for mer periglacial ar eas in north east ern Po land (Woronko et al., 2013). It is ap par ent from this study that the tex tures re flect not only the in flu ence of flu vial/ae olian as so ci a - tions by the sup ply of ae olian ma te rial into the river val leys, but also the re work ing of pre-ex ist ing sed i ments, as no ticed within the periglacial zone of the last gla ci ation (Zieliñski et al., 2009;
Velichko et al., 2011). The con tri bu tion of the lat ter could be ex - plained by the pres ence of the un der ly ing morainic com plex.
Note wor thy is the prev a lence of ae olian-type grains in the sam - ple from a depth of 6.7 m; these could only re sult from lon - ger-term ae olian ac tiv i ties caused by in creas ing cli mate arid ity.
The 0.8–1.0 mm quartz grains tend to re veal the stron gest ae - olian abra sion (Mycielska-Dowgia³³o and Dzierwa, 2003). In our study, how ever, sim i lar num bers of both well-rounded (RM) and par tially-rounded (EM/RM) matt grains are ob served and, there fore, it ar gues that ae olian ac tion has no sig nif i cant role in abrad ing the coarser frac tion.
The min er al og i cal ma tu rity, de fined as com po si tion where there is a dom i nance of quartz (Pettijohn et al., 1972), is stated as be ing achieved from ex tended pe ri ods of ae olian ac tiv ity (Muhs, 2004). It is likely, given by the rel a tively large amount of feld spars and lithic par ti cles, par tic u larly in the sam ple from a depth of 10 m, that their source was from a com bi na tion of ig ne ous or meta mor phic rocks. Such a com po si tion ap pears to be sim i lar to the flu vio gla cial sed i ments of cen tral Po land, with 70–75% of quartz, ex clu sively (Mycielska-Dowgia³³o, 1993). Feld spars, how - ever, are mostly of rounded out line, mean ing the whole ma te rial un der went ae olian trans for ma tion (cf. Weckwerth et al., 2011).
The feld spar de ple tion in the sam ple from a depth of 6.7 m was likely over lap ping with the de te ri o ra tion of cli mate con di tions re - corded in the up per part of the pro file.
PALAEOENVIRONMENTAL IDENTIFICATION OF TILLS
Based on the petrographic in di ces of the Zwierzyniec till, it can not un am big u ously be es tab lished whether or not the till is of the Wartanian age. Al though the Wartanian tills have been ob - served in the area (Lisicki, 2003; Marks et al., 2006), our O/K, K/W and A/B petrographic in di ces cor re spond nei ther to the re - gional lithotype for Wartanian till nor the older tills. The cause of this is likely due to a strong weath er ing.
PALAEOENVIRONMENTAL RECONSTRUCTION
The sed i ment cores to a max i mum depth of 20 m at the Zwierzyniec site rep re sent a sed i men tary re cord of the Eemian–Late Gla cial se quence in cen tral Po land. This data com bined with the multi-proxy ap proach ap plied in this study al - low the eval u a tion of the palaeoenvironmental pat tern of the se - quence, which is dis cussed be low.
Based on petrographic com po si tion of the low er most morainic till, we as sume that, al though strongly weath ered, it is prob a bly of Wartanian age. An un even up per bound ary of the till ranges be tween 70 to 74 m a.s.l. Ei ther this is in her ited af ter the pri mary-pre served un even sur face of the morainic pla teaus, or eroded by the proglacial wa ter.
Ac cu mu la tion of fine- and me dium-grained sands post dates the gla cial con di tions. Sands are pre sum ably of flu vial or i gin;
this is sup ported by the abudance of the shiny well- and par - tially-rounded quartz grains (EL+EM/EL) and lack of mica. This
min eral, due to its platy habit (Marcinkowski and Myciel - ska-Dowgia³³o, 2013), con tra dicts with wa ter flow ing con di tions.
The nu mer ously cracked quartz grains co in cide with the gla - cial-inter gla cial tran si tion and could be pos si bly in her ited from the un der ly ing till. The con tin u ous or ganic de pos its, termed as the lower peat, cover the sands. For ma tion of the or ganic de - pos its oc curred prob a bly dur ing the late Eemian, and co in cides with the end of spruce and be gin ning of the pine phase (Mamakowa, 1989; Zagwijn, 2000; Biñka and Nitychoruk, 2011;
Biñka et al., 2011), when con ti nen tal con di tions pre vailed. Lo - cally, the lower peat is re placed by two peat ho ri zons al ter nated by a sandy ho ri zon and un der lain by gyttja (Zw-4; Fig. 3). That com plex com bi na tion can not be ex plained at this stage of re - search. How ever, colder-inter gla cial in ter val can not be ex - cluded. Macrofossil re cord at the Horoszki Du¿e site (Granoszewski, 2003) pro vides the min i mum mean July tem - per a ture es ti mates of 17–18°C, and Jan u ary tem per a tures be - tween –1 and –5°C for the late Eemian (cf. Helmens, 2014).
These are lower than the es ti mates from con ti nen tal Eu rope (Klotz et al., 2003), but slightly higher than in the East ern Bal tic re gion (ŠeirienÅ et al., 2014).
Rapid en vi ron men tal changes are in ferred for the lower peat-sand tran si tion; this is well-doc u mented in all bore holes, where the to tal thick ness of sands be tween the lower and the up per peat is occassionally up to 5 m (Kowalczyk et al., 2015).
In sand the flu vial-ae olian grain mix ing pre vails, giv ing ev i dence of a fluvioperiglacial en vi ron ment (Mycielska-Dowgia³³o and Woronko, 2004). Col lec tively, the cracked (C-type) and ae - olian-type (EM/RM+RM) grains dem on strate in tense frost weath er ing and long-last ing ae olian pro cesses. As such, ae - olian de po si tion is likely to co in cide with stadials of the early Vistulian (MIS 5d and b), when a gen eral trend to wards colder tem per a tures and dryer con di tions in Cen tral Eu rope is ob - served (Brewer et al., 2008); the plant cover sharply de creased and even cold-re sis tant spe cies did not form dense for ests (Novenko et al., 2008). As sum ing the BrÝrup age of the over ly - ing up per peat ho ri zon (see be low), the timeframe of sand de - po si tion can be nar rowed to the cold Herning stadial (MIS 5d), when the flu vial ac tiv ity and ocassionally solifluction pre vailed in Po land (Marks et al., in press). How ever, only a suf fi cient dat ing can stratigraphically po si tion that sandy ho ri zon.
The up per peaty se quence doc u mented in the Zw-1 and Zw-3 pro files is dis con tin u ous. For ex am ple, no peat is re - corded in the Zw-2 and Zw-4 bore holes, which seems to be re - placed by the sandy se ries with or ganic mat ter. A plant re cord of the Zw-3 pro file co in cides with the BrÝrup on set (the LPAZ Z-2 zone), and prob a bly rep re sents ei ther its intra-interstadial cold fluc tu a tion or the first part of the Rederstall stadial (LPAZ Z-3). This stadial is con sid ered to be the cool est pe riod dur ing the Early Vistulian (eirienÅ et al., 2014). A frag men tary na ture of the Zw-3 pro file does not al low stat ing whether the plant re - cord is of intra-interstadial fluc tu a tion or the first part of Rederstall stadial age. How ever, prevalance of pine (LPAZ Z-2) com bined with a strong steppe con ti nen tal phase doc u mented by larch in the LPAZ Z-3 (and sim i lar to that found in the Zw-4;
Fig. 5) sup ports rather the late BrÝrup and the Rederstall stadial age. A sim i lar pol len pat tern, as signed to the BrÝrup on set, has been re ported from cen tral and east ern Po land (Granoszewski, 2003; Biñka and Nitychoruk, 2011; Ko³aczek et al., 2012).
Given the arid con ti nen tal steppe con di tions with larch in the wet ter lo ca tion, the min i mum mean tem per a ture be tween –27 and –34°C and from 16 to 18°C of Jan u ary and July, re spec - tively, to gether with an an nual pre cip i ta tion <400 mm, were es - tab lished (Kuneš et al., 2008). In our study the tem per a tures must have been slightly higher due to the pres ence of Betula.
Meadow steppe for ma tions with patches of Betula pro vided the
tem per a tures be tween 20 and 21°C for July and the an nual pre - cip i ta tion be tween 300–350 mm (Pelánková et al., 2008). Ac - cord ing to Granoszewski (2003) the tem per a tures of the warm - est and the cold est months var ied be tween 15–17°C and –8 to –14°C.Win ter tem per a tures in West ern Eu rope seem to be, in con trast, milder with an an nual preciptitaion of ca. 600 mm (Kühl et al., 2007). The peaty ho ri zon in our study was prob a bly con tin u ous, how ever, eroded par tially by a wa ter flow. This is sup ported by the pres ence of a thin grav elly ho ri zon that oc curs in the over ly ing sandy se quence.
Widely dis trib uted varved clays oc cur in the War saw Ba sin.
Be tween two glaciolacustine ho ri zons a thin 0.5 m thick fine-sandy layer oc curs; this is doc u mented by the Zw- 4 bore - hole and al lows us to es tab lish two phases of ice-dammed lake de vel op ment within the likely short drain age event in be tween.
It is sup ported by lithological differentation of sed i ments in Zw-2 and Zw-3 bore holes. Ow ing to the unique al ter na tion of the inter gla cial/interstadial-gla cial/stadial sed i men tary re cord, the Zwierzyniec se quence al lows us to cor re late the varved clays, and con se quently the ice-dammed lake with the last gla ci ation.
Two damm ing events likely co in cide with the Main Stadial, when the ice po si tioned ca. 100 km west of War saw. The Leszno and Poznañ phases of the max i mum Vistulian ice-sheet ad vance (MIS 2) are of sim i lar range in cen tral Po land (Skompski, 1969; Marks, 2002; Mojski, 2005; Wysota et al., 2009), and can be, there fore, linked with the de vel op ment of the lower and up per glaciolacustrine ho ri zons, re spec tively. The thin sandy ho ri zon re flects a rel a tively short time gap when the ice-dammed lake did not ex ist, which could co in cide with an up to 5 ka dif fer ence be tween the phases, as in di cated by the cosmogenic iso tope ages and cal i brated ra dio car bon data (Marks, 2012).
The to tal thick ness of the glaciolacustrine se quence, as ob - served in Zwierzyniec east of War saw, dif fers sig nif i cantly from west of War saw, wherein 12 to 18 m pro files were ex am ined in Plecewice and I³ów (Fig. 1), re spec tively (Dzier¿ek, 2015).
Thus, the Zwierzyniec site is likely to rep re sent a more pe riph - eral zone of the ice-dammed lake/lakes.
The sandy se quence over lies the varved clays, thus dom i - nat ing the Radzymin–Marki level land scape. The fine-grav elly ho ri zon in the low er most part of the sandy se quence is due to ero sion and grav els, that orig i nate pre sum ably from the ad ja - cent morainic pla teau. The flu vial or i gin of the sands was pro - posed by Sarnacka (1982), and Baraniecka and Konecka-Bet - ley (1987). How ever, west of War saw at the Plecewice site, the ae olian char ac ter of sed i ments pre vails (Kaliñska, 2012). Ad di - tion ally, sandy ae olian-like de po si tion took place at 15–16 ka and 12 ka only 15 km SE of the Zwierzyniec site (Kaliñska-Nartiša and Nartišs, 2016b). A stepwise ice re ces -
sion to gether with si mul ta neous vari a tions in the wa ter level re - sulted in the for ma tion of the ter races of the Vistula River. The Otwock ter race is ad ja cent to the in ves ti gated area (Fig. 2) and con sid ered to have been formed in the Late Weichselian (Vistulian; Baraniecka and Konecka-Bet ley, 1987; Sarnacka, 1992), Af ter sur face dry ing, ae olian ac tiv ity formed dune fields ob served through out the War saw Ba sin (Manikowska, 1982, 1991).
FINAL REMARKS AND CONCLUSIONS
1. This study was the first to pro vide a sed i men tary re cord of the Zwierzyniec site, where two glaciolimnic se - quences are un der lain by two or ganic ho ri zons. The multi-proxy ap proach re veals the Wartanian(?)–Eem - ian–Vistulian se quence, in which the Late Eemian and the BrÝrup seem to be well-ex pressed.
2. The Eemian op ti mum is man i fested in the gyttjas and lower peats; the up per most part of the lower peat, how - ever, re veals grad ual cli mate de te ri o ra tion.
3. The Early Vistulian cli mate, as in ferred from the li thol ogy and the sed i men tary pat tern re corded in the quartz grains, re veals both its de te ri o ra tion and dry ness. This was later fol lowed by the ac cu mu la tion of the up per peat in the warmer BrÝrup.
4. Cli ma tic de te ri o ra tion is char ac ter is tic for the on set of gla ci ation, and thus in di cates ero sion. The up per most part of the up per peaty se quence was there fore eroded, and sub se quently re placed by the sandy ac cu mu la tion.
5. The varved se quence of the Radzymin–Marki level cor - re sponds to the last gla ci ation. A sce nario of the Leszno–Poznañ phases is sup ported by the gen eral palaeo geo graphi cal out line in cen tral Po land.
6. Our study dem on strates to which ex tent the Zwierzyniec pro file can con trib ute to a better un der stand ing of the palaeoenvironmental changes dur ing the Wartan - ian–Eem ian–Vistulian se quence. As such, its fur ther de - tailed ex plo ra tion re mains open.
Ac knowl edge ments. We are grate ful to Dr. M. Nartiës (Uni ver sity of Lat via) for com ments on text and dis cus sion.
A.P. Gumsley (Lund Uni ver sity) is thanked for his Eng lish proof-read ing. Our ap pre ci a tion is ex pressed to Dr. O. Borisova (Rus sian Acad emy of Sci ences), anon y mous re viewer and Dr. W. Granoszewski (Geo log i cal Quar terly) who helped to im - prove our manu script.
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