Palaeo geo graphi cal sig nif i cance of the Eemian biogenic sed i ments at the Bór site (Warta River val ley, cen tral Po land)
Joanna PETERA-ZGANIACZ1, *, Ryszard K. BORÓWKA2, Jacek FORYSIAK1, Gra¿yna MIOTK-SZPIGANOWICZ3 and Dominik PAW£OWSKI4
1 De part ment of Geo mor phol ogy and Palaeo ge ogra phy, In sti tute of Earth Sci ence, Fac ulty of Geo graph ical Sci ences, Uni ver sity of £ódŸ, Narutowicza 88, 90-139 £ódŸ, Po land
2 Ge ol ogy and Palaeo ge ogra phy Unit, Fac ulty of Geosciences, In sti tute of Ma rine and Coastal Sci ences, Uni ver sity of Szczecin, Mickiewicza 18, 70-383 Szczecin, Po land
3 Pol ish Geo log i cal In sti tute – Na tional Re search In sti tute, Ma rine Ge ol ogy Branch, Koœcierska 5, 80-328 Gdañsk, Po land
4 In sti tute of Ge ol ogy, Adam Mickiewicz Uni ver sity, Maków Polnych 16, 61-606 Poznañ, Po land
Petera-Zganiacz J., Borówka R. K., Forysiak J., Miot-Szpiganowicz G. and Paw³owski D. (2013) Palaeo geo graphi cal sig nif i - cance of the Eemian biogenic sed i ments at the Bór site (Warta River val ley, cen tral Po land). Geo log i cal Quar terly, 57 (4):
687–700, doi: 10.7306/gq.1122
An in ves ti gated area is lo cated in the mid dle reach of the Warta River val ley. Dur ing drillings in the Bór site or ganic de pos its such as de tri tal cal car e ous gyttja and cal car e ous de tri tal gyttja has been doc u mented in a depth be tween 14.9 and 16.6 m.
The or ganic de pos its are cov ered by min eral, mostly sandy de pos its. The ac cu mu la tion took place in the small lake formed as an aban doned chan nel. Palynological anal y sis led to the con clu sion that biogenic ac cu mu la tion be gan at the end of Wartanian and took place at least to the Eemian Inter gla cial op ti mum. Re sults of palynological, Cladocera and geo chem i cal anal y ses in di cate wa ter level changes and the in creas ing of the tro phy sta tus of the res er voir. Pres ence of Me so zoic sub stra - tum very close to the palaeolake bot tom in flu enced sig nif i cantly the chem i cal fea tures of the or ganic de pos its. As Eemian or - ganic de pos its are un com mon in the Warta River val ley, the Bór site seems im por tant for palaeo geo graphi cal re con struc tions of the Warta River val ley dur ing Eemian Inter gla cial.
Key words: gyttja, palynology, Cladocera, geo chem is try, Warta River val ley de pos its.
INTRODUCTION
In cen tral Po land, there are a lot of well-doc u mented sites of biogenic sed i ments from the Late Wartanian and Eemian Inter - gla cial (e.g., Klatkowa, 1990; Bruj and Ro man, 2007), which are lo cated in the morainic pla teau, while not nu mer ous were found in river val leys. This sit u a tion pro vides solid back ground for the palaeo geo graphi cal in ter pre ta tion of the pla teaus, but it does not en able a suc cess ful re con struc tion of the river val ley floors of the pe riod in ques tion.
The data pre sented is a con tri bu tion to the knowl edge about the func tion ing of the river sys tem in cen tral Po land dur ing the Eemian Inter gla cial. The Vistula drain age sys tem from that pe - riod is rec og nized much better (Marks and Pochocka, 1999;
Marks, 2005b) than those known from the Odra and Warta rivers. Most of the in for ma tion co mes from drillings, and palaeo - geo graphi cal re con struc tions are based on anal y sis of prop er - ties of the min eral de pos its due to the short age of or ganic ma te -
rial suit able for pol len anal y sis and re li able dat ing (Marks, 2005b). For this rea son each site, where Eemian Inter gla cial or - ganic de pos its are doc u mented is very im por tant and al low us to ver ify the in ter pre ta tion based on min eral ma te rial. It is ob vi ous that the sites where age was de ter mined paly no logi cal ly have the great est value as pre sented in this pa per Bór site or e.g., Krzy¿ówki (Noryœkiewicz, 1999), but the mol lusc anal y sis can be also suf fi cient to con firm Eemian age of fluviolacustrine de pos its (e.g., Skompski, 1983; Sza³amacha and Skompski, 1999; Meng et al., 2009).
Un til re cently, the palaeo ge ogra phy of the mid dle reach of Warta River val ley dur ing Eemian Inter gla cial was re con structed on the base of the min eral, mostly sandy de pos its (Czarnik, 1972; Trzmiel, 1996). The sit u a tion has greatly im proved, when lake de pos its and peat have been found in the Krzy¿ówki site, near Ko³o (Sza³amacha and Skompski, 1999) and on the ba sis of palynological data were de ter mined as be long ing to the late gla cial of the Wartanian and the Eemian Inter gla cial (Noryœkiewicz, 1999). Their de po si tion took place in a shal low lake, per haps an ox bow lake, which has grad u ally trans formed into a mire. In ves ti ga tions in the Bór site bring (Fig. 1A, B) new data about the palaeo ge ogra phy of the me rid i o nal sec tion of the Warta River val ley close to Uniejów dur ing the Wartanian ter mi - na tion and Eemian Inter gla cial.
* Corresponding author, e-mail: jap@geo.uni.lodz.pl Received: March 14, 2013; accepted: August 13, 2013; first published online: October 23, 2013
688 Joanna Petera-Zganiacz, Ryszard K. Borówka, Jacek Forysiak, Gra¿yna Miotk-Szpiganowicz and Dominik Paw³owski
GEOLOGICAL SETTING
The Bór site is lo cated in the mid dle sec tion of the Warta River val ley (Fig. 1A), in area where the val ley joins with the War - saw–Berlin ice-mar ginal streamway. Be tween Sarbice and Dobrów it wid ens and reaches a width of sev eral km. The study area lies within the Mid dle Pol ish Glaciations ex tent. Dur ing the Last Gla cial Max i mum the Bór site was sit u ated in an extraglacial zone (Kozarski, 1981; Stankowska and Stankow ski, 1988; Stankowski and Krzyszkowski 1991).
In the Me so zoic sub stra tum of the in ves ti gated area the Adamów graben oc curs. It be longs to the sys tem of grabens of the Konin el e va tion, formed within the Szczecin–£ódŸ–Mie chów Trough (Widera, 1998). Within the graben, thick Neo gene de - pos its, in clud ing brown coal, and Qua ter nary se ries were ac cu - mu lated.
The old est Qua ter nary de pos its are rep re sented by tills and other glaciogenic de pos its of South Pol ish Com plex (based on stra tig ra phy pos tu lated by Ber et al., 2007; Lindner and Marks, 2012), which filled deep ero sional forms de vel oped in the sub-Qua ter nary sur face (Fig. 1D). The up per till of South Pol ish Com plex (prob a bly Sanian 2), are more wide spread and de - formed by glaciotectonic pro cesses. Flu vial sands and sands with grav els rep re sent ing be gin ning of the Mid dle Pol ish Com - plex lie above. Two ho ri zons of the Mid dle Pol ish Com plex tills were found (Czubla et al., 2010). Out side the Adamów graben the tills are thick, and dom i nate the Qua ter nary se ries, while in the graben their thick ness de creases or they are com pletely eroded or/and sep a rated by glaciolacustrine de pos its of the KoŸmin gla cial lake and glaciofluvial sand and grav els (Fig. 1D).
The glacigenic de pos its of the Mid dle Pol ish Com plex form up - lands: morainic and glaciofluvial plains as well as the War - saw–Berlin ice-mar ginal streamway ter races (K³ysz, 1981;
Klatkowa, 1993; Nowacki, 1995; Trzmiel, 1996; Czubla, 2001;
Forysiak, 2005).
Flu vial sands ly ing at a depth of 14–24 m were de scribed as Eemian de pos its by Czarnik (1972) and Trzmiel (1996). The or - ganic sed i ments of Eemian age were rec og nized only at the Bór site. Now a days, the site is lo cated in the wide val ley but in the Eemian, it was lo cated in very dis tal part of the val ley. The bot - tom of the Bór res er voir was close to the Adamów graben east edge (Fig. 1D).
The thick Weichselian al lu via, ex ceed ing lo cally 20 m in thick ness, cover older de pos its (Fig. 1D). Mor pho log i cally, Weichselian de pos its form two lev els: the al lu vial high ter race and lower ter race. The great part of the val ley is oc cu pied by the lower ter race (Fig. 1B). The lower ter race is cut by re mains of the mul ti chan nel river sys tem which de vel oped in the Youn ger Dryas and also func tioned in the Ho lo cene. Some of the chan - nels are still oc cu pied by small streams (Petera, 2002;
Turkowska et al., 2004; Forysiak, 2005).
The Ho lo cene flu vial de pos its usu ally oc cupy nar row frag - ments of the val ley, along the nu mer ous small streams and Warta River. They are rep re sented by sands with silt and al lu vial
clay (Forysiak, 2005). The ae olian sands and dunes oc cur, the most fre quently in the right side of the val ley.
MATERIAL AND METHOD
The or ganic se ries were doc u mented dur ing drillings in the Bór site. There were un der taken drillings around the site (Fig. 1C) to es tab lish their spread and geo log i cal con text. At the Bór site the drill ing reached a depth of 18.5 m, and the ver ti cal pro file is as fol lows:
Depth [m] Li thol ogy 0.0–0.3 sandy soil, brown 0.3–1.1 me dium sand, grey beige
1.1–8.5 me dium and coarse sand, grey beige 8.5–10.0 fine sand with silt, grey beige 10.0–14.0 me dium and coarse sand, grey beige 14.0–14.6 sand with gravel
14.6–14.85 gravel
14.85–16.35 de tri tal cal car e ous gyttja 16.35–16.60 cal car e ous de tri tal gyttja 16.60–16.75 silt mixed with gravel 16.75–17.45 gravel
17.45–17.95 fine and me dium sand with silt 17.95–18.50 till
ANALYSIS OF MINERAL DEPOSITS
21 sam ples of min eral de pos its (Fig. 2) were ex am ined by grain-size anal y sis: sieve and aerometric method (Mycielska-Dowgia³³o, 1995), and stan dard Folk and Ward co ef - fi cients were counted us ing GRADISTAT soft ware. The quartz-grain abra sion anal y sis was per formed for the frac tion 0.8–0.63 mm, us ing mod i fied Cailleux method (Klatkowa, 1991;
Manikowska 1993). More over, the cal cium car bon ate con tent was de ter mine for all min eral sam ples us ing the Scheibler method.
ANALYSIS OF GYTTJA
The gyttja from the Bór pro file was ana lysed by means of pol len, Cladocera, granulometric and geo chem is try anal y ses.
The sam ples from de tri tal cal car e ous gyttja were col lected in in - ter vals of 10 and 5 cm from cal car e ous de tri tal gyttja, within the depth range of 14.9–16.6 m.
The pol len anal y ses were done for 20 sam ples. For the mi - cro scopic in ves ti ga tions the sam ples were pre pared us ing Faegri and Iversen (1978) and Berglund (1979) meth ods. The re sults are pre sented as per cent age pol len di a gram drawn us ing POLPAL soft ware.
The anal y sis of Cladocera was based on 21 sam ples of 1 cm3 vol ume and were pro cessed ac cord ing to the stan dard pro ce dure (Frey, 1986). The tax on omy of cladoceran re mains fol lows that pre sented by Frey (1962) and Szeroczyñska and
Fig. 1. Lo ca tion of the Bór site in Po land with geo log i cal sec tions
A – lo ca tion of the in ves ti gated area in re la tion to ex tents of the ice-sheets (af ter Marks, 2005a); B – geomorphological map (af ter Forysiak, 2005); C – lo ca tion of the bore holes in Bór vil lage; D – geo log i cal cross-sec tion: Cre ta ceous: 1 – marl, 2 – weath ered marl; Neo gene: 3 – clay, silt, sand and lig nite; Qua ter nary, Elsterian: 4 – the old est till and glaciolacustrine silt, 5 – older till and glaciolacustrine silt, 6 – youn ger till;
Saalian: 7 – flu vial sand and grav els; Wartanian: 8 – lower till, 9 – lower glaciofluvial sand and grav els, 10 – glaciolacustrine silt and fine sand, 11 – glaciolacustrine sand and sand with silt, 12 – up per glaciofluvial sand and grav els, 13 – up per till, 14 – gla cial loamy sand; Eemian Inter - gla cial: 15 – gyttja; Weichselian and Ho lo cene: 16 – flu vial sand, sand and gravel, and sand with silt, 17 – ae olian sand
Sarmaja-Korjonen (2007). Eco log i cal pref er ences of cladoceran taxa were de ter mined on the ba sis of White side (1970) and Szeroczyñska (1998).
Sed i ment granulometry and geo chem is try was ana lysed in 21 sam ples. In di vid ual sam ples were freeze-dried in lyophiliser and sam ples were min er al ised in the pro cess of com bus tion (550°C) to cal cu late per cent con tri bu tion of or ganic and min eral parts of each sam ple. The ash pro duced by com bus tion was ana lysed for grain-size re lated and geo chem i cal char ac ter is tics.
Grain-size anal y sis of the min eral part was car ried out in a la - ser analyser which pro cesses sam ples of 300–0.3 mm mean grain-size. Stan dard Folk and Ward co ef fi cients were cal cu lated us ing the GRADISTAT soft ware. Per cent con tri bu tions of in di - vid ual frac tions were cal cu lated as well.
In or der to per form geo chem i cal as says, the ash sam ples were dis solved in Tef lon bombs us ing a mi cro wave mineraliser.
Min er ali sa tion was car ried out in two mi cro wave cy cles: the first one in con cen trated ni tric acid with 2 ml 10% chlor ic acid and the sec ond one in hy dro gen per ox ide. The so lu tion ob tained was ana lysed for con cen tra tions of Na, K, Ca, Mg, Fe, Mn, Cu, Zn, and Pb with atomic ab sorp tion spec trom e try. All the anal y ses were con ducted at the Geo chem i cal Lab o ra tory in Uni ver sity of Szczecin.
Part of the geo chem i cal anal y ses were con ducted in Lab o ra - tory of the Earth Sci ence In sti tute, Uni ver sity of £ódŸ. Twenty sam ples of sed i ment were an a lysed us ing the fol low ing meth - ods: Scheibler vol u met ric method in or der to de ter mi na tion of the car bon ate con tent in the sed i ment, potentiometric method for mea sure ment of pH, con duc tiv ity and volt age.
RESULTS
TEXTURAL FEATURES OF MINERAL DEPOSITS
The till doc u mented at the Bór site has typ i cal tex tural fea - tures: high value of mean grain di am e ter, is poorly sorted, pos i - tive skew ness co ef fi cient and low value of kurtosis (Fig. 2). The quartz grain abra sion is rep re sen ta tive for tills: RM (round mat)
~35%, M (in ter me di ate) ~25% and EL (shiny) ~23% with high con tent of the bro ken grains. The CaCO3 con tent var ies from about 4 to 6%, which is typ i cal as well. The top of the till has sand ad mix ture, is better sorted and neg a tively skewed, prob a bly due to fine frac tion re move. Above, me dium and fine-grained sands with silt oc cur. The de pos its are me dium or poorly sorted, with neg a tive skew ness and CaCO3 con tent of about 4%. These sed - i ments have been clas si fied as glaciolacustrine de pos its of the KoŸmin gla cial lake.
The next se ries con sists of me dium and poorly sorted coarse sand and grav els. The gyttja is un der lain by or ganic-min eral silt with grav els and sand and cov ered by the Weichselian al lu via, rep re sented by sand, sand with grav els, and fine sand with silt (Fig. 2). The con tent of CaCO3 in Weichselian de pos its is low (about 1%) ex cept at the base where it reaches al most 15%. At the base, the quartz grain abra sion is char ac ter ized by a rel a tively small amount of RM grains and a sig nif i cant con tent of EL grains.
At depths of about 8 m the pro por tions of RM and M grains in - crease to wards the top, and reach, re spec tively about 50 and 35%. Con sid er able con tent of wind-abraded grains is typ i cal for Weichselian al lu via, as well for Warta River de pos its (Petera, 2002; Forysiak, 2005).
690 Joanna Petera-Zganiacz, Ryszard K. Borówka, Jacek Forysiak, Gra¿yna Miotk-Szpiganowicz and Dominik Paw³owski
Fig. 2. Li thol ogy and tex tural fea tures of de pos its in Bór site
Mz – mean grain-size, d1 – stan dard de vi a tion, Sk1 – skew ness KG – curtosis, RM – round mat, M – in ter me di ate, EL – shiny, C – crushed, NU – unabraded (fresh)
PROPERTIES OF ORGANIC DEPOSITS POLLEN ANALYSIS
Changes of the per cent age share of taxa in cre ation of veg e - ta tion as so ci a tions in Bór bore hole, al low for the dis tinc tion of six lo cal pol len as sem blage zones (LPAZ), ac cord ing to Janczyk-Kopikowa (1987; Fig. 3).
Pinus–NAP LPAZ (16.48–16.63 m). Pinus (55.3–58.0%) as the dom i nat ing taxon is ac com pa nied by Betula (20.0–26.3%) and in small amounts – Juniperus (0.8%). Of the herbal plants (NAP: 23%) the main constitutents are Cyperaceae and Poaceae and spe cies of steppe-like as so ci a tions (Ar te mi sia, Chenopodiaceae). Pre dom i nance of non-for est as so ci a tions in the veg e ta tion shows that the sed i ments of this zone have been ac cu mu lated dur ing the cold cli mate, prob a bly in the pe riod be - tween the Late Gla cial and the old est Eemian.
Pinus–Betula LPAZ (16.38–16.48 m). A de crease of Pinus to 47.5% and an in crease of Betula + Betula nana up to 42.4% is ob served. The amount of NAP also de creases, es pe cially Cyperaceae, Chenopodiaceae and Ar te mi sia. It in di cates the de vel op ment of birch shrub as so ci a tions and open birch-pine for ests and shows the im prove ment of cli mate con di tions proved also by pres ence of Typha latifolia pol len.
Betula LPAZ (16.23–16.38m). The dom i nance of Betula (to 55.6%) over Pinus (33.2–41.3%), shows the de vel op ment of birch and birch-pine for ests.
The zones Betula and Pinus–Betula, as well as prob a bly the youn ger part of Pinus–NAP zone, we can cor re late with the old - est re gional pol len zone of Eemian – E1 (Mamakowa, 1988, 1989).
Pinus–Betula–Ulmus LPAZ (15.73–16.23 m). A high amount of Pinus (57.5–70.1%) ac com pa nied with a lower amount, in com par i son to the pre vi ous zone, of Betula (11.9–29.5%). Small amounts of pol len grains of Ulmus (max. 4.3%) and Quercus (max. 6.5%) are also pres ent. The pres ence of new spe cies proves the im prove ment of cli mate and edaphic con di tions al - low ing the de vel op ment of mixed for est with Ulmus and
Quercus. The gen eral palynological pic ture of this zone al lows for its cor re la tion with the zone E2 in strati graphic di vi sion of the Eemian (Mamakowa, 1988, 1989).
Quercus LPAZ (15.03–15.73 m). Quercus (15.2–30.9%) is dom i nant and ac com pa nied by Pinus (42.0–62.7%), Betula (4.7–14.9%) and Ulmus (1.9–3.1%), as well as the con tin u ous per cent age curve (up to 2.2%) of Corylus in the mid dle part. The pol len of Hedera proves the ex is tence of a warm and hu mid cli - mate (Iversen, 1958). The pol len spec tra of this zone al low for its cor re la tion it with the E3 zone in the Eemian veg e ta tion suc ces - sion (Mamakowa, 1988, 1989).
Corylus LPAZ (14.90–15.03 m). The char ac ter is tic fea ture is the sig nif i cant amount of Corylus pol len grains (up to 10.5%). Al - though this zone was dis tin guished on the ba sis of pol len spec - trum of only one sam ple, we can as so ci ate it, with high prob a bil - ity, with the be gin ning of E4 zone in the Eemian suc ces sion (Mamakowa, 1988, 1989).
Sum ming up, the ob tained palynological re sults are sim i lar to pre vi ously de scribed Eemian se ries known from other sites of cen tral Po land (Noryœkiewicz, 1978; Stankowski and Tobolski, 1981; Jastrzêbska-Mame³ka, 1985; Tobolski, 1986, 1991a, b;
Klatkowa and Balwierz, 1990; Klatkowa and Win ter, 1990;
Kotarbiñski and Krupiñski, 1995; Malkiewicz, 2002), which al - lows for a strong in di ca tion of the age of de po si tion of in ves ti - gated sed i ments.
CLADOCERA ANALYSIS
In the Bór pro file, 23 Cladocera spe cies were rec og nized (Fig. 4), be long ing to four fam i lies. The most nu mer ous were the lit to ral spe cies of the Chydoridae fam ily. The num ber of pe lagic forms (from the Bosminidae, Daphnidae and Sididae fam i lies) in places ex ceeds 30% of all Cladocera in di vid u als.
On the ba sis of the Cladocera com mu ni ties and the changes in fre quency of the var i ous spe cies, five zones of Cladocera de - vel op ment were dis tin guished and con nected with the Eeemian Inter gla cial pe riod.
Fig. 3. Per cent age pol len di a gram
Zone Bór I (16.48–16.63 m). At the be gin ning a low di ver sity of Cladocera is noted, com pris ing only two ini tial spe cies: Alona affinis and Eurycercus lamellatus. Later the di ver sity of Cladocera spe cies in creases to 8. The most nu mer ous are Chydorus sphaericus, Alona affinis, Alonella nana and Acroperus harpae which tol er ate cold wa ter in the lake.
Zone Bór II (16.23–16.48 m). The plank tonic form is noted up to 30% fre quency of all Cladocera. The di ver sity of Cladocera spe cies in creases at the be gin ning to 9 spe cies but later de - creases to 5 spe cies.
Zone Bór III (15.73–16.23 m). The di ver sity of Cladocera spe cies in creases to 12 spe cies. These in clude spe cies in di cat - ing warmer wa ter: Camptocercus rectirostris, Pleuroxus trigo - nel lus, P. trun catus and P. uncinatus, as well as macro phyte-as - so ci ated spe cies are pres ent. Plank tonic forms oc cur in mid dle part of this zone.
Zone Bór IV (15.53–15.73 m). The most nu mer ous spe cies are Chydorus sphaericus and Alona affinis. The di ver sity of Cladocera spe cies de creases to 8 spe cies at the end of the zone. Daph nia pulex and Graptoleberis testudinaria ap pear for the first time.
Zone Bór V (14.90–15.53 m). This zone is char ac ter ized by the max i mum of zoo plank ton de vel op ment. Four teen spe cies of Cladocera have been found, and two subzones have been dis - tin guished. In subzone Bór Va (15.03–15.53 m) the di ver sity of Cladocera spe cies sys tem at i cally in creases. Plank tonic forms fre quent reach 15% of all Cladocera. Among plank tonic forms Bosmina longirostris dom i nates dur ing pe ri ods of in creased sup - ply of nu tri ents. Among lit to ral forms Chydorus sphaericus and Alona rectangula dom i nate and Leydigia acanthocercoides and Disparalona rostrata ap pear for the first time. Spe cies in di cat ing warmer wa ter e.g., Camptocercus rectirostris, Graptoleberis testudinaria and Pleuroxus spp., are also pres ent ac com pa nied by Acroperus harpae, Eurycercus lamellatus and Alona affinis, which are of ten as so ci ated with a high den sity of wa ter plants.
Subzone Bór Vb (14.90–15.03 m) is char ac ter ized by the high - est fre quency and di ver sity of Cladocera re mains and spe cies.
Chydorus sphaericus and Alona rectangula dom i nate in this zone. The plank tonic forms dis ap pear and the pres ence of Graptoleberis testudinaria, Camptocercus rectirostris and Pleuroxus spp. sug gests that the warm cli ma tic con di tions con - tin ued.
692 Joanna Petera-Zganiacz, Ryszard K. Borówka, Jacek Forysiak, Gra¿yna Miotk-Szpiganowicz and Dominik Paw³owski
Fig. 4. Ab so lute num ber of Cladocera in di vid u als, ra tio of plank tonic (P) to lit to ral (L) forms and pro posed Cladocera zones (CAZ) in the sed i ments of Bór palaeolake
* – scale on di a gram shows spec i mens in 1 cm3 of fresh sed i ments
GRAN-SIZE ANALYSIS OF GYTTJA
The grain-size dis tri bu tion var ied only slightly along the stud - ied pro file. Ex clud ing the low est sam ple, the sed i ment con sists of silts dom i nated by the coarse silt frac tion (0.031–0.016 mm) which makes up, on the av er age, about 30% of the sam ple weight. The very coarse silt (0.063–0.031 mm) and mod er ately coarse silt (0.016–0.008 mm) ac count for 20 and 22%, re spec - tively (Fig. 5). The to tal con tent of silt-clay frac tion (<0.063 mm) is 85% on av er age.
The grain-size vari abil ity in the pro file was rel a tively low. It was no ticed (on depth 15.5–16.5 m) that there is a ten dency to - wards a grad ual in crease of the mean grain-size (Fig. 5). The ten dency is pri mar ily re lated to a re duc tion of mod er ate- and fine-grained silt frac tions (0.016–0.008 and 0.008–0.004 mm, re spec tively; Fig. 5). The stan dard de vi a tion (d1), a mea sure of sed i ment sort ing, var ied from 1.1 to 1.7 phi, in di cat ing poor sort - ing. Grain-size dis tri bu tion skew ness var ied slightly only, from –0.1 to +0.1, a range typ i cal of sym met ri cal dis tri bu tions (Racinowski et al., 2001).
GEOCHEMISTRY
In the or ganic de pos its con tent of the CaCO3 is much higher than in min eral de pos its and is 25.9% on av er age (Fig. 6). The high est value was ob tained in the base part – in the cal car e ous de tri tal gyttja – al most 50%. De ter mi na tion of the re ac tion al lows for the clas si fi ca tion biogenic de pos its as neu tral and slightly al - ka line (Okruszko, 1976). The low est val ues were es ti mated in the base part while in the mid dle and top part of the or ganic de - pos its, re ac tion ranges from 7.2 to 7.5. The con duc tiv ity of de - pos its is char ac ter ized by con sid er able vari abil ity. The value of that pa ram e ter ex ceeds 1200 mS in the base, de creases in the mid dle part of the pro file to 540 mS and at the top again in - creases to 1280 mS.
Con tents of so dium, po tas sium, mag ne sium and lead in the chem i cal com po si tion of ana lysed sed i ment is, on av er age, much lower than those re corded in silty for ma tions or sand - stones (Ta ble 1). Con tents of cop per and zinc is within the range typ i cal to sand stones, whereas the con tent of cal cium, iron, and man ga nese is dis tinctly higher, com pared to con tents known from silty de pos its.
Fig. 5. Grain-size com po si tion and Folk and Ward co ef fi cients of the min eral mat ter in gyttja Ex pla na tions as in Fig ure 2
Fig. 6. Physicochemical prop er ties of or ganic de pos its from the Bór site Ex pla na tions as in Fig ure 2
The ana lysed sed i ments show a sta tis ti cally sig nif i cant (at the level of 0.1%) pos i tive cor re la tion be tween the con cen tra tion of or ganic mat ter and the con tents of man ga nese, zinc, and cop - per as well as weak cor re la tion in case of mag ne sium, so dium, and po tas sium (Ta ble 2). More over, sig nif i cant con nec tions are ob served in con tents of Zn and Mg, Cu and Mn, and some lithophilous met als: Na and K, Na and Mg, and K and Mg (Ta - ble 2). Cal cium and iron do not show stron ger cor re la tions with other as sayed el e ments. The per cent age con tent of silt-clay frac tion (<0.063 mm), cor re lates the stron gest with con tent of so dium and iron (Ta ble 2), al though the sig nif i cance of those cor re la tions is at the level of 1%.
Anal y sis of geo chem i cal di a grams (Figs. 7 and 8) al low for the iden ti fi ca tion of three geo chem i cal in ter vals, which are mark - edly dif fer ent in their chem i cal com po si tion.
In ter val Bór I (16.43–16.63 m) shows the high est con tent of min eral ma te rial (>92%), and cal cium (150.5 mg/g) but the low - est val ues of the re main ing el e ments, par tic u larly po tas sium, man ga nese and zinc (Ta ble 1). The high est Fe/Mn ra tio (80–180) as well as some what el e vated Cu/Zn and Ca/Mg are ob served (Fig. 8).
In ter val Bór II (15.5–16.43m) con tain on av er age 22.9% or - ganic mat ter (up to about 30%). This level is char ac ter ized by
rel a tively the high est con cen tra tions of all met als ex cept iron, while the high con tents of Ca and Zn in the base of in ter val dis - tinctly de creases to the top. In the case of the other el e ments there are only some slight vari a tion of the con tents, which are as so ci ated only to a small ex tent with sub tle changes in li thol - ogy, what is vis i ble, inter alia, in cor re la tions of or ganic mat ter con tent and per cent age of clay-silty frac tion with each metal.
Through out the in ter val the Fe/Mn and Cu/Zn ra tios are uni - form and low. On the other hand, the Fe/Ca ra tio was clearly higher than in the In ter val Bór I, in di cat ing an in creas ing trophic sta tus of the ba sin. Minor vari a tions of Ca/Mg ra tio are ob served, what prob a bly re flect sub tle changes in the sup ply of min eral de - pos its.
In ter val Bór III (14.90–15.50 m) was iden ti fied on the base of chang ing in the trend of the cal cium and zinc con tents in the pro - file (Fig. 7). Con tents of in di vid ual met als, ex cept iron, are lower than those in In ter val Bór II. In ad di tion, the in ter val shows ini - tially a grow ing and then a de creas ing trend in the con tent of al - most all el e ments, which re flects changes in grain-size of the min eral frac tion (Fig. 5) which at tain, on av er age, ca. 85%. In the top part of the in ter val the Fe/Mn ra tio in creases.
694 Joanna Petera-Zganiacz, Ryszard K. Borówka, Jacek Forysiak, Gra¿yna Miotk-Szpiganowicz and Dominik Paw³owski
Geo chem i cal in ter val
MO
[%] Na
[mg/g] K
[mg/g] Ca
[mg/g] Mg
[mg/g]
Fe
[mg/g] Mn
[mg/g]
Cu [mg/g]
Zn [mg/g]
Pb [mg/g
Bór; av er age 17.1 0.16 1.37 108.9 3.20 48.92 1.34 7.48 35.53 1.20
Silty de pos its* – 7–15 22 22 15 33–47 0.4–0.8 40–60 80–120 20–40
Sand stones * – 10–15 12 27 7–10 9–30 0.1–0.5 5–30 15–30 5–10
Bór III 15.7 0.15 1.35 95.1 3.15 52.24 1.36 6.92 32.88 0.62
Bór II 22.9 0.17 1.60 96.4 3.53 47.78 1.75 8.68 45.82 1.93
Bór I 7.1 0.13 0.91 150.5 2.58 47.21 0.47 5.76 18.14 0.46
* – con tents most fre quently found in silty de pos its and sandstones (ac cord ing to Kabata-Pendias and Pendias, 1993)
T a b l e 1 Av er age con cen tra tion of min eral ma te rial (MO) and av er age con tents of el e ments ana lysed in the pro files
and geo chem i cal in ter vals (cf. Fig. 5)
R 0.063 MO Na K Ca Mg Fe Mn Cu Zn Pb
0.063 1
MO 0.51 1
Na 0.67 0.62 1
K 0.52 0.60 0.88 1
Ca 0.43 –0.14 0.02 –0.15 1
Mg 0.57 0.64 0.84 0.88
0.12 1
Fe 0.63 0.24 0.53 0.42 0.46 0.53 1
Mn 0.46 0.93 0.52 0.49 –0.11 0.52 0.23 1
Cu 0.42 0.81 0.56 0.60 –0.27 0.52 0.12 0.66 1
Zn 0.54 0.88 0.70 0.72 –0.03 0.79 0.24 0.78 0.73 1
Pb 0.39 0.48 0.74 0.82 –0.08 0.76 0.15 0.28 0.51 0.74 1
T a b l e 2 Bór pro file: co ef fi cients of cor re la tion be tween metal con tents and per cent con tri bu tion of silt-clay frac tion (<0.063 mm)
and or ganic mat ter con cen tra tion (bold char ac ters de note highly sig nif i cant cor re la tions, as shown by Stu dent’s t test)
Fig. 7. Geo chem i cal di a gram
Fig. 8. Ver ti cal dif fer en ti a tion of se lected geo chem i cal pa ram e ters
PHASES OF THE BÓR PALAEOLAKE DEVELOPMENT
The ob tained re sults al low to dis tin guish four phases of the lake de vel op ment in the Bór site (Fig. 9):
Phase 1 (16.53–16.63 m)
The low est part of the in ves ti gated sed i ments was de pos ited in the fi nal part of the Wartanian, in a cold cli mate when tun dra as so ci a tions were pres ent and in ten sive cal cium car bon ate sup - ply to the sed i men tary ba sin took place. That pe riod was also char ac ter ized by a high, al though grad u ally de creas ing, in ten sity of me chan i cal de nu da tion pro cesses in di cated by more than 90% con tri bu tion of the min eral frac tion, at first sandy and then silt-clay (Fig. 5) and the high Fe/Mn ra tio with the si mul ta neous high Fe con tents (Mackereth, 1966). It may be con cluded that sed i men ta tion at Phase 1 pro ceeded dur ing a cool cli mate when the plant cover was sparse, which is in agree ment with the pol len anal y sis re sults. The con di tions were most prob a bly anal o gous to those prev a lent in the Late Gla cial in the Eu ro pean Low land, when in tense me chan i cal de nu da tion was ac com pa nied by car - bon ate de po si tion in sed i men tary bas ins, par tic u larly as a re sult of hydrocarbonate iron sup ply with ground wa ter (Nowaczyk and Tobolski, 1980; Kowalkowski, 1988; Borówka, 1992; Borówka and Tomkowiak, 2010; Forysiak et al., 2010). At the be gin ning Cladocera spe cies tol er at ing cool, oligotrophic wa ter ex isted in the lake. The slightly higher amount of Cladocera and pres ence of plank tonic forms might be a con se quence of fa vor able con di - tions like an in crease in the amount of wa ter in the res er voir and/or better ther mal con di tions. The sed i ments of the up per
part of this phase, prob a bly de vel oped in the very be gin ning of Eemian Inter gla cial.
Phase 2 (15.68–16.53 m)
The char ac ter is tic fea ture of the Phase 2 is the high est con - tent of the or ganic ma te rial (>20%) and sig nif i cant amount of CaCO3 (15–30%). This phase in clude three LPAZ: Pinus– Be - tula, Betula, and Pinus–Betula–Ulmus, which are cor re lated with the old est re gional pol len zones of Eemian – E1 and E2. The be - gin ning of the Eemian Inter gla cial was ex pressed by a greater di ver sity of Cladocera (Fig. 4) and the ini tially high fre quency of plank tonic forms (Cladocera zone Bór II). It is pos si ble that this sit u a tion was re spond to in crease of wa ter ta ble. The di ver sity of Cladocera spe cies in creased at the be gin ning but later de - creased to rise again (Cladocera zone Bór III). Spe cies in di cat - ing warmer wa ter, Camptocercus rectirostris, Pleuroxus trigonellus, P. truncatus and P. uncinatus are pres ent. Also spe - cies as so ci ated with a high den sity of wa ter plants, oc cur there.
Lack of plank tonic forms which is ob served in mid dle part of this zone, prob a bly in di cates a short-term shallowing, but can also be a re sponse to geo chem i cal changes in wa ter (Fig. 7) or re - flect sub tle changes in the sup ply of min eral de pos its (Fig. 5).
Higher or ganic mat ter con cen tra tion, ac com pa nied by a si - mul ta neous in crease of the Fe/Ca ra tio, which in di cate a rais ing of the trophic level, most likely as so ci ated with warm ing of the cli - mate. In the base part of the Phase 2 (lower part of the geo - chem i cal In ter val Bór II), the high est Zn and Pb con tents are ob - served, likely as a re sult of bioaccumulation of those el e ments.
The in crease in Zn con tent could have been as so ci ated with the ap pear ance of the light-re quir ing birch char ac ter ized as hav ing a strong abil ity to bioconcentrate zinc (For tes cue, 1980; Reimann et al., 2007). The rel a tively low Fe/Mn ra tios ev i denced per sis - tence of ox i da tive con di tions in the wa ter body (Mackereth, 1966; Borówka, 2007).
Phase 3 (15.50–15.68 m)
In the Phase 3 the per cent age of the min eral ma te rial in - creases and val ues of the Mz co ef fi cient de creases, what in di - cates that the ba sin be came a re cip i ent of a fairly high amount of min eral ma te rial, in clud ing fine sands. It may thus be con tended that the wa ter body was ei ther a flow-through. The Phase 3 is con nected with the be gin ning of the Quercus LPAZ with char ac - ter is tic rapid in crease amount of Quercus pol len and in creased per cent age of the NAP, in clud ing plants of wet com mu ni ties.
The di ver sity of Cladocera spe cies de creases at the end of phase, the most nu mer ous were Chydorus sphaericus and Alona affinis. Daph nia pulex and Graptoleberis testudinaria ap - pears for the first time. The oc cur rence of Daph nia pulex, which is a spe cies typ i cal of the open-wa ter zone, sug gests a slight raise of the wa ter level in the res er voir, per haps due to the in flow of flood wa ters into the ba sin.
The veg e ta tion cover was dense in this part of the Eemian Inter gla cial, which ex cludes the in ten si fi ca tion of the de nu da tion or ae olian pro cesses. The in creas ing of hu mid ity and wa ter level in the lake can by ac counted for flood ac tiv ity.
The grad ual re duc tion of cal cium car bon ate con tent (Fig. 8) can in di cate a de creas ing rate of leach ing of that com pound from the for mer drain age area, which could have been as so ci - ated with: ex haus tion of CaCO3 re sources in the drain age area, more com pact veg e ta tion cover which can in hibit leach ing CaCO3 from soil by bind ing the com pound via bio chem i cal pro - cesses, or a change in the pre cip i ta tion-evapotranspiration re la - 696 Joanna Petera-Zganiacz, Ryszard K. Borówka, Jacek Forysiak, Gra¿yna Miotk-Szpiganowicz and Dominik Paw³owski
Fig. 9. Phases of the Bór palaeolake de vel op ment
tion ships in fa vour of evapotranspiration, which is as so ci ated with re duced in fil tra tion of pre cip i ta tion and in con se quence leach ing of car bon ates, char ac ter ized by high sol u bil ity in wa ter.
An in take of wa ter dur ing floods can be take into con sid er ation as well.
Phase 4 (14.90–15.50 m)
The Phase 4 is cor re lated with the up per part of the level Quercus LPAZ (E 3) and Corylus LPAZ (E 4) which de ter mine the cli ma tic Eemian Inter gla cial op ti mum (Mamakowa, 1988, 1989). The in crease of the sum of the herbs and plants char ac - ter is tic for wet com mu ni ties prob a bly re flect lo cal con di tions in the river val ley bot tom, whereas in case of high ground wa ter level a larger role could have been played by open, tree less com mu ni ties.
In the Phase 4 the num ber of Cladocera spe cies rap idly in - creased (Cladocera zone Bór Va). The pres ence of
“thermophilic spe cies” shows the con tin ued warm cli ma tic con di - tions. An in crease in the num ber of phytophilous cladocerans in - di cates the rich macrovegetation in the lake. Pres ence of spe - cies which have big ger re quire ments, sug gests a higher trophic level of the lake. Oc cur rence of plank tonic spe cies, which liv ing in open-wa ter zone sug gests suf fi cient of wa ter level, but finally a re duc tion of plank tonic forms took place (Cladocera zone Bór Vb).
The high trophic level is in di cated by re sults of anal y sis of changes in the Fe/Ca ra tio in In ter val Bór III (Fig. 8). At the same time, the sup ply of min eral mat ter, in clud ing CaCO3, in creased.
There is also a ten dency to wards an in crease in the Fe/Mn ra tio ac com pa ny ing the high iron con tent (Figs. 7 and 8), which also ev i dences the dom i na tion of allochthonous min eral mat ter sup - ply (Mackereth, 1966; Boyle, 2001). It may be thus in ferred that the study site lo cated in a river val ley, was ex pe ri enc ing an in - creased fre quency of floods. The ba sin it self ac cu mu lated not only the flood-borne sed i ment, but also de pos ited plant re mains (mainly leaves), which would ex plain the per sis tence of rather high CaCO3 con cen tra tions.
DISCUSSION AND PALAEOGEOGRAPHICAL CONCLUSIONS
The Bór palaeolake was a small and shal low res er voir lo - cated in the dis tal part of the for mer val ley, rather far from the ac - tive river chan nel and close to the val ley edge, where the Me so - zoic sub stra tum lays rel a tively high. The lake ap peared as a re - sult of aban don ment of one of the chan nels or subchannels of the braided river which de vel oped in the Warta River val ley dur - ing the Wartanian ter mi na tion. The be gin ning of the lake in fill ing took place dur ing that time and lasted, at least to the Eemian Inter gla cial op ti mum. The top part of the or ganic de pos its were – most prob a bly – eroded due to in ten sive flu vial pro cesses in Weichselian.
The palynological re cord starts from the end of the Wartanian. Dur ing that pe riod the cladoceran suc ces sion com - prises a very rich fre quency which might be mir rored by a fa vour - able con di tions for zoo plank ton. The sed i ments of the Bór palaeolake were ac cu mu lated in a hu mid en vi ron ment, most prob a bly on the shore, which is sup ported by the pres ence of pol len grains orig i nat ing from: rushes (Sparganium, Typha - latifolia), wa ter plants (Nuphar, Potamogeton, Myriophyllum) and large amounts of fern spores (Filicales) in the sed i ments.
The Cladocera spe cies in di cate the oligotrophic sta tus of the
lake ini tially and then an in crease of the trophic sta tus in Eemian op ti mum. At the be gin ning of the Eemian op ti mum the wa ter level in creased, which is in di cated by the in creas ing amount of pol len grains of the wa ter plants and plank tonic Cladocera forms. Next, the res er voir be came shal lower, but prob a bly the ground wa ter level was high, what ef fected in places on de vel op - ment of the tree less, wet com mu ni ties. Gen er ally, con di tions in Bór res er voir are sim i lar to other Pol ish Eemian palaeolakes (e.g,. Tobolski, 1991a; Malkiewicz, 2002; Miros³aw-Grabowska et al., 2009; Paw³owski, 2011).
The im pos si bil ity of a re con struc tion of the for mer to pog ra - phy made an es ti ma tion of the in ten sity of de nu da tion pro cesses dif fi cult. The ob tained re sults point to a lake mostly fed by cal - cium car bon ate-rich ground wa ter, which is un der stand able in the case of nearby Me so zoic sub stra tum. How ever, the sed i - ments also con tain a high pro por tion of car bon ate-free min eral frac tion, there fore it has to be as sumed that it was sup plied to the ba sin via sur face trans port. It is most prob a ble that the ac cu - mu la tion pro ceeded in a small lake de vel oped from an aban - doned chan nel lo cated close to a val ley mar gin, pe ri od i cally fed by sur face wa ters and at the same time ex pe ri enc ing con di tions ame na ble to ground wa ter trans port. Physicochemical prop er ties of de pos its from Bór palaeolake are com pa ra ble to re sults ob - tained for con tem po rary peatland in the Bartochów site, lo cated in the Warta River val ley at the base of the Warta Hills, pos si bly, in an anal o gous sit u a tion.
The ap plied meth ods like pol len, Cladocera, geo chem is try, and lithological anal y ses, as well as palaeogeomorphological anal y ses al lowed for the re con struc tion of an im age of the func - tion ing of the res er voir dur ing time from Wartanian ter mi na tion to Eemian Inter gla cial op ti mum. A key point of the stud ies was to es tab lish the spa tial re la tion be tween the Me so zoic sub stra tum and the palaeolake lo ca tion. The in flu ence of the Me so zoic sub - stra tum man i fested in the geo chem i cal prop er ties of the de pos - its and re sults led to the con clu sion about the meth ods of feed - ing the lake. The re sults of in ves ti ga tions in the Bór site shows how im por tant are de tailed multi-proxy anal y ses of the or ganic de pos its in or der to es tab lish an as wide as pos si ble geo log i cal con text which con fer the pos si bil ity of re con struct the var i ous el - e ments of the palaeoenvironment. It is worth in ves ti gat ing the river val leys, be cause such an in ves ti ga tion can pro vide valu - able and var i ous in for ma tion.
It is worth pay ing at ten tion to the es ti mated level of the val ley beds of the sec tions of Warta and Vistula rivers within the War - saw–Berlin ice-mar ginal streamway in Eemian Inter gla cial. On the west side there are two sites with Eemian Inter gla cial biogenic sed i ments: Krzy¿ówki (lo cated about 2 km to the north-west from Ko³o, on the right bank of the Warcica River – right trib u tary of the Warta River) and Bór (lo cated in the Warta River val ley about 3 km south from the con tem po rary mouth of the Ner River) which is pre sented here. The base of the biogenic de pos its at al ti tudes of 80.8 m a.s.l. in the Bór and about 71 m a.s.l. in the Krzy¿ówki con firm a sim i lar ity to the pres ent course of the Warta River. On the east side the Vistula River bed in the Bzura River mouth area is lo cated at about 54 m a.s.l. (Marks and Pochocka, 1999) and the bed of Eemian al lu via in £êczyca vi cin ity lay at al ti tudes about 75 m a.s.l. (Jewtuchowicz, 1967).
The im pli ca tions of these facts are con nected with the di rec tion of the flow of the rivers drained the £ódŸ Pla teau in the sec tions within War saw–Berlin ice-mar ginal streamway – to the east or to the west as Jewtuchowicz (1967) claimed. Tak ing into ac count the al ti tude of the Lower Bzura Val ley in the Eemian Inter gla cial, the val leys of the rivers, which flowed through the edge zone of the £ódŸ Pla teau should be in cised deeper. As sum ing that the Lower Ner Val ley bed has dropped grad u ally sim i larly to those in the pres ent day, the base level of ero sion of the val leys men -
tioned above, should have lie on al ti tude 80–90 m a.s.l. and rais - ing to the east. It cor re sponds well with the po si tion of Eemian Inter gla cial and Early Weichselian biogenic sed i ments, de pos - ited in the val ley beds or wide bas ins in Piaski Stare (Jewtuchowicz, 1970), Walewice (Dylik, 1967), in Moszczenica Val ley near Gieczno (Kamiñski, 1993) and in Bobrówka Val ley (Klajnert and Piechocki, 1972). These facts point to dif fer ent from the pres ent, di rec tion of out flow of the river within the War - saw–Berlin ice-mar ginal streamway in the Eemian Inter gla cial.
The re con structed im age of the Warta River val ley dur ing the Eemian Inter gla cial, com pared with its con tem po rary im age shows, how big is the trans for ma tion of flu vial re lief in the past 130,000 years. Top o graphic dif fer ences in the val ley be tween the edge and the bot tom of the val ley de clined, in some parts, more than two fold (e.g., in Dobrów). The Warta River val ley was a tran si tional val ley, run ning through the Eemian lakeland (Klatkowa, 1990). The source area was cer tainly be yond the reach of the Mid dle Pol ish Glaciations, to the Ko³o vi cin ity run - ning in a sim i lar way as it does cur rently. Its down stream course
is not en tirely ex plained, how ever, there are sug ges tions that the river flowed di rectly north, to the Bal tic Ba sin (Mojski, 2005).
It is also worth pay ing at ten tion to the lack of an up per part of the inter gla cial pro file (from the up per part of the Eemian Inter - gla cial op ti mum) at the Bór site and in Peene Val ley (Meng et al., 2009), and a hi a tus in the top of the Eemian op ti mum in Krzy¿ówki site (Noryœkiewicz, 1999). One may won der if there is a gen eral ten dency of some cli mate change af ter op ti mum, re - sult ing in ero sion, low er ing of the ground wa ter level and the end of the de po si tion of or ganic sed i ments. How ever, cur rent state of re search lead to in ter pre ta tion of ab sence of the up per parts of pro files, as an ef fect of Weichselian ero sion.
Ac knowl edge ments. The study was sup ported by a grant from the Pol ish Min is try of Sci ence and Higher Ed u ca tion, No N 306 2840 33 “Or i gin, age and depositional con di tions of KoŸmin gla cial lake sed i ments (Ko³o Ba sin, Cen tral Po land)”. The au - thors are grate ful to the re view ers: H. Win ter and J. Satkñnas and ed i tors: T. Peryt and W. Granoszewski for re vi sion and valu - able com ments.
REFERENCES
Ber A., Lindner L., Marks L. (2007) Propozycja podzia³u stratygraficznego czwartorzêdu Polski. Przegl¹d Geologiczny, 55: 115–118.
Berglund B.E. (1979) Pol len anal y sis. In: Palaeohydrological changes in the tem per ate zone in the last 15000 years (ed. B.E.
Berglund). Subproject B, 2: 133–167.
Borówka R.K. (1992) The pat tern and mag ni tude of de nu da tion in intraplateau sed i men tary bas ins dur ing the Vistulian and Ho lo - cene (in Pol ish with Eng lish sum mary). Adam Mickiewicz Uni ver - sity Press, Seria Geografia, 54: 1–177.
Borówka R.K. (2007) Geochemiczne badania osadów jeziornych strefy umiarkowanej. Studia Limnologica et Telmatologica, 1:
33–42.
Borówka R.K., Tomkowiak J. (2010) Sk³ad chemiczny osadów z profilu torfowiska ¯abieniec. In: Torfowisko ¯abieniec: warunki naturalne, rozwój i zapis zmian paleoekologicznych w jego osadach (ed. J. Twardy, S. ¯urek and J. Forysiak): 163–172.
Bogucki Wydawnictwo Naukowe, Poznañ, .
Boyle J.F. (2001) In or ganic geo chem i cal meth ods in palaeolimnology. In: Track ing En vi ron men tal Change Us ing Lake Sed i ments, 2. Phys i cal and geo chem i cal meth ods (ed. W.M.
Last, J.P. Smol): 83–140. Kluwer Ac a demic Pub lish ers, Dordrecht.
Bruj M., Ro man M. (2007) The Eemian lakeland ex tent in Po land ver sus strati graphi cal po si tion of the Middle Pol ish Glaciations (in Pol ish with Eng lish sum mary). Biuletyn Pañstwowego Instytutu Geologicznego, 425: 27–34.
Czarnik J. (1972) Paleogeography of the en vi rons of Turek in the Up - per Ter tiary and Pleis to cene (in Pol ish with Eng lish sum mary).
Studia Geologica Polonica, 40.
Czubla P. (2001) Fennoscandian er rat ics in Qua ter nary De pos its of Mid dle Po land and their value for strati graphic pur poses (in Pol - ish with Eng lish sum mary). Acta Geographica Lodziensia, 80.
Czubla P., Forysiak J., Petera-Zganiacz J. (2010) Lith o logic and petrographic fea tures of tills in the KoŸmin re gion and their value for strati graphi cal in ter pre ta tion of the de pos its of the KoŸmin gla cial lake, cen tral Po land. Geologija, 52 (1–4): 1–8.
Dylik J. (1967) Site VIII/28 Walewice. Guide of Ex cur sion of the Sym - po sium of the Com mis sion on the Evo lu tion of Slopes and of the Com mis sion on Periglacial Geo mor phol ogy of the In ter na tional Geo graph ical Un ion, Po land: 84–93.
Faegri K., Iversen J. (1978) Podrêcznik analizy py³kowej.
Wydawnictwo Geologiczne.
For tes cue J.A.C. (1980) En vi ron men tal geo chem is try. A ho lis tic ap - proach. New York, Springer-Verlag.
Forysiak J. (2005) The de vel op ment of the Warta River val ley be - tween Burzenin and Dobrów in the Late Qua ter nary pe riod (in Pol ish with Eng lish sum mary). Acta Geographica Lodziensia, 90.
Forysiak J., Borówka R.K., Paw³owski D., P³óciennik M., Twardy J., ¯elazna-Wieczorek J., Koss M., ¯urek S. (2010) Rozwój zbiornika ¯abieniec w póŸnym glacjale i jego znaczenie dla paleoekologii i paleogeografii. In: Torfowisko ¯abieniec. Warunki naturalne, rozwój i zapis zmian paleoekologicznych w jego osadach (ed. J. Twardy, S. ¯urek, J. Forysiak): 191–202. Bogucki Wydawnictwo Naukowe, Poznañ.
Frey D.G. (1962) Cladocera from the Eemian Inter gla cial of Den - mark. Jour nal of Pa le on tol ogy, 36: 1133–1154.
Frey D.G. (1986) Cladocera anal y sis. In: Hand book of Ho lo cene Paleoecology and Paleohydrology (ed. B.E. Berglund): 667–692.
John Willey and Sons.
Iversen J. (1958) The bear ing of gla cial and inter gla cial ep ochs on the for ma tion and ex tinc tion of plant taxa. Uppsala Universiteit Arssk, 6: 210–215.
Janczyk-Kopikowa Z. (1987) Re marks on palynostratigraphy of the Qua ter nary (in Pol ish with Eng lish sum mary). Kwartalnik Geologiczny, 31 (1): 155–163.
Jastrzêbska-Mame³ka M. (1985) The Eemian Inter gla cial and Early Vistulian at Zgierz-Rudunki in the £ódŸ Pla teau (in Pol ish with Eng lish sum mary). Acta Geographica Lodziensia, 53.
Jewtuchowicz S. (1967) Or i gin of the War saw-Berlin Pradolina be - tween rivers Ner and Moszczenica (in Pol ish with Eng lish sum - mary). Prace Geograficzne Instytutu Geografii PAN, 62.
Jewtuchowicz S. (1970) Evo lu tion of land-forms in the re gion of
£êczyca since the Mid dle-Pol ish Gla ci ation (in Pol ish with Eng - lish sum mary). Prace Geograficzne Instytutu Geografii PAN, 85.
Kabata-Pendias A., Pendias H. (1993) Biogeochemia pierwiastków œladowych. Wydawnictwo Naukowe PWN, Warszawa.
Kamiñski J. (1993) Late Vistulian and Ho lo cene trans for ma tion of the Moszczenica River val ley as a re sult of changes of the nat u - ral en vi ron ment and man ac tiv ity (in Pol ish with Eng lish sum - mary). Acta Geographica Lodziensia, 64.
698 Joanna Petera-Zganiacz, Ryszard K. Borówka, Jacek Forysiak, Gra¿yna Miotk-Szpiganowicz and Dominik Paw³owski
Klajnert Z., Piechocki A. (1972) The Up per-Pleis to cene de pos its with mol lus can fauna in the Bobrówka Val ley near £owicz (in Pol - ish with Eng lish sum mary). Folia Quaternaria, 40: 1–36.
Klatkowa H. (1990) The oc cur rence of the Eemian or ganic de pos its and re marks on the paleomorphology of Cen tral Po land at the Wartanian de cline and dur ing the Eemian pe riod (in Pol ish with Eng lish sum mary). Acta Geographica Lodziensia, 61: 7–17.
Klatkowa H. (1991) The re sults of grain abra sion anal y sis of the se - lected Qua ter nary sed i ments of Cen tral Po land (in Pol ish with Eng lish sum mary). In: Geneza, litologia i stratygrafia utworów czwartorzêdowych (ed. A. Kostrzewski). Wydawnictwo Naukowe Uniwersytetu im. Adama Mickiewicza w Poznaniu, Seria Geografia, 50: 277–287.
Klatkowa H. (1993) Some fea tures of the Warta glacigenic de pos its in Mid dle Po land (in Pol ish with Eng lish sum mary). Acta Geographica Lodziensia, 65: 99–140.
Klatkowa H., Balwierz Z. (1990) A closed de pres sion with the Eemian flora at Modlna near £ódŸ (in Pol ish with Eng lish sum - mary). Acta Geographica Lodziensia, 61: 39–49.
Klatkowa H., Win ter H. (1990) The Eemian Integlacial at Ostrów near Grabica (in Pol ish with Eng lish sum mary). Acta Geographica Lodziensia, 61: 59–68.
K³ysz P. (1981) Morphogenesis of a se quence of mar ginal forms in the sur round ings of Konin, Ko³o and Turek (in Pol ish with Eng lish sum mary). Wydawnictwo Naukowe Uniwersytetu im. Adama Mickiewicza w Poznaniu, Seria Geografia.
Kotarbiñski J., Krupiñski K.M. (1995) Eemian Inter gla cial de pos its in Studzieniec and Babiec Piaseczny near Sierpc (cen tral Po - land) (in Pol ish with Eng lish sum mary). Przegl¹d Geologiczny, 43: 565–571.
Kowalkowski A. (1988) Wiek i geneza gleb. In: Przemiany œrodowiska geograficznego Polski (ed. L. Starkel): 45–85.
Zak³ad Narodowy im. Ossoliñskich, Wroc³aw.
Kozarski S. (1981) Stra tig ra phy and chro nol ogy of the Vistulian in Great Po land Low land (in Pol ish with Eng lish sum mary). PAN, Oddzia³ w Poznaniu, Geografia, 6.
Lindner L., Marks L. (2012) Climatostratigraphic sub di vi sion of the Pleis to cene Mid dle Pol ish Com plex in Po land (in Pol ish with Eng lish sum mary). Przegl¹d Geologiczny, 60: 36–45.
Mackereth F.J.H. (1966) Some chem i cal ob ser va tions on post-gla - cial lake sed i ments. Philo soph i cal Trans ac tions of the Royal So - ci ety, Lon don, B, 250 (765): 165–213.
Malkiewicz M. (2002) The his tory of veg e ta tion of the Eemian integlacial in the Great Pol ish Low land. Acta Societatis Botanicorum Poloniae, 71: 311–321.
Mamakowa K. (1988) Pol len stra tig ra phy of Eemian and ad join ing gla cial de pos its based on con tin u ous se quences in Po land. Bul - le tin of the Pol ish Acad emy of Sci ences, Earth Sci ences, 36:
299–307.
Mamakowa K. (1989) Late Mid dle Pol ish Gla ci ation, Eemian and Early Vistulian veg e ta tion at Imbramowice near Wroc³aw and the pol len stra tig ra phy of this part of the Pleis to cene in Po land. Acta Palaeobotanica, 29: 11–176.
Manikowska B. (1993) Min er al ogy and abra sion of sand grains due to Vistulian (Late Pleis to cene) ae olian pro cesses in Cen tral Po - land. Geologie en Mijnbouw, 72: 167–177.
Marks L. (2005a) Pleis to cene gla cial lim its in the ter ri tory of Po land.
Przegl¹d Geologiczny, 53: 988–993.
Marks L. (2005b) Pleis to cene river sys tem in the south ern peribaltic area as in di ca tion of inter gla cial sea level changes in the Bal tic Ba sin. Qua ter nary In ter na tional, 130: 43–48.
Marks L., Pochocka K. (1999) River val leys of the Eemian Inter gla - cial in cen tral Po land. Geo log i cal Quar terly, 43 (2): 163–168.
Meng S., Börner A., Strahl J., Thieke H.U. (2009) Bio- and lithostratigraphical in ves ti ga tions of Eemian fluviolacustrine sed - i ments and tills from the Lower Peene Val ley (NE Ger many). Pol - ish Geo log i cal In sti tute Spe cial Pa pers, 25: 37–48.
Miros³aw-Grabowska J., Niska M., Sienkiewicz E. (2009) Evo lu - tion of the paleolake at Ruszkówek (cen tral Po land) dur ing the Eemian Inter gla cial based on iso tope, cladoceran and di a tom data. Jour nal of Paleolimnology, 42: 467–481.
Mojski J.E. (2005) Ziemie polskie w czwartorzêdzie. Zarys morfogenezy. Pañstwowy Instytut Geologiczny, Warszawa.
Mycielska-Dowgia³³o E. (1995) Se lected tex tural fea tures of de pos - its and their in ter pre ta tion value (in Pol ish with Eng lish sum - mary). In: Badania osadów czwartorzêdowych (ed. E.
Mycielska-Dowgia³³o): 220–235. Wyd. Wydzia³u Geografii i Studiów Regionalnych Uniwersytetu Warszawskiego.
Noryœkiewicz B. (1978) The Eemian Inter gla cial at Nak³o on the River Noteæ (N Po land) (in Pol ish with Eng lish sum mary). Acta Palaeobotanica, 19: 67–112.
Noryœkiewicz B. (1999) Palynology of biogenic sed i ments of the Eemian Inter gla cial at Krzy¿ówki near Ko³o, cen tral Po land. Geo - log i cal Quar terly, 43 (1): 107–111.
Nowacki K. (1995) Objaœnienia do Szczegó³owej Mapy Geologicznej Polski w skali 1:50 000, arkusz D¹bie. Pañstwowy Instytut Geologiczny, Warszawa.
Nowaczyk B., Tobolski K. (1980) Re marks on Late-Gla cial limnic sed i ments ac cu mu lated in the wa ter en vi ron ment (in Pol ish with Eng lish sum mary). Badania Fizjograficzne nad Polsk¹ Zachodni¹, 33: 65–78.
Okruszko H. (1976) Zasady rozpoznawania i podzia³u gleb hydrogenicznych z punktu widzenia potrzeb melioracji.
Biblioteka Wiadomoœci, Instytut Melioryzacji i U¿ytków Zielonych, 52: 7–53.
Paw³owski D. (2011) Evo lu tion of an Eemian lake based on Cladocera anal y sis (Konin area, Cen tral Po land). Acta Geologica Polonica, 61: 441–450.
Petera J. (2002) Vistulian val ley de pos its in the Uniejów Ba sin and their palaeo geo graphi cal sig nif i cance) (in Pol ish with Eng lish sum mary). Acta Geographica Lodziensia, 83: pp. 164.
Racinowski R., Szczypek T., Wach J. (2001) Prezentacja i interpretacja wyników badañ uziarnienia osadów czwartorzêdowych. Wydawnictwo Uniwersytetu Œl¹skiego.
Reimann C., Arnoldussen A., Boyd R., Finne T.E., Koller F., Nordgulen Ø., Englmaier P. (2007) El e ment con tents in leaves of four plant spe cies (birch, moun tain ash, fern and spruce) along anthropogenic and geogenic con cen tra tion gra di ents. Sci ence of the To tal En vi ron ment, 377: 416–433.
Skompski S. (1983) Eemian inter gla cial mol lus cans from ¯migród upon the Barycz River (in Pol ish with Eng lish sum mary).
Kwartalnik Geologiczny, 27 (1): 151-187.
Stankowski W., Krzyszkowski D. (1991) The Qua ter nary stra tig ra - phy of the Konin area (in Pol ish with Eng lish sum mary). In:
Przemiany œrodowiska geograficznego obszaru Konin – Turek (ed. W. Stankowski): 11–31. Inst. Badañ Czwartorzêdu Uniwersytet im. Adama Mickiewicza w Poznaniu.
Stankowska A., Stankowski W. (1988) Max i mum ex tent of the Vistulian Ice Sheet in the vi cin ity of Konin, Po land: a geomorphological, sedimentological and ra dio met ric ev i dence.
Geographia Polonica, 55: 141–150.
Stankowski W., Tobolski K. (1981) Eemian peat and lac us trine de - pos its from the Kazimierz ex po sure of the brown coal mine Konin – pre lim i nary re port (in Pol ish with Eng lish sum mary). Badania Fizjograficzne nad Polsk¹ Zachodni¹, 34: 171–178.
Sza³amacha G., Skompski S. (1999) Biogenic sed i ments of the Eemian Inter gla cial at Krzy¿ówki near Ko³o, cen tral Po land. Geo - log i cal Quar terly, 43 (1): 99–105.
Szeroczyñska K. (1998) Cladocera as in for ma tion source in stud ies of lake sed i ments (in Pol ish with Eng lish summary). Studia Geologica Polonica, 112: 9–28.
Szeroczyñska K., Sarmaja-Korjonen K. (2007) At las of subfossil Cladocera from Cen tral and North ern Eu rope. Friends of Lower Vistula So ci ety, Œwiecie.
Tobolski K. (1986) Paleobotanical stud ies of the Eemian inter gla cial and Early Vistulian at W³adys³awów in the vi cin ity of Turek (Pre - lim i nary re port). Qua ter nary Stud ies in Po land, 7: 91–101.
Tobolski K. (1991a) Biostratigraphy and palaeo ec ol ogy of the Eemian Inter gla cial and the Vistulian Gla ci ation of the Konin re - gion (in Pol ish with Eng lish sum mary). In: Przemiany œrodowiska geograficznego obszaru Konin – Turek (ed. W. Stankowski):
45–87. Wydawnictwo Naukowe Uniwersytetu im. Adama Mickiewicza w Poznaniu.
Tobolski K. (1991b) Eemian and Vistulian biostratygraphy of Great Po land-Kujawy Low land (in Pol ish with Eng lish sum mary). In:
Geneza, litologia i stratygrafia utworów czwartorzêdowych (ed.
A. Kostrzewski). Uniwersytetu im. Adama Mickiewicza w Poznaniu, Seria Geografia, 50: 573–583.
Trzmiel B. (1996) Objaœnienia do Szczegó³owej Mapy Geologicznej Polski w skali 1:50 000, arkusz Turek (550). Pañstwowy Instytut Geologiczny, Warszawa.
Turkowska K., Forysiak J., Petera J., Miotk-Szpiganowicz G.
(2004) A Warta River sys tem dur ing the Youn ger Dryas in the Ko³o Ba sin (Mid dle Po land). Questiones Geographicae, 23:
83–107.
White side M.C. (1970) Dan ish Chydorid Cladocera: mod ern ecol ogy and core stud ies. Eco log i cal Mono graphs, 40: 79–118.
Widera M. (1998) Palaeomorphological and palaeotectonical evo lu - tion of the Konin El e va tion (in Pol ish with Eng lish sum mary).
Geologos, 3: 55–103.
700 Joanna Petera-Zganiacz, Ryszard K. Borówka, Jacek Forysiak, Gra¿yna Miotk-Szpiganowicz and Dominik Paw³owski
