Palaeoenvironmental and climate changes recorded in the lacustrine sediments of the Eemian Interglacial (MIS 5e) in the Radom Plain (Central Poland)

Quaternary International xxx (2016) 1e14

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Palaeoenvironmental and climate changes recorded in the lacustrine sediments of the Eemian Interglacial (MIS 5e) in the Radom Plain (Central Poland) * _ Marcin Zarski , Hanna Winter, Magdalena Kucharska Polish Geological Institute e National Research Institute, Poland

a r t i c l e i n f o

a b s t r a c t

Article history: Received 9 February 2016 Received in revised form 8 November 2016 Accepted 1 December 2016 Available online xxx

The Radom Plain is a region with numerous fossil palaeolakes that formed a palaeolakeland. Lacustrine sediments of thickness varying from 0.5 to 18 m were encountered in numerous boreholes. Pollen analyses of the sediments filling the palaeolakes have proven that their sedimentation began after the retreat of the Saalian ice-sheet (MIS 6), continued during the Eemian Interglacial (MIS 5e), and terminated at the beginning of the Weichselian Glaciation (MIS 5d). Climate and palaeoenvironmental changes have been recorded in different deposits: muds, peats and gyttja. Local factors, such as reservoir depth, and geological conditions have influenced the type of the accumulated sediments. Eemian sites occur in two geomorphological positions: in small depressions on the glacial plateau and in small valleys in oxbow palaeolakes. Eemian lakes were formed from the melting of dead-ice blocks. Pollen data obtained from the palaeolake sediments document climate and vegetation changes characteristic of the Late Glacial period, the Eemian Interglacial, and the beginning of the Weichselian Glaciation. In many sites, a record of a complete Eemian succession is present, whereas in others it is fragmentary. Comparison of pollen data between the Radom region and other localities in Poland shows local and regional differences in the development of forest communities in the Eemian. In the Eemian sequences of the Radom Plain, a considerable contribution of Tilia, Picea and Abies pollen is distinct in the forest communities, often higher than in other Eemian sites of Central Poland. The particularly high percentage of Tilia (exceeding 30%), Picea (up to 67%) and Abies (30%) pollen are recorded in the Babin site. This phenomenon may indicate favourable environmental and climate conditions, facilitating further propagation of these trees. In the pollen record from the Babin site, three distinct abrupt/cool climate oscillations have been noted, with the oldest one recorded in the Saalian Glaciation. The two younger oscillations have been distinguished at the very beginning and at the very end of the Last Interglacial, respectively. Eemian sites from the Radom Plain are important for the reconstruction of palaeoenvironmental and palaeoclimate changes in the Eemian Interglacial in Poland and Europe. © 2016 Elsevier Ltd and INQUA. All rights reserved.

Keywords: Pollen analysis Eemian Interglacial Palaeolake Palaeoenvironmental changes Radom Plain

1. Introduction Deposition of sediments with the record of environmental and climate changes during the last interglacial (Eemian Interglacial, MIS 5e) (Mangerud, 1989) took place in various accumulation basins such as lakes, seas and oceans, volcanic craters and in various facies of fluvial and peat sediments. However, the reconstruction of environmental and climate changes of this interglacial is most precise based on data obtained from terrestrial sediments (Zagwijn,

* Corresponding author. _ E-mail address: [email protected] (M. Zarski).

1961, 1989, 1996; Andersen, 1966; Wijmstra and Smit, 1976; Beaulieu and Reille, 1984, 1992; Grüger, 1989; Litt, 1994; Mamakowa, 1989; Turner, 2002; Borisova, 2005; Velichko et al., 1991; Tzedakis et al., 2003; Seiriene and Kondratiene, 2005; Velichko et al., 2005; Brewer et al., 2008; Novenko et al., 2008; Boettger et al., 2009; Mirosław-Grabowska, 2009; MirosławGrabowska et al., 2015; Kupryjanowicz et al., 2016), and to a lesser degree e marine sediments (Seidenkrantz and Knudsen, ~ i et al., 1999, Seidenkrantz et al., 2000; Head 1997; S anchez Gon et al., 2005; Marks et al., 2013; Otvos, 2015). Based on pollen data, changes in vegetation indicate a specific trend in the vegetation succession, at first with the very high contribution of

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Quercus, followed by Corylusin forest communities, preceding the development of multispecies forests with Carpinus, Tilia, Acer andwith gradually entering Picea and Abies. The beginning and end of the interglacial is recorded in the development of pine-birch forests, in which trees with higher climatic requirements, such as Ulmus and Fraxinus, appeared and disappeared. High resolution palinological investigations of terrestrial sediments, coupled with other investigations, including studies of marine (McManus et al., 1993; Seidenkrantz and Knudsen, 1997) and ice cores (Grootes et al., 1993; Jouzel et al., 1996), have allowed for a detailed reconstruction of climate changes during this interglacial. Although climate changes in Western and Central Europe had a larger amplitude than in Southern Europe, numerous pollen data have indicated that the climate of the Eemian Interglacial was stable and did not reveal larger fluctuations (Guiot et al., 1989, Zagwijn, 1996; Aalbersberg and Litt, 1998; Kühl and Litt, 2003; Klotz et al., 2004). The record from high resolution pollen sequences has indicated the presence of short-term cool or arid climatic oscillationsin the nchez Gon ~ i et al., 2005; oldest interglacial (Cheddadi et al., 1998; Sa Müller et al., 2005; Sirocko et al., 2005; Seelos and Sirocko, 2007; Karabanov et al., 2000). Controversial results obtained from the Bispingen profile (Field et al., 1994) have pointed to a strong cooling during the Carpinus phase, not recorded in other profiles from Europe that were investigated using numerical methods (Guiot et al., 1989; Litt et al., 1996; Kühl and Litt, 2003; Klotz et al., 2004). A cold event at the termination of the Eemian Interglacial has also been observed in many long pollen sequences from Poland (Kupryjanowicz et al., 2016). The occurrence of climate oscillations during the interglacial obtained from pollen data has been supplemented with data from marine (McManus et al., 1993; Seidenkrantz and Knudsen, 1997) and ice cores (Greenland Icecore Project (GRIP) Members, 1993; Grootes et al., 1993; Jouzel et al., 1996; North Greenland Ice Project members, 2004, The North Greenland Eemian Ice Drilling-NEEM (Community Members, 2012), indicating the instability of Eemian climate. The majority of sites in Poland with lake sediments from the Eemian Interglacial (MIS 5e, Martinson et al., 1987) occur in a parallel belt in the central and eastern part of the country, between the maximal range of the last main phase of the Weichselian Glaciation (Kupryjanowicz, 2008; Kupryjanowicz et al., 2016; Marks, 2011, 2012) and the maximal range of the Saalian Glaciation (MIS-6; Cohen and Gibbard, 2010), particularly the Wartanian Stadial (Bruj and Roman, 2007; Lindner and Marks, 2012). The northern range of this occurrence is marked by the 51
300 northern meridian, and the southern e by the 53
300 northern meridian. Apart from this belt, sites with lake sediments are rather rare. In northern Poland, lake sediments are covered by a thick complex of glacial deposits from the Weichselian Glaciation (Marks, 2012), whereas in the south they have been removed by processes of erosion. Eemian lakelands continue to the west in Germany, where they have been recognized to the south of the maximal range of the €rner Weichselian Glaciation (Menke, 1982; Caspers et al., 2002; Bo et al., 2015), as well as in the Netherlands (Bosch et al., 2000). Similarly as in Poland, these lakelands are dominated by small palaeobasins resulting from the melting of dead ice blocks after the Saalian Glaciation (MIS 6). Relatively numerous palaeobasins with sediments from the Eemian Interglacial occur also in Belarus, Lithuania, Ukraine and Russia (Marciniak et al., 2007; Pavlovskaya,  nas et al., 1998; Satku  nas and Grigiene, _ 2012; Lozhkin 2000; Satku and Anderson, 1991; Borisova, 2005). Therefore, one of the aims of this paper, beside the reconstruction of the palaeoenvironment in the study area by the correlation of pollen and sedimentological data, is estimation of climate changes and documentation of short-term climatic events.

2. Study area and geological setting The investigated area (Radom Plain) is located in the southern zone with sites demonstrating Eemian sediments (Fig. 1) _ _ (Kucharska, 2009; Zarski, 2014; Zarski et al., 2010, 2015) and thus is a part of the huge palaeolakeland. The Radom Plain occurs in the transitional zone between the influence of continental and oceanic climates. The mean annual temperature for this zone exceeds 7.5
C (Okołowicz and Martyn, 1984; Chrzanowski, 1991). So far, the state of knowledge on the palaeoclimate and palaeoenvironment of the Radom Plain area during the Eemian Interglacial was not satisfactory. The discovery of over a dozen sites with sediments of this age during the preparation of the Detailed Geological Maps of Poland (Złonkiewicz, _ 2001; Kucharska, 2009; Zarski, 2014) has contributed to pollen analysis in selected sites, which enabled recognizing the floral, palaeoclimate and palaeoenvironmental changes of the Radom Plain in the Eemian Interglacial, and presenting the specific climate of the region in the studied interval. The study area is located within the Radom Plain (Kondracki, 2001), located in the southern part of the Mazovian Lowland. From the south, the Radom Plain borders with the foreland of the Holy Cross Mountains, which are part of the Małopolska Upland. The ground surface is generally located at 160e180 m a.s.l. The glacial plateau of the Radom Plain is cut by valleys of small rivers, which are tributaries of the Vistula River. The surface is generally covered by glacial tills, in places by fluvioglacial sands of the Saalian _ Glaciation (MIS 6) (Kucharska, 2009; Zarski, 2014), the ice-sheet of which was the last to cover the study area. Large parts of the area are covered by eolian sands and dunes, formed at the end of the Weichselian Glaciation. River valleys are filled with sands, gravel and muds of the Weichselian Glaciation, and by Holocene peats, _ muds and sands (Kucharska, 2009; Zarski, 2014). Sites with lacustrine and biogenic sediments of the Eemian Interglacial are present in the Radom Plain in two geomorphological positions: on the plateau and in the valleys. The plateau sites are located in small depressions, usually landlocked, on a post-glacial plateau built of _ glacial tills (Zarski, 2014). The valley sites are situated in contemporary valleys of small streams that incise the post-glacial plateau. Preparation of subsequent sheets of the Detailed Geological Map of Poland has induced pollen studies in several sites that are briefly described below. Based on pollen data, the Saalian/Eemian and Eemian/Weichselian boundaries have been distinguished in the  ski, 2007a, 2007b, 2008, 2009). sections (Krupin 2.1. Plateau sites  w (l e 21
400 18.500 , 4 e 51
230 26.300 - WGS 84, h e Łuczyno 168 m a.s.l), Nowy Zamos c (l e 21
4401.800 , 4 e 51
2108.400 , h e  w( l e 21
440 46.700, 4 e 51
230 43.800 , h e 165 m a.s.l.) and Floriano  170 m a.s.l.) are located in landlocked depressions near Zwolen vicinity (Fig. 1). Length and width of these depressions reach about 60e150 m. The lithological column for these boreholes is presented in the compilation (Fig. 2). The boreholes terminated in glacial tills of the Saalian Glaciation (MIS 6). The tills are covered by diluvialw, Nowy Zamos slope sands (Łuczyno c) or ice-dammed muds w) overlain by Eeemian lake muds, peats and gyttjas. The (Floriano biogenic series reaches a thickness of: 4.10 m, 4.15 m and 3.90 m. Above the interglacial sediments occur muds (Nowy Zamos c, Flow), diluvial sands (Łuczyno w) of the Weichselian Glaciation riano and Holocene peats or humus horizon (Fig. 2). 2.2. Valley sites Policzna (l e 21
370 20.900 , 4 e 51
260 31.300 , h e 163 m a.s.l.),

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Fig. 1. Location sketch-map of the Radom Plain with Eemian sites.

 ski (2007a,b, 2009) and Winter in this Fig. 2. Stratigraphic and palinostratigraphic correlation of the analyzed sequences based on local pollen assemblage zones L PAZ after Krupin paper and regional pollen assemblage zones R PAZ (Mamakowa, 1989).

 w (l e 21
41017.900 4 e 51
200 7.200 , h e 161 m a.s.l., Fig. 3), Mirko  w (l Babin (l e 21
41028.500 , 4 e 51
190 27.800 , h e 159 m a.s.l.), Mako e 21
150 25.0000 , 4 e 51
200 35.5000 , h e 178 m a.s.l., Czarna Rola (l e 21
150 54.0000 , 4 e 51
200 21.5000 , h e 179 m a.s.l.) are located in small

 and Radom vicinity (Fig. 1). The series of river valley near Zwolen Eemian sediments (lacustrine muds, peats and gyttjas) directly overlies glacial tills of the Saalian Glaciations. The Eemian lake series reaches a thickness: 2.35 m, 6.05 m, 5.42 m, 2.20 m, 1.90 m

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sediments were treated with heavy liquid and then subjected to Erdtman's acetolysis. At least 250 pollen grains were counted per sample. The calculation of percentages is based on the total terrestrial pollen sum (AP þ NAP), excluding pollen of aquatic plants, spores, and reworked sporomorphs; the latter comprised sporomorphs of pre-Quaternary age. 4. Results 4.1. Biostratigraphic age assignment

_  w site (photo M. Zarski). Fig. 3. Mirko

(Fig. 2). Sediments from the Weichselian Glaciation include fluvial and dyluvial sands, lacustrine muds cover the Eemian sediments  w site. except Mirko w, the transition between the Eemian Interglacial In the Mirko and the Weichselian Glaciation e Early Weichselian, Herning Stadial (Behre, 1989) occurs within the peats at the depth of 6.05 m. €rup Interstadial and the Redestall Stadial are above Peats of Bro  w is (Fig. 2). The sequence of lacustrine-swamp sediments in Mirko terminated by a Weichselian laminated mud and fluvial sands. The sequence in all profiles is capped by Holocene peats or fluvial sands. Based on geological data, including lithological differences between the sediments, it can be concluded that the Eemian reserw, although located within one shallow voirs in Babin and Mirko valley, were isolated from one another. The remaining valley sites with Eemian sediments, in which pollen analyses were conducted include Sławno (Tołpa, 1961),  ski, 2007b, 2008). In Sławno, the Adolfin and Ponikwa (Krupin peats, gyttja and peaty shales reach 17 m in thickness (Tołpa, 1961; Rühle, 1961). The Ponikwa site is located in a landlocked depression within the wide Krypianka valley (Fig. 1). The thickness of the Eemian biogenic series encompassing gyttja, peats and muds rea_ ches 13 m (Zarski, 2014). Biogenic sediments occurring in valley depressions and assigned to the Eemian Interglacial were _ encountered in boreholes pierced in Kijanki, Okre˛ znica _ (Karaszewski, (Złonkiewicz, 2001), Ła˛ czany (Barcicki, 1990), Rozki w (Jaskowski et al., 1992) (Fig. 1). In Kijanki 1975) and Franciszko _ and Okre˛ znica, the biogenic series reaches a thickness of about 4 m, _ e 8 m, and Franciszko  w e 16 m. Usually in Ła˛ czany e 5 m, Rozki glacial tills of the Saalian Glaciation (MIS 6) occur below the lacustrine and swamp sediments in these sites, whereas Weichselian muds and sands, and partly also Holocene peats occur above. 3. Methodology Pollen analysis was carried out for the biogenic sediments from palaeolakes discovered during the preparation of the Detailed Geological Map of Poland in the scale 1: 50 000. Due to the thickness of the Babin sequence, the series between 3.11 and 8.95 m was subject to high-resolution investigations. Sediments from the other sites were subject to low-resolution studies. Thus, pollen analysis w, 26 samples from Nowy was made for 16 samples from Łuczyno  w, 10 samples from Policzna, 6 Zamos c, 46 samples from Mirko w, 15 samples from Czarna Rola, and 7 samples from Floriano w (Krupin  ski, 2007a,b, 2009). samples from Mako All samples subject to pollen analysis were covered with 10% HCl and later boiled in 10% KOH. To remove the mineral fraction, the

The pollen record obtained from the sites on the Radom Plain exhibits vegetation changes indicating an Eemian age of the studied sediments (Tables 1e7, Figs. 4e7). The sequence begins with the expansion of birch and pine, preceding the encroaching of oak and elm, a prominent Quercus and Corylus phase, associated with Fraxinus, Tilia and Taxus and the presence of Hedera and Viscum. Next, Picea, Abies, Ilex and Buxus appear in the Carpinus phase. Such trend of changes is representative for the Eemian Interglacial in the entire north-western and central Europe (Zagwijn, 1961; Andersen,  ka and 1974; Mamakowa, 1989; Litt et al., 1996; Kuszel, 1997; Bin ~ i, 2007; Nitychoruk, 2003; Granoszewski, 2003; S anchez Gon Malkiewicz, 2008; Kupryjanowicz, 2008; Winter et al., 2008; Granoszewski et al., 2012). However, due to the low-resolution of the pollen records from the Radom Plain, excluding the Babin site, there is no record of climate oscillations from the Eemian Interglacial for this area. 4.2. Palinostratigraphy of the pollen records Pollen data from particular succession have been the base of  ski, local pollen assemblage zones L PAZ (Tables 1e6) (Krupin 2007a,b, 2009)and pollen diagrams (Figs. 4e7), which were the base to reconstruct the vegetation and climate changes in the Radom Plain. Unfortunately, lack of numerical data from the  w succession did not allow to prepare a pollen diagram for Mirko this site. In many profiles from the study area, the zones were distinguished based on a single sample, but the state of recognition of the pollen sequence from different parts of Poland based on about 200 profiles studied, and correlation of local assemblage zones with the regional pollen subdivision for Poland (Mamakowa, 1989) allows for a precise correlation (Kupryjanowicz et al., 2016). 5. Discussion A characteristic feature of all Eemian palaeolakes on the Radom Plain and in other parts of Poland (Klatkowa, 1997; Kupryjanowicz, 2007, 2008; Bruj and Roman, 2007; Forysiak, 2015) are their small sizes, not exceeding the diameter of several hundreds of metres, and a small depth rarely exceeding 10 m. They were small, progressively overgrowing lakes. The origin of Eemian lakes occurring w, Floriano w) and valleysites in the plateau (Nowy Zamos c, Łuczyno w, Czarna Rola, Mako w, Policzna) (Fig. 1) is related (Babin, Mirko mainly to the melting of dead-ice blocks. The process of lake formation from dead-ice blocks is commonly known and has been € se, 1995; Błaszkiewicz, 2005, 2008). In the extensively described (Bo valley sites, dead-ice blocks were situated in shallow troughs that in the and Weichselian times were transformed into river valleys (Klatkowa, 1997). Up to 12 m deep depressions were formed on the ground surface after melting of ice. Based on pollen and lithological analyses in the sections, it can be estimated that the rate at which ice melted differed among the various depressions. This process was described for Late Weichselian (Błaszkiewicz, 2005) and Eemian lakes (Kupryjanowicz, 2007, 2008). The largest ice-

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Table 1 Babin description of Local Pollen Assemblage Zones. L PAZ after Winter

Depth in m

Description of L PAZ

Ba 14 NAP-Artemisia-Betula

3.55e2.11

Ba 13 Pinus-NAP

4.15e3.55

Ba 12 Betula-Picea-Pinus

4.58e4.15

Ba 11 Pinus-Picea Ba 10 Picea-Abies-Carpinus

4.7e4.58 5.28e4.7

Ba 9 Carpinus-Picea-Abies

5.48e5.28

Ba 8 Carpinus-Corylus-Tilia

7.08e5.48

Ba 7 Corylus-Quercus-Tilia

7.50e7.08

Ba 6 Quercus-Ulmus-Fraxinus

7.80e7.50

Ba 5 Pinus-Quercus-Ulmus

8.04e7.80

Ba 4 Pinus-Betula

8.55e8.04

Ba 3 Betula-Artemisia

8.75e8.55

Ba 2 Betula-NAP-Salix

8.91e8.75

Ba 1 Pinus-NAP-Cyperaceae

8.95e8.91

NAP contribution rises above 42%. Pollen of herbaceous plants is dominated by Artemisia above 26%, Cyperaceae and Poaceae. Taxa such as Chenopodiaceae (up to 1.8%), Caryophyllaceae (up to 1.3%). Asteraceae (up to 1.3%) and Thalictrum (0.7%) also appear. Increase in Pinus values above 70% and decrease in Betula (down to 10%) and Picea below 2% are characteristic of the zone. Pollen of Larix and Salix appears. Values of NAP rise up to 21%, particularly of Artemisia (up to 10%), Poaceae and Cyperaceae. Zone characterized by the increase of Betula pollen (above 72%) and the fall of Pinus contribution; Picea reaches up to 3% and Abies is also present. Increase of Pinus pollen above 81% and a gradual fall of Picea and Abies contribution is visible in the zone. Picea and Abies pollen attains the maximal values, up to 68% and 32.3%, respectively. However, Abies reaches the maximal contribution earlier than Picea, and the fall in the contribution of Carpinus below 3% is synchronous with the fall of Abies. Although pollen of thermophilous trees is rare, the presence of Buxus pollen has been noted in the zone. Pollen of Carpinus still attains high values up to 42%, but values of Picea (up to 27%) and Abies (up to 7.5%) also rise. The contribution of Quercus and Tilia falls, but Corylus reaches up to 16%. Pollen of Ulmus, Fraxinus, Acer, Hedera and Viscum disappears. Zone characterized by the rise of Carpinus above 62%, and the fall in Tilia contribution. The content of Corylus is still high and reaches even up to 45%, although it generally oscillates between 14% and 22%. Pollen of Picea and Acer appears. Hedera is still present, Viscum appears, and by the end of the zone e also Ilex. Rapid increase of the contribution of Corylus (above 45%) and the fall in the contribution of Quercus took place in Zone Ba 7. Equally rapid is the increase of Tilia (up to 32%) and Carpinus (up to 14%). The contribution of Fraxinus falls, but that of Alnus increases. Zone has the maximal contribution of Quercus (66%) and an increasing contribution of Fraxinus (up to 2.2%). The content of Ulmus is insignificant. A rapid fall of Quercus to 24% and an increase in Pinusabove 59% were noted in a sample from depth 7.61 m. Increasing contribution of Pinus pollen up to 80% is correlated with the decrease of Betula values. The contributions of Quercus and Ulmus (2, 2%) are higher, and Hedera pollen appears. Zone has high values of Pinus (up to 69%) and significant values of Betula. Pollen of Ulmus and Quercus appears. The Betula Subzone was distinguished in the zone, in which the values of Pinus decrease and the values of Betula increase above 38%. Increasing contribution of Betula pollen above 67% and decrease of pollen of herbaceous plants below 15.2%, with Artemisia up to 6% and Cyperaceae at 5.6% characterize this zone. Changes are reflected in the decrease of Pinus pollen, increase of Betula pollen to 51% and Salix above 1.5%, and increase of NAP values up to 27%. The main taxa of herbaceous plants are: Artemisia (16.10%), Cyperaceae (17.2%), Poaceae (3.4%), Chenopodiaceae (3%), and Asteraceae (1.7%). Zone dominated by tree pollen: Pinus (above 61%), Betula (8.9%) and Picea (1.7%). NAP contribution reaches up to 26% and is dominated by the Cyperaceae (18.8%) and Artemisia (up to 5%).

w. After melting of ice, but still dammed lake was formed in Floriano during the glacial period, an ice-dammed lake was formed in the depression, with an initial depth reaching probably down to 10 m, and in which muds were accumulated. Lack of high-resolution pollen data did not allow further recognition of the development w and Nowy Zamosc, after the of this reservoir. In Policzna, Łuczyno retreat of the Saalian ice-sheet, diluvial sands from the closest vicinity were accumulated in the existing depressions. It cannot be excluded that they were deposited on the surface of dead-ice blocks w and Policzna, ice-dammed res(Błaszkiewicz, 2005). In Łuczyno ervoirs with mud accumulation were formed after the sand accumulation.

5.1. Dynamics of vegetation, climate and palaeoenvironmental changes Pollen data from the Radom Plain allowed to recognize the evolution of vegetation and climate changes and correlate them with Regional Pollen Assemblage Zones (R PAZ) distinguished for the Late Saalian Glaciation, Eemian Interglacial and Early Weichselian by Mamakowa (1989) (Table 7). w, Nowy Zamos  w record a Pollen data from Łuczyno c and Mirko complete Eemian floral succession encompassing pollen zones E1  ski 2007a, 2009). The studied to E7 (Figs. 2, 4e6, Table 7); Krupin sections have also documented the Early Weichselian: Zone EV1  w section e corresponding to the Herning Stadial, and in the Mirko €rup Interstadial and Zone EV3 Zone EV2 corresponding to the Bro  ski, 2009). The Czarna corresponding to the Redestal Stadial (Krupin Rola succession shows the record of pollen zones from E2 to E7

 ski, 2007b), the Policzna succession e zones (Table 7, Fig. 2; Krupin  ski, 2009), and Mako w e zones E3, E4 and E5 E1, E2 and E5 (Krupin  ski, 2007b). (Table 7, Fig. 2; Krupin The record of vegetation and climate changes at the end of the Saalian Glaciation is registered in Babin site and indicates the presence of lake reservoirs already at this time. In the Late Saalian Glaciation (Zone LG MGP NAP-Picea-Pinus), the area of the Radom Plain was overgrown by loose pine forests with birch and a small admixture of spruce, and by small patches of various vegetation in open habitats. Such vegetation communities evidence boreal climate conditions. Cooling and increase of climate continentalization/aridization are evidenced by the proliferation of communities of steppe-like open habitats formed by Artemisia and Chenopodiaceae, and tundra-like habitats with Cyperaceae, Poaceae and bushes of Salix and Juniperus. A significant vegetation change took place in Zone E1 PinusBetula, reflected in the increase of birch contribution followed by pine, and evidencing a gradual warming. However, a significant decline of pine forests in favour of birch, which became the main forest component, took place in the Betula Subzone. Such shortterm cool/arid climate oscillation was distinguished only in the Babin succession, and does not have equivalents in other pollen records from the Radom Plain. Nevertheless, it is distinct in other successions from Poland, including Imbramowice (Mamakowa, 1989), Rzecino (Winter et al., 2016; in this volume), and ZgierzRudunki (Jastrze˛ bska-Mamełka, 1985). Climate warming in the Eemian Interglacial (Zone E1) resulted in the formation of 5e12 m deep lakes in almost all reservoirs, with  w. Lake formation was the exception of Czarna Rola and Mako

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6 Table 2 Mirkow description of Local Pollen Assemblage Zones.  ski L PAZ after Krupin (2009)

Depth in m

Description of L PAZ

MIR-15 NAPeArtemisiaPinus

2.65e1.70

MIR-14 Equisetum-PinusSalix

2.85e2.65

MIR-13 Pinus-NAP e(Artemisia)

4.75e2.85

MIR-12 Pinus-(Betula)

5.15e4.75

MIR-11 Betula-Pinus

5.25e5.15

MIR-10 Pinus-(Betula-NAP)

5.55e5.25

MIR-9 NAP-(PinusArtemisia)

6.05e5.55

MIR-8 Pinus-(NAP)

9.55e6.05

MIR-7 Picea-Abies(Carpinus-Pinus)

10.05e9.55

MIR-6 Carpinus-(CorylusAlnus)

10.60e10.05

MIR-5- Cortylus-TiliaCarpinus

11.15e10.60

MIR-4 Corylus

11.55e11.15

Zone with high contribution of NAP up to 69%, with dominating Poaceae (up to 29%), Cyperaceae (11%) and Ranunculus of the Batrachium type at 21% and Artemisia (5e6%). The taxonomic composition of pollen of herbaceous plants is similar as in the previous zones. Among trees a higher frequency is noted for Pinus and Betula. Low contribution of Salix (up to 0.8%) and Juniperus (up to 0.5%). Zone with high values of Eqisetum up to 56%. Contribution of Pinus is up to 63%, Betula e up to 12%, and Salix e up to 1%. Contribution of NAP falls down to 16%, heliotrophic taxa disappear, whereas Gramineae (7%), Cyperaceae (13%) and Artemisia (1.6%) are still present. Contribution of Pinus and NAP pollen is still significant, at 45e59% and 26e34%, respectively. The values of Betula fall (10 e14%) and those of Picea rise to 3.7%. Among herbaceous plants dominate Gramineae (8e15%), Cyperaceae (up to 12%) and Artemisia (2e3%). Present is pollen of Ericaceae, Apiaceae, Caryaophyllaceae, Chenopodiaceae, Asteraceae, Rubiaceae, Thalictrum, Ranunculus, Armeria type A, P. major/media and H. oelandicum. Values of Pinus rise up to 66%, and those of Betula decrease to 16%. In the upper part of the zone NAP values rise to 16%, along with the taxonomic diversity. Zone with significant contribution of Pinus (45%) and Betula (35%), the contribution of other trees is insignificant, and the pollen of Hippophae appears. The values of NAP reach 16%. Values of Pinus rise to 54% and Betula e up to 28%, whereas the values of NAP decrease to 16%. The contribution of the remaining trees is lower. Decrease in the values of particular taxa of herbaceous plants is significant, and the taxonomic diversity is much lower. Poaceae (15-6%), Cyperaceae (5e0.3%) and Artemisia (1.6e0.5%) still prevail. NAP reach high values (40e50%) with the dominance of Gramineae (18e20%), Cyperaceae (13e14%) and Artemisia (5 e7%). Taxonomic diversity is significantly high. Present are numerous heliophytes such as Centaurea montana, Plantago media/major, Polemonium, Helianathemum nummularia type and others. Tree pollen is represented by Pinus (24e26%), Betula (14e15%) and Picea (2e3%). The contribution of Carpinus is significant e up to 6%. Salix still attains the value of 2%, whereas Juniperus e 0.2e2%. Zone characterized by increased values of Pinus up to 76% and NAP up to 34%, contribution of other trees is low, and pollen of Salix is more common e up to 2%. Taxonomic diversity of NAP is high, whereas the Gramineae reach up to 11%, Cyperaceae e up to 17%, and Artemisia up to 2.9%. Contribution of Pinus rises to 50%, and contribution of Carpinus decreases. Picea and Abies reach 8e9% and 3e4%, respectively. Alnus does not exceed 11%. Pollen of Quercus, Ulmus, Fraxinus, Corylus, Betula, Taxus baccata, Tilia cordata type is present, pollen of Buxus and Fagus is sporadic. Contribution of Carpinus rises up to 57%, values of Corylus vary within 21%e24%, Tilia cordata type e within 3%e5%, and values of Alnus do not exceed 9%. Low contribution was noted for Quercus, Fraxinus, Ulmus, Taxus baccata and Picea. Pollen of Hedera, Ligustrum and Viscum is present. Values of Corylus pollen decrease to 26%, values of Carpinus rise to 38%, of Alnus e to 8%, and of Taxus e to 1%. Contribution of the remaining trees, excluding Tilia cordata type, is lower. Few pollen grains of Acer, Tilia platyphyllos type, Abies, Picea, Hedera, Viscum, Vitis and Viburnum also apperar. Corylus reaches the highest values up to 54% in the zone, in the Quercus subzone the values of Quercus reach 16% and then fall gradually. Pollen of Tilia cordata type z (5e8%), Carpinus (5e11%), Alnus (2e6%) and Taxus baccata (up to 0.9%) is present. Ulmus and Fraxinus are still present; Acer, Hedera and Evonymus appear sporadic. Values of Quercus rise to 52%, and of Pinus and Betula decrease. Pollen of Ulmus (4e5%) falls and the contribution of Fraxinus reaches up to 5%. In the Corylus subzone, values of Corylus reach up to 21%. Contribution of Pinus rises to 34%, and value of Betula decreases. Pollen of Quercus reaches values of 6%, Ulmus e 6% and Fraxinus e 1%. NAP values fall to 7.4%. Zone with the domination of Betula pollen to 61% and Pinus to 26%. Values of NAP do not exceed 11%, and Poaceae (6%) prevail.

Quercus MIR-3 Quercus

Corylus

MIR-2 Betula-Pinus(Ulmus) MIR-1 Betula-(Pinus-NAP)

11.75e11.55 11.85e11.75 12.00e11.85

induced by melting of dead-ice blocks and permafrost degradation (Błaszkiewicz, 2011; Kupryjanowicz, 2008; Forysiak, 2013). Gyttja w, Babin) and lacustrine muds (Łuczyno w, Nowy Zamos (Mirko c, Policzna) were accumulated in the lakes. Fall of Betula pollen and rise of Pinus pollen in Zone E2 PinusBetula-Ulmus indicate the return of pine forests enriched in Quercus. With the growing contribution of Ulmus, riparian forests developed along the rivers. Such changes in vegetation evidence gradual climate warming. Hedera appearing at the end of the zone signalizes mild winters with temperatures of the coldest month not falling below 2
C, or even higher: 1.5
C (Iversen, 1944; Zagwijn, 1996), and decline of climate seasonality. Improvement of climate conditions was evidently related to the transgression of the Eemian Sea (Marks et al., 2013). Lakes functioned in most reservoirs at this w, Łuczyno w, Policzna). In turn, the lake in Nowy time (Babin, Mirko Zamos c became shallower and was transformed into a peatland. In Czarna Rola, peats from Zone E2 directly overlie the glacial till from the Saalian Glaciation. Lack of Zone E1 may be the result of a slightly later melting of the dead-ice block (Kupryjanowicz, 2007, 2008). Another reason of the later formation of lakes could also be the fact w were very shallow that the depressions in Czarna Rola and Mako reservoirs with depths at 2e3 m, in which there were no conditions

for the development of a lake, whereas progressing warming and increasing evaporation favoured decrease of the water level. Expansion of Quercus, which was the predominant component of forest communities, is characteristic of Zone E3 and evidences gradual climate warming. Changes were also observed in riparian forests, in which Fraxinus commonly appeared. At the end of the zone, hazel (Corylus) has a wider range, and in Zone E4 it could have even formed individual shrubs (Mamakowa, 1989). Together with hazel, Tilia entered the forest communities; this tree became a very important forest component around the Babin lake. Such changes initially point to the development of mesophilous oak-linden forests hazel (Corylus), yew (Taxus) and maple (Acer). In the Babin pollen record, the contribution of Taxus is very low and does not exceed 0.5%, whereas in other sites its values reach up to 3%, indicating the insignificant role of yew in the forests. The mean temperatures of the winter months were at 1.5
C, and the mean temperatures of the summer months grew up to 18
C, as evidenced by the pollen of Trapa natans (Aalbersberg and Litt, 1998) in Babin. Similarly, the presence of fragments of Salvinia w, Policzna and microsporangia in the successions from Łuczyno Nowy Zamos c indicates favourable climate conditions (Mamakowa, 1989).

_ Please cite this article in press as: Zarski, M., et al., Palaeoenvironmental and climate changes recorded in the lacustrine sediments of the Eemian Interglacial (MIS 5e) in the Radom Plain (Central Poland), Quaternary International (2016), http://dx.doi.org/10.1016/j.quaint.2016.12.001

_ M. Zarski et al. / Quaternary International xxx (2016) 1e14

7

Table 3 Nowy Zamosc description of Local Pollen Assemblage Zones.  ski (2007a,b) L PAZ after Krupin

Depth in m

Description of L PAZ

ZA-11 NAP-Artemisia- Pinus

1.85e1.45

ZA-10 Pinus-(Betula-NAP)

2.05e1.85

ZA-9 Pinus-(Picea) ZA-8 Picea-Abies-(Carpinus)

2.35e2.05 2.55e2.35

ZA-7 Carpinus

3.05e2.55

ZA-6 Corylus -Tilia-Carpinus

3.45e3.05

ZA-5 Corylus-(Quercus)

3.85e3.45

ZA-4 Quercus-(Corylus)

4.65e3.85

ZA-3 Pinus-(Ulmus-Quercus)

5.05e4.65

ZA-2 Betula-(Pinus-NAP)

5.25e5.05

ZA-1 Pinus-Artemisia-Juniperus

5.55e5.25

Zone with high contribution of NAP up to 60%, including Gramineae (up to 22.6%), Cyperaceae (up to 25.2%) and Artemisia (up to 6%). Pollen of Chenopodiaceae, Caryophyllaceae, Brassicaceae, Ranunculus flammula type, R. acris type, Cichorioideae, Asteraceae, Rubiaceae, Saxifraga officinalis, Geum type and others is also present. The contribution of tree pollen includes Pinus and Betula above 16%, Salix up to 1%, and Juniperus not exceeding 1%. Zone dominated by NAP up to 41%, mainly Gramineae, Cyperaceae and Artemisia (3.3%). Pollen of trees includes Pinus (33%), Betula (16%), and Picea (4%). Values of Salix reach 1%. Contribution of Pinus rises to 58%, and values of Picea slightly decrease. Contribution of Carpinus (18e19%), other thermophilous trees and Alnus decrease. Values of Picea rise to 25% and Abies e to 19%. Pollen of Fraxinus, Ulmus and Taxus disappears in the upper part of the zone, and value of Pinus rises. Pollen of Carpinus reaches its highest contribution at 36e45%, and the contribution of Quercus, Tilia, Alnus and Ulmus decreases. The zone is subdivided into two subzones: the lower Corylus with values at 13e16%, and the upper, with values exceeding 12% and values of Abies up to 2%. Corylus (32e37%) again reaches high values, the contribution of Quercus (5e15%) decreases, whereas the values of Tilia cordata type (7e9%), Carpinus (8e29%), Alnus (3e5%), Taxus (1e2%), Fraxinus and Ulmus are higher. Pollen of Viscum appears. The zone with the highest contribution of Corylus (43e51%) and significant values of Quercus (21e30%). Values of Ulmus and Fraxinus decrease. Pollen of Tilia cordata type, Taxus baccata, Alnus and Acer appears, and Carpinus at the end of the zone. Pollen of Hedera and Cumulus appears, as well as microsporangia of Salvinia. High values are attained by Quercus up to 34%, the values of Pinus decrease to 15%, and of Corylus rise to 34%. Pollen of Ulmus rises to 4% and Fraxinus to 5%. Single pollen grains of Hedera and Vitis are present. Tree pollen dominates, with the prevalence of Pinus (41e47%) and Betula (26-17%), and an increasing contribution of Quercus up to 22% and Ulmus up to 3%. Pollen of Corylus and microspores of Salvinia is present. Tree pollen dominates, mainly Betula (43%) and Pinus (38%). The contribution of NAP reaches 15% and includes Gramineae (11%) and Cyperaceae. In the upper part of the zone the values of Quercus rise up to 9%. Zone with prevalence of AP up to 75% and NAP contribution up to 25%. AP are represented by Pinus (42e46%) and Betula (23e27%). Juniperus reaches values from 1% to 5%. Pollen of Pinus cembra and Salix is present, including morphotypes of tundra species. Hippophae and Ephedra distahya type appear. Herbaceous plants include Gramineae, Cyperaceae and Artemisia (5e6%).

Table 4 Luczynow description of Local Pollen Assemblage Zones.  ski L PAZ after Krupin (2007a,b)

Depth in m

Description of L PAZ

LU-8 Pinus-Betula-Artemisia

3.2e1,7

LU-7 Pinus

3.85e3.2

LU-6 Picea-Abies-Carpinus LU-5 Carpinus Picea-Abies Corylus

4.05e3.85 4.65e4.05

LU-4 Corylus-Tilia-Carpinus

4.85e4.65

LU-3 Corylus

5.15e4.85

LU-2 Quercus

5.35e5.15

LU-1 Pinus-Betula

5.55e5.35

Values of AP decrease, including Pinus down to 26%. Betula values increase to 36%. Values of NAP oscillate between 35% and 44%. This is mainly pollen of Gramineae (12e21%), Cyperaceae (8e14%) and Artemisia (6e9%). Pollen of herbaceous plants is taxonomically variable and represented by the Chenopodiaceae, Caryophyllaceae, Asteraceae, Apiaceae, Ranunculaceae, Thalictrum, Ranunculus acris type, Geum type and others. Zone dominated by pollen of Pinus (65e72%), values of Betula rise up to 19% and those of NAP e to 13%, including Artemisia (3.2%) beside Gramineae and Cyperaceae. Contribution of Carpinus is still significant, up to 32%. Values of Picea rise up to 16% and Abies e to 6%. Values of Carpinus (45e48%) and Alnus (up to 7%) increase, and values of Quercus decrease to 3%, and of Fraxinus, Ulmus, Tilia and Taxus e to 1%. Present is pollen of Acer, Hedera, Viscum and Humulus, as well as Buxus. In the Corylus subzone, the contribution of this taxon reaches 26%. In turn in the Picea-Abies subzone increase values of Picea to 4% and Abies to 1.1%. Values of Corylus decrease to 40% and Quercus to 11%, whereas values of Tilia rise to 7%, Alnus to 3% and Taxus to 2.7%. Contribution of Fraxinus and Ulmus is close to values from the previous zone. Pollen of Hedera, Viscum and Cumulus is present. Zone with high contribution of Corylus to 50% and Quercus to 25% and much lower values of Fraxinus (3e5%) and Ulmus (2e3%). Pollen of Tilia cordata type, Taxus, Carpinus and Alnus appears; Ligustrum and Hedera are still present. Zone with domination of AP and high values of Quercus (37%) and Corylus (22%), and much lower contribution of Fraxinus (4%) and Ulmus (2%). Pollen of Ligustrum and Hedera is present. Zone dominated by AP pollen (79%), with Pinus (39%) and Betula (38%). Pollen of Pinus cembra, Salix and Juniperus is present. Among herbaceous plants dominates pollen of Gramineae (11%), Cyperaceae (6%) and Artemisia (2.2%).

The climate record of the beginning of the Eemian Interglacial based on data from profiles from the Radom Plain corresponds with the general trends for central and north-eastern Europe, where the temperature increase of the winter months was more intense than in western and south-western Europe (Kaspar et al., 2005; Brewer et al., 2008). The appearance of such taxa as Viscum and Hedera indicates decreasing climate seasonality noted by Cheddadi et al., 1998 and Klotz et al., 2004 for east-central Europe. Further decrease of seasonality takes place with the increase of average temperatures of the summer months, as evidenced by the appearance of Trapa natans pollen, which corresponds to climate evolution towards oceanic climate for west-central Europe (Cheddadi et al., 1998; Klotz et al., 2004).

Lakes with gyttja and mud accumulation functioned at that time w, Nowy Zamos in Babin, Mirko c, and probably also Policzna and w. On the contrary, peatlands existed at that time in Nowy Floriano  w. In Mako w, the peats directly Zamos c, Czarna Rola and Mako overlie glacial tills of the Saalian Glaciation. The existence of peatlands in these sites was caused by local factors. In Nowy Zamos c, where at that time the lake had a depth of 4e5 m (Fig. 2), beside climate change, disappearance of the water reservoir could have been caused by hydrological conditions and the geological setting. For instance, the presence of a thick sand horizon below the sediments of the Eemian Interglacial could have induced water w, at the boundary beinfiltration from the reservoir. In Łuczyno tween zones E4 and E5, a transition of muds into peats took place

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_ M. Zarski et al. / Quaternary International xxx (2016) 1e14

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Table 5 Czarna Rola description of Local Pollen Assemblage Zones.  ski (2007a,b) L PAZ after Krupin

Depth in m

Description of L PAZ

CR-7 Pinus-NAP

1.87e1.15

CR-6 Picea-Abies

2.25e1.87

CR-5 Carpinus-(Picea-Abies)

2.37e2.25

CR-4 Carpinus-(Corylus)

2.55e2.37

CR-3 Corylus-Carpinus

2.65e2.55

CR-2 Quercus-Pinus

2.85e2.65

CR-1 Pinus-Betula-Quercus

3.00e2.85

High contribution of NAP (up to 44%) in the zone. Values of Pinus (30e58%) and Betula (18%) are higher. Pollen of thermophilous trees disappears. Pollen of Larix and Juniperus appears. Among NAP dominate Gramineae up to 12.7%, Cyperaceae up to 26.5%, and Artemisia up to 4%. Pollen of Caryophyllaceae, Apiaceae, Chenopodiaceae, Ranunculaceae, Asteraceaeand Thalictrum is common. The zone contains high values of Picea (19e31%) and Abies (11%). The decrease of Carpinus takes place; in the lower part of the zoneit reaches values of 14e15%. Pollen of Buxus is still present. The zone shows the decrease of Carpinus to 25%, increase of Abies to 11% and Picea to 14%. Values of Quercus, Corylus, Alnus, Tilia, and other trees decrease. Values of Carpinus reach up to 35%, and Corylus to 24%. Contribution of Tilia, Quercus, Ulmus and Alnus is lower. Pollen of Picea reaches 7.8% and Abies appears. Pollen grains of Acer, Hedera, Viscum and Humulus is noted. Values of Corylus rise to 36%; Carpinus appears with contribution up to 26%, Alnus to 6%, Tiliacordata type to 4% and Taxusbaccata to 0.8%. Values of Quercus (6%) decrease. Quercus reaches significant values up to 30%. Ulmus (2%) and Fraxinus (2e3%) still occur. Values of Pinus and Betula decrease, and contribution of Corylus rises to 12%. Zone with domination of AP, with Pinus up to 40%, Betula up to 33% and Quercus up to 19%. Pollen of Ulmus (1e2%) and Fraxinus (1%) is present. Contribution of Corylus reaches 5%. Values of NAP fall from 11% do 7%, mainly of Gramineae, Cyperaceae and Artemisia. Pollen of Salix and Hippopha€ e is present.

Table 6 Policzna description of Local Pollen Assemblage Zones.  ski (2009) L PAZ after Krupin

Depth in m

Description of L PAZ

PO-4 Carpinus-(Corylus)

3.85e3.1

PO-3 Pinus-Betula-Quercus

4.05e3.85

PO-2 Pinua-Betula

4.55e4.05

PO-1 NAP-Betula-(Artemisia)

5.1e4.55

Zone with high contribution of Carpinus (39e54%), significant contribution of Corylus (14e24%) and Alnus (11e14%). Pollen of Quercus (up to 3%), Ulmus and Fraxinus (up to 2%), Taxus baccata (0.4e1.2%) and Acer also occurs. Present is Hedera, Viscum and Vitis. The Tilia subzone was distinguished in the zone (up to 4%). In the upper part of the zone appears pollen of Picea (1e2%) and Abies. Contribution of Pinus (33%) and Betula (31%) pollen is still significant in the zone, but the contribution of Quercus rises up to 17%, Ulmus e up to 4%, Fraxinus e up to 2.4% and Corylus up to 4.7%. Contribution of NAP is higher (91%), with a domination of Pinus and Betula pollen. The contribution of Pinus after an increase to 52% decrease down to 39%, whereas the contribution of Betula increases up to 44%. The contribution of Ulmus (up to 2.6%) and Quercus (up to 2.4%) also increases. Pollen of Fraxinus and Corylus is also present. Humulus appears. Zone with significant contribution of NAP (28e34%). Among pollen of trees prevails pollen of Betula (28e35%) and Pinus (24e25%). The contribution of Salix is low (0.9e1%). Values of Juniperus are significant (4e6%). The taxonomic composition of NAP is variable, with the prevalence of Gramineae (12e15%), Cyperaceae (7e10%), Artemisia (up to 5%) and Chenopodiaceae (0.8e1.8%). Pollen of Apiaceae, Caryophyllaceae and Ranunculaceae is present.

due to climate warming and decreasing rainfall (Fig. 2). At that time, the lake dried up completely and was transformed into a peatland. In Zone E5, hornbeam (Carpinus) gradually enters the forests in favour of linden and other trees. Riparian forests are characterized by the disappearance of Fraxinus and the introduction of Alnus. Climatic conditions were similar to those from Zone E4, which is evidenced by the presence of Hedera helix and Vitis. However, the sporadic appearance of Ilex aquifolium may evidence increase of mean winter temperatures to 0.5
C (Zagwijn, 1996). A slight decrease of the mean temperatures of summer months may be indicated by the disappearance of Trapa pollen. However, the presence of Tilia platyphyllos type pollen may evidence that the mean temperature of the warmest month was at least 17.5
C (Granoszewski, 2003). In the younger part of Zone E5 a significant change takes place in the forests, in which oak and linden were an insignificant element, in favour of the dominating spruce, and later also fir. The evolution of forest communities is related to the decrease of summer temperatures and increased rainfall. Mild winters are evidenced by the presence of Buxus pollen, a taxon appearing in areas within the 0
C isotherm for the coldest month and the 17
C isotherm for the warmest month (Zagwijn, 1996). Increased rainfall is not only indicated by Buxus pollen (maximum annual rainfall exceeding 1000 mm), but also Picea and Ilex. In the Mid-Eemian, along with appearance of hornbeam in the forest communities, the decrease of the average summer temperatures most probably took place. This is concordant with the trend observed by Cheddadi et al., 1998 andRioul et al., 2001. Such

changes may be also evidenced by the appearance of Abies and Picea pollen, and Ilex and Buxus pollen. The presence of the latter two taxa suggest a short-term increase of the average temperature of the winter months. At that time, a cooling probably occurred in northern Europe, but the course of these changes was more complex, problematic, and difficult to recognize due to the presence of taxa exotic to the contemporary flora (Brewer et al., 2008). Climate changes in the Radom Plain in the mid-Eemian times are reflected not only by temperature changes but also rainfall increase. Increased rainfall could have been responsible for the spread of Abies, followed by Picea, clearly recorded in the sediments from Babin. This is concordant with the general trend of climate evolution in central and northern Europe (Kühl and Litt, 2003). Nevertheless, the reconstruction of climate change during the MidEemian in the Radom Plain remains unconfirmed, similarly as in western and central Europe due to the lack of present day analogues for the contemporary plant communities (Brewer et al., 2008), despite the application of multiproxy analyses (Iversen, 1944; Zagwijn, 1996; Guiot, 1990; Kühl et al., 2002). w, Policzna, and probably In this interval, lakes existed in Mirko w. Decalcified gyttja and muds were accumulated in also in Floriano the lakes. Peaty gyttja, followed by peats accumulated in Babin. This change indicates a gradual, oscillatory shallowing of the reservoir and its transformation into a peatland. Peats were accumulated in w. Sediments from the Nowy Zamos c, Czarna Rola and Mako younger part of the Eemian Interglacial have not been observed in w (Fig. 2). Mako Significant changes in the forest communities took place in Zone

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_ M. Zarski et al. / Quaternary International xxx (2016) 1e14

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Table 7  ski (2007a,b, 2009) and Winter in this paper with Correlation of local pollen assemblage zones L PAZ distinguished in the analyzed sections from the Radom Plain after Krupin regional pollen assemblage zones R PAZ (Mamakowa, 1989). Policzna

w Mako

Czarna Rola

CR-7 Pinus(NAP)

CR-6 PiceaAbies

PO-4 Carpinus(Corylus)

PO-3 PinusBetulaQuercus PO-2 PinusBetula PO-1 NAPBetula(Artemisia)

MA-4 Carpinus- CR-5 (Corylus) Carpinus(Abies-Picea) MA-3 Carpinus- CR-4 Tilia-Corylus Carpinus(Corylus) CR-3 CorylusCarpinus MA-2 Corylus(QuercusTaxus) MA1-Quercus- CR-2 QuercusCorylus-Pinus Pinus CR-1 PinusBetulaQuercus

w Łuczyno

LU-8 PinusBetulaArtemisia LU-7 Pinus

Nowy Zamos c

w Mirko

Babin

Ba 14 NAPArtemisiaBetula Ba 13 PinusNAP Ba 12 BetulaPicea-Pinus Ba 11 PinusPicea Ba 10 PiceaMIR-7 PiceaAbies-(Carpinus- Abies-Carpinus Pinus) MIR-6 Carpinus- Ba 9 Carpinus(Corylus-Alnus) Picea-Abies

E V 2 Betula-Pinus R PAZ

€ rup Bro Interstadial

E V 1 GramineaeArtemisia-Betula nana R PAZ E 7 Pinus R PAZ

Herning Stadial

Ba 8 CarpinusCorylus-Tilia Ba 7 CorylusQuercus-Tilia

E 4 Corylus-Quercus-Tilia R PAZ

LU-2 Quercus

MIR-3 Corylus Quercus MIR-2 BetulaPinus-(Ulmus)

Ba 6 QuercusUlmus-Fraxinus Ba 5 PinusQuercus-Ulmus

E 3 Quercus-FraxinusUlmus R PAZ E 2 Pinus-Betula-Ulmus R PAZ

MIR-1 Betula(Pinus-NAP)

Betula Ba 4 PinusBetula Ba 3 BetulaArtemisia Ba 2 NAPBetula-Salix Ba 1 Pinus-NAPCyperaceae

E 1 Pinus-Betula R PAZ

ZA-1 PinusArtemisiaJuniperus

E6. The pollen assemblages evidence progressive transformation of the broad-leaved, mesophilous deciduous forests with hornbeam, oak, linden and hazel, into mixed forests with hornbeam, spruce and fir, and later only with spruce and fir. Near Babin, fir with values reaching 27.5% became a very important forest component, whereas spruce began to dominate at the end of Zone E6, which is evidenced by its contributions up to 68%. In other successions, the maximal values are lower and reach  ski, 2007b), and 16.9% for fir 38.4%for spruce (Czarna Rola, Krupin (Czarna Rola). Most probably, low-resolution analysis of the remaining successions from the Radom Plain does not allow to determine the actual distribution of these trees in the forests of Zone E5. Such domination of these trees in the Babin pollen record may be related to the close vicinity of the Holy Cross Mountains. The

EEM Interglacial

E 5 Carpinus-CorylusAlnus R PAZ

MIR-5 CorylusTilia-Carpinus MIR-4 Corylus Quercus

LU-1 PinusBetula

Early glaciation (Weichselian)

E 6 Picea-Abies-Alnus R PAZ

LU-4 Corylus- ZA-6 CorylusTilia-Carpinus Tilia-Carpinus LU-3 Corylus ZA-5 Corylus(Quercus) ZA-4 Quercus(Corylus) ZA-3 Pinus(UlmusQuercus) ZA-2 Betula(Pinus-NAP)

Stratigraphy after Behre (1989)

V 3 Gramineae-Artemisia- Rederstall Betula nana R PAZ Stadial

MIR-15 NAPArtemisia(Pinus) MIR-14 EquisetumPinus-Salix MIR-13 PinusNAP-(Betula) MIR-12 Pinus(Betula) MIR-11 BetulaPinus MIR-10 Pinus(Betula-NAP) ZA-11 NAPMIR-9 NAPArtemisia-Pinus (PinusArtemisia) ZA-10 PinusMIR-8 Pinus(Betula-NAP) (NAP)

ZA-9 Pinus(Picea) ZA-8 PiceaLU-6 PiceaAbiesAbies(Carpinus) (Carpinus) LU-5 Carpinus ZA-7 Carpinus

R PAZ after Mamakowa (1989)

LP MGP eCyperaceaeArtemisia-Betula nana R PAZ

Late Saalian

mountain slopes were probably overgrown by spruce-fir forests similar to modern lower mountain forests and the pollen of both taxa probably derived from these sites. It is also possible that the area of the Radom Plain was under the influence of mountainous climate. Vegetation of Zone E6 indicates increase of rainfall, lower summer temperatures, but warm winters. The presence of Buxus pollen may still indicate mean temperatures of the coldest month up to 0
C, and the strong influence of oceanic climate was regionally enhanced by the influence of mountainous climate. A cooling occurred in the later part of the zone, at a simultaneous high humidity of the climate. During Zone E6, all described reservoirs became peatlands (Fig. 2). Transformation of a lake into a peatland took place in this  w. This was caused by decrease interval in the deepest lake in Mirko

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Fig. 4. Pollen diagram for the Babin section.

w after Krupin  ski (2007a). Fig. 5. Simplified pollen diagram for Łuczyno

of the water level in the lake. The change may suggest the influence of climate factors related to warm summers of Zone E5, but also a change in local hydrological conditions. A slightly different case took place in this interval in northern Podlasie (eastern Poland), where Eemian lakes do not record sediments from the middle of Zone E5 to the end of Zone E6, which is explained by water level

decrease and indirectly also lower rainfall (Kupryjanowicz, 2007, 2008). Increase in the values of Pinus up to 81.6% and decrease in the contribution of Picea and Abies have been observed in Zone E7. Changes in the pollen record of this zone should be linked with the expansion of pine, which superseded Picea and Abies from the

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 ski (2007a). Fig. 6. Simplified pollen diagram for Nowy Zamosc after Krupin

forests, and developed pine forests. Changes in the forest communities reflect cooling and increase of climate continentalization. A drastic change in the forest communities reflected in the increase of Betula contribution up to 72% and NAP pollen up to 12% in Zone E7 is characteristic of the Babin pollen record. This event points to significant cooling and climate aridization. Similar changes were registered in many successions from Poland (Kupryjanowicz et al., 2016, in press, Winter et al., 2016; in this volume). A minor short-term warming is indicated by the return of pine forests at the end of Zone E7, but the spread of open communities with a significant contribution of Artemisia may evidence progressing cooling and climate continentalization. w at the end of the Eemian A peatland was present in Mirko Interglacial (Zone E7). Sedimentary change took place with proceeding cooling. At first, peats were accumulated in Nowy Zamos c w, and later replaced by muds. Gyttja with peat inand Łuczyno terbeds accumulated in Babin, and silty sands with humus e in Czarna Rola. Most probably, changes of hydrological conditions due to rainfall increase lead to the transformation of peatlands into lakes. Zones EV13 represent vegetation changes related to the beginning of the glaciation. Expansion of various open, steppe-like communities with Artemisia and Chenopodiaceae, and tundra-like communities with Cyperaceae and Poaceae takes place in Zone EV1. The beginning of the Weichselian Glaciation is marked by a strong cooling and climate continentalization reflected in its aridization. The return of loose forest communities with pine and birch w site indicates in Zone EV2 distinguished only in the Mirko improvement of climate conditions, which again underwent significant deterioration in Zone EV3. At that time, pine retreated and

birch restricted its occurrence in favour of variable open commu ski, 2009). nities (Krupin The general shift of climate change in the Radom Plain during the termination of the Eemian Interglacial as recorded by pollen data is concordant with that observed in central and northern Europe (Cheddadi et al., 1998; Klotz et al., 2004; Kühl and Litt, 2003), but also with oxygen isotope estimations (Rioul et al., 2001, Mirosław-Grabowska, 2009). These changes are reflected in a significant decrease of summer and winter temperatures, the proceeding climate aridization and rising seasonality (Brewer et al., 2008). Analysis of the rate of dynamics of climate changes during the Eemian/Weichselian transition in the Radom Plain has allowed to conclude that these changes took place much slower than during the Saalian/Eemian transition, similarly as in entire Europe (Brewer et al., 2008). In the Early Weichselian (Zone EV1), in very cool climate conw and Nowy Zamos ditions, lakes existed in Babin, Łuczyno c. Muds generally accumulated there. Later, the lake reservoirs ceased to  w, in which peats were accuexist. The only exception was Mirko mulated from the Early Weichselian (Herning Stadial), (Behre, €rup (EV2), till the Redestall Stadial 1989) through the Bro  ski, 2009). Transformation of peatlands into lakes in the (Krupin Early Weichselian is a common phenomenon observed in Polish successions (Klatkowa, 1997; Kupryjanowicz, 2007, 2008; Błaszkiewicz, 2008). Climate cooling and thus lower evaporation caused water level increase in continental climate conditions. Supply of humus to the lakes was restricted due to the disappearw ance of forest communities. However, a peatland existed in Mirko in the entire Early Weichselian. This was caused probably by local conditions, including intense growth of peat-forming vegetation

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 ski (2007b). Fig. 7. Simplified pollen diagram for Czarna Rola after Krupin

such as Sphagnum. The reason for the disappearance of lakes in the Weichselian was probably lower humidity, and also activation of denudation processes. In the plateau sites, depressions were filled with diluvial sands, and in the valley sites e by fluvial and diluvial sands. In w, the depression that existed till the Redestall Stadial was Mirko buried by fluvial sands. In Babin, the lake was buried by fluvialdiluvial sands in the early Weichselian and eolian sands at the end of the Weichselian. The situation changed in the Holocene. In the plateau sites, compaction of Eemian biogenic sediments resulted in the deflection of the ground surface by several metres and formation of Holocene reservoirs, reflecting exactly the outlines of Eemian lakes (Klatkowa, 1997; Kupryjanowicz, 2008). Rise of water level also took place due to increased rainfall. The Holocene reservoirs are periodical swampy areas, in which peats and diluvial sands are accumulated. A similar case took place in the valley sites. Localities of Eemian lakes are at present marked by widened valleys. The depressions have been included in modern river systems.

3.

4.

5.

6. Conclusions 1. Eemian lakes in the Radom Plain were formed as a result of the melting of dead-ice blocks from the end of the Saalian Glaciation to the beginning of the Eemian Interglacial. The reservoirs were characterized by small sizes and depths between 3 and 12 m. 2. Analysis of the variability of sediments infilling the palaeolakes and climate changes indicates that climate conditions were not the only factor significantly influencing sedimentation change. In the early and middle Eemian (climate optimum) lakes func w, Łuczyno w), tioned in the deeper basins (Babin, Mirko whereas peatlands developed in shallower lakes, with the

6.

exception of the relatively deep basin in Nowy Zamos c, which was a peatland throughout almost the entire Eemian. In the later part of the Eemian Interglacial (post-optimum interval) most lakes developed into peatlands, and in the Early Weichselian e  w site, which again into lakes, with the exception of the Mirko remained a peatland. Most Eemian basins ceased to function in the Early Weichselian. Their rejuvenation took place in the Holocene due to deflection of the ground surface caused by compaction of biogenic sediments, and due to water level rise. Despite the fact that the quality of pollen studies in the profiles is variable in the investigated area, it allows for the reconstruction of large-scale climatic changes during the Eemian Interglacial distinguished in Europe, at the same time corresponding to the general trends of temperature changes during the summer and winter months and climate seasonality. The pollen sequences from the Radom Plain indicate a similar vegetation development and climate changes in Poland and in Central Europe. However, the Eemian sequence in Babin registers significant, abrupt vegetation changes, which should be linked with the variability of local conditions. In relation to the evolution of vegetation communities in the Eemian Interglacial, it has to be concluded that the contribution of Corylus was rather low, whereas Tilia was a significant component of the forests in Zone E5. In Zone E6, the variability of forest communities is evidenced by much higher values of Picea and Abies pollen in comparison to other parts of Poland. Such pollen assemblages indicate the domination of these trees in forest communities and very high annual rainfall. Two cool climate oscillations were distinguished in the Eemian Interglacial, at the beginning and the end of the sequence, which could have a transregional record.

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Acknowledgments This research was supported by Polish Geological Institute, during the preparation of the Detailed Geological Maps of Poland in  ski for palinoscale 1: 50 000. We are grateful to Krzysztof Krupin  and Pionki logical elaborations of the Eemian profiles at Zwolen sheets of Geological Map. We are specially grateful to Mirosława Kupryjanowicz for including our paper to QI volumen of the Eemian in Poland. The Authors would like to thank an anonymous Reviewers and Min-Te Chen Editor-in-Chief Quaternary International for helpful comments.

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_ Please cite this article in press as: Zarski, M., et al., Palaeoenvironmental and climate changes recorded in the lacustrine sediments of the Eemian Interglacial (MIS 5e) in the Radom Plain (Central Poland), Quaternary International (2016), http://dx.doi.org/10.1016/j.quaint.2016.12.001