The last million years recorded at the Stari Slankamen (Northern Serbia) loess-palaeosol sequence: revised chronostratigraphy and long-term environmental trends

Quaternary Science Reviews 30 (2011) 1142e1154

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The last million years recorded at the Stari Slankamen (Northern Serbia) loess-palaeosol sequence: revised chronostratigraphy and long-term environmental trends Slobodan B. Markovi
c a, *, Ulrich Hambach b, Thomas Stevens c, George J. Kukla d, Friedrich Heller e, William D. McCoy f, Eric A. Oches g, Björn Buggle h, Ludwig Zöller b Chair of Physical Geography, Faculty of Sciences, University of Novi Sad, Trg D. Obradovi
ca 3, 21000 Novi Sad, Serbia Chair of Geomorphology, University of Bayreuth, D-95440 Bayreuth, Germany Centre for Quaternary Research, Department of Geography, Royal Holloway, University of London, Egham, Surrey TW20 0EX, UK d Lamont-Doherty Earth Observatory of Columbia University, Rt. 9W, Palisades, NY 10964, USA e Institut für Geophysik, Department of Earth Sciences, CH-8093 Zürich, Switzerland f Department of Geosciences, University of Massachusetts, Amherst, MA 01003, USA g Department of Natural and Applied Sciences, Bentley University, Waltham, MA, USA h Chair of Soil Physics, University of Bayreuth, D-95440 Bayreuth, Germany a

b c

a r t i c l e i n f o

a b s t r a c t

Article history: Received 16 September 2010 Received in revised form 2 February 2011 Accepted 9 February 2011 Available online 9 March 2011

The Stari Slankamen loess-palaeosol section is located on the northeastern part of the Srem Loess Plateau (Vojvodina region, North Serbia). The c. 40-m thick cliff comprises loess intercalated with 9 major palaeo pedocomplexes and can be considered to be one of the most important Quaternary sections in the Carpathian (Panonnian) basin. Here we present new magnetostratigraphic and aminostratigraphic evidence that demonstrates the importance of the site in terms of its age and the long-term palaeoclimatic record it preserves. Directional palaeomagnetic data, obtained through alternating field demagnetization demonstrates the presence of reversed polarity below a profile depth of 36 m indicating a Matuyama chron age of this interval. This interpretation is confirmed by new high resolution palaeomagnetic investigations (434 oriented samples) from the lower part of the profile. The new magnetic susceptibility record and aminostratigraphy indicate a missing pedocomplex (V-S2), with an erosional unconformity represented by a distinct gravel layer. The combined new magnetostratigraphic and aminostratigraphic based age model requires a significant revision of hitherto published chronostratigraphic subdivisions at the site. The relative completeness and long time frame covered by the section is unusual in European loess sequences. Hence, the sequence could form the basis of a continental scale stratigraphic scheme that would alleviate much current chronostratigraphic uncertainty and enable more broad-scale climatic reconstructions. The section also provides a rare opportunity to investigate detailed and long-term climatic change over the Middle Pleistocene in a region influenced by air masses originating from high and middle latitudes, as well as the North Atlantic and Mediterranean. The changing relative importance of these air masses through time provides insight into local and regional atmospheric systems and their evolution through the last c.1 Ma. The section can thus be considered as one of the key climatic archives in the Europe. Ó 2011 Elsevier Ltd. All rights reserved.

Keywords: Loess Magnetism Palaeoclimate Palaeosol Aminostratigraphy Pleistocene Matuyama-Brunhes Serbia Stari Slankamen

1. Introduction Loess deposits are considered to be some of the most detailed and long-term records of late Caenozoic climate change (Porter, 2001).

* Corresponding author. Tel.: þ381 21 485 2837; fax: þ381 21 459 696. E-mail address: [email protected] (S.B. Markovi
c). 0277-3791/$ e see front matter Ó 2011 Elsevier Ltd. All rights reserved. doi:10.1016/j.quascirev.2011.02.004

Modern loess research effectively began with the pioneering  palaeomagnetic investigation of the Red Hill (Cerveny Kopec) loess exposure near to Brno in the Czech Republic (Bucha et al., 1969). While the Upper Pleistocene and part of the Middle Pleistocene have now been removed after raw material exploitation, the section originally contained about 1 Ma of loess sediments and provided the chronostratigraphic framework for Kukla’s (1970, 1975, 1977) correlations of palaeoclimatic fluctuations recorded in terrestrial

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deposits, with oscillations recorded in deep-sea sediments. However, although these initial magnetostratigraphic investigations were made in the Danubian loess sequences (e.g. Fink and Kukla, 1977), with the work of Heller and Liu (1982, 1984, 1986) the focus subsequently shifted to China where aeolian deposits potentially extend to the base of the Miocene (Guo et al., 2002). Initial investigations in China focused on palaeomagnetic zonation of the c. 2.5 Ma Luochuan loess sequence, and on the record of magnetic susceptibility (MS) variations as one of the most sensitive loess proxies for palaeoclimatic change. Many MS studies of Chinese, Central Asian, European, New Zealand and North and South American loess deposits followed and made significant advances in the reconstruction of terrestrial Pleistocene environmental processes (e.g. Heller and Evans, 1995; Evans and Heller, 2001). However, a persistent problem in loess research is the apparent absence of a significant pre-Late Pleistocene record from many of the loess belt areas, notably in Europe. The lack of such loess has previously been explained as a consequence of recycling of previously deposited material during subsequent glacial periods (van Loon, 2006), but in any case has severely limited understanding of Early and Middle Pleistocene climate in continental regions. The loess sequence at Stari Slankamen in northern Serbia comprises multiple couplets of loess and palaeosol units in 40 m of sediments. This strongly suggests a considerably longer record is preserved at the site than that in the majority of loess deposits (Singhvi et al., 1989). Despite this obvious significance, detailed chronostratigraphic and palaeoclimatic investigations of the Stari Slankamen loess exposure have so far been limited (Bronger, 1976, 2003; Singhvi et al., 1989). A significant difficulty in analysing Middle Pleistocene palaeoclimate records obtained from loess deposits lies in the construction of an accurate age model. Few independent dating techniques that cover this age range can be applied to loess. As such, many studies have correlated sequences over long distances using soil stratigraphy (Kukla, 1975; Bronger, 2003). However, regional pedofacies changes and the possibility of missing or truncated soil or loess units limit such age models. Magnetostratigraphic characterization is more objective and can determine the broad chronostratigraphy of a sequence, if long enough, but will not be suitable for differentiating between glacialeinterglacial cycle units of the Middle Pleistocene, if only magnetic polarity stratigraphy is applied. However, amino acid geochronology has been successfully applied to Middle Pleistocene loess deposits throughout Europe and China and enables stratigraphic subdivision of glacialeinterglacial units (Oches and McCoy, 2001). In particular, the ratio of diastereoisomers D-alloisoleucine and L-isoleucine extracted from shells of fossil gastropods (notably Helicopsis, Pupilla, Trichia and Vallonia sp.) have the potential to provide relative chronologies for loess-palaeosol sequences of the Middle Pleistocene and have previously been successfully applied to Serbian loess (Markovi
c et al., 2004). A combination of these dating techniques has the potential to allow development of a detailed and long-term age model over multimillennial timescales at Stari Slankamen. Stari Slankamen is significant not only because of the age range covered by the loess, but also because it is influenced by air masses originating in both high and middle latitudes, as well as the North Atlantic and Mediterranean. The near-continental nature of the climate at the site means that even small changes in precipitation associated with the changing influence of these air masses should register significant changes in the climate proxies (Duci
c and Radovanovi
c, 2005). Such information is certainly of regional significance, but likely originates from wider scale shifts in atmospheric and oceanographic systems. Thus the record at Stari Slankamen has the potential to provide rare and significant insight into local- and broad-scale atmospheric-oceanographic changes and provide insight into the long-term evolution of Middle and Late Pleistocene climate in Europe.

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Here, we apply magnetostratigraphic and amino acid racemization (AAR) dating, together with litho- pedostratigraphic analyses to the Stari Slankamen exposure in order to ascertain the a) age and b) potential palaeoclimatic significance of the site. The magnetostratigraphy includes magnetic polarity as well as magnetic susceptibility stratigraphy (Opdyke and Channell, 1996; Hambach et al., 2008). The data presented in this study confirm and emphasize the antiquity of the sediments preserved in the section and demonstrate the significance of the detailed and relatively complete palaeoclimatic record they contain. 2. Sampling and methods The exposure at Stari Slankamen is located in the southeastern part of the Carpathian Basin (Fig. 1) in the northeastern part of Srem Loess Plateau, on the western bank of the Danube River, opposite the Tisa confluence (45 070 5800 N; 20180 4400 E) (Fig. 2). Fifty nine oriented samples spanning a thickness of 40 m were taken for palaeomagnetic analysis. The analyses were performed at the palaeomagnetic Laboratory of the Institute of Geophysics at the ETH Zürich, Switzerland. Directional palaeomagnetic data, were obtained after alternating field (AF) demagnetization between 5 and 15 mT using a 2G cryogenic magnetometer with in line two axis AF demagnetizer (Evans and Heller, 2001, 2003). In situ and laboratory measurements of low field initial magnetic susceptibility (MS) were conducted at 10 cm intervals in palaeosol horizons and at 15 cm intervals in loess layers. MS variation in the lower part of the profile, below the loess layer V-L5, was measured in situ using a portable Bartington MS2 susceptibility metre. At each level, 10 repeat readings were taken and averaged. Samples from the upper part of the exposure were measured on a Bartington susceptibility MS2B metre with a 36 mm opening at the Lamont-Doherty Geophysical laboratory in Palisades, New York. Selected samples from the lower part of the profile were re-measured, which made it possible to crosscalibrate MS values obtained by different instruments. In 2005, high resolution magnetostratigraphic sampling was undertaken in the lower part of the profile. 434 samples were collected from two parallel columns in steps of 5 cm. Oriented specimens were taken using brass tubes and an orientation holder. Samples are cubes with an edge length of 2 cm, giving a volume of 8 cm3. Full spatial orientation was provided by magnetic compass measurements. Measurements of palaeo- and rock-magnetic parameters were performed in the Laboratory for Palaeo- and Environmental Magnetism (PUM), University of Bayreuth. All specimens were subjected to standard rock and palaeomagnetic laboratory procedures to reveal their rock-magnetic characteristics and to decipher the directional trends of the Earth’s past magnetic field stored in the sediment (Hambach et al., 2008). The initial low field magnetic susceptibility was measured in an AC-field of 300 A/m at 875 Hz using the AGICO KLY-3-Spinner-Kappa-Bridge (AGICO, Brno, Czech Republic) and is given as mass specific susceptibility (c). Stepped demagnetisation and remanence measurements were conducted employing an AGICO JR-6A spinner magnetometer and a Magnon AFD 300 (MAGNON, Dassel, Germany) demagnetiser. Full details of the palaeomagnetic analyses require a dedicated paper and will be presented in a future submission. Here, an outline of the key results obtained is presented, sufficient to draw the chronostratigraphical conclusions relevant to the multi-millennial timescales addressed in this paper. Six bulk sediment samples were collected in 2002 from each loess unit at Stari Slankamen (except V-L5), from which mollusc shells were extracted after wet-sieving for measurement of amino acid racemization. Gastropod shells of Pupilla, Helicopsis, Succinea, and Trichia genera were recovered in sufficient number for robust analysis. The ratio of D to L isomers of various amino acids in

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 Fig. 1. Topographic map showing the locations of the main Middle Pleistocene loess sites in the Danube Basin: Stari Slankamen, Mosorin, Batajnica, Ruma, Cerveny Kopec, Krems, Stranzendorf, Paks, Ljubenovo, Viatovo, Koriten, Mostis¸tea, Mircea Voda, and Costines¸ti.

gastropod shells can be obtained and correlated with values obtained from other loess-palaeosol units elsewhere in Europe in order to independently assess chronostratigraphic interpretations of loess profiles (Oches and McCoy, 2001). Rates of racemization differ between genera, as well as among several amino acids and hence must be interpreted separately. The amount of the increase in D/L ratio from loess of one glacial cycle to the next decreases with increasing age as the extent of racemization asymptotically approaches an equilibrium value of 1.0 (w1.3 for AI). Thus the resolution of the method decreases with age and the method generally cannot reliably discriminate glacial cycles older than about 700,000 years in the midlatitudes. Samples were prepared and analysed using the reverse-phase liquid chromatography method following the procedure of Kaufman and Manley (1998).

3. Results 3.1. Section description Earlier descriptions of the Stari Slankamen exposure were made by Markovi
c-Marjanovi
c (1972); Butrym (1974); Bronger (1976); Butrym et al. (1991); Markovi
c et al. (2003); and Schmidt et al. (2010). Some differences in these descriptions result from analysis of two neighbouring exposures: a longer loess-palaeosol sequence on the bank of the Danube (marked as A on Fig. 2) and a sequence of apparently younger loess (Gorijanovi
c-Kramberger, 1921) 1.1 km from the main section (B on Fig. 2). A further complicating factor is an erosion layer (labelled EL in Fig. 3) marked by gravel-sized rock

fragments and located in the loess below palaeosol V-S1 (for stratigraphic nomenclature see Fig. 3). Both the gravel layer and the overlying loess deposits, display horizontal bedding, although below, the loess-palaeosol strata dip 10 to the south. Further complications arise because the lower part of the main section from the middle part of the loess layer V-L9 to the base is currently obscured by slump material. During the field work in 2005, a trench was dug in this section, enabling detailed morphological description and collection of new high resolution samples for palaeoand rock-magnetic analyses. The relationship between this dataset and an earlier one published in Markovi
c et al. (2003) is presented in Fig. 4. During the trench description, a more complicated structure of the loess-paleosol units below V-S8 than was presented in Markovi
c et al. (2003) was observed, identifying, relative to the neighbouring pedocomplexes, a weakly developed palaeosol V-S9 and the underlying loess unit V-L10. Below V-L10 lies a complex of multiple but indistinguishable soils. In this study, the section (A) facing the Danube is the main focus. The descriptions of the Stari Slankamen loesspalaeosol sequences are presented in Fig. 3 and Table 1.

3.2. Trends in directional palaeomagnetic data One of the key control points in the chronostratigraphical subdivision of the Stari Slankamen sequence is the MatuyamaBrunhes palaeomagnetic boundary (MBB; 0.78 Ma according to Cande and Kent, 1995). The directional palaeomagnetic data obtained after AF demagnetization from the main section demonstrate the presence of reversed polarity below a profile depth of

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of the natural remanent magnetisation (NRM) vectors are shown as function of stratigraphy and AF-amplitude. The progressive change of the NRM-inclinations with the field amplitude during AFdemagnetisation reveals normally overprinted reversed remanences in the lower half of the profile. As discussed above, the lowermost metre and the upper 6 m are clearly of normal polarity. The preliminary results demonstrate that AF-demagnetisation in fields up to 40 mT is not enough to separate normal and reversed overprints from primarily reversed or normal remanences respectively. 3.3. Magnetic susceptibility record

Fig. 2. Location of the Stari Slankamen loess sites: main section (A) and section in loess gully between Novi Slankamen and Stari Slankamen. Embedded legend in Fig. 1. Bars for protection of the fluvial erosion; 2. Settlement; 3. Contours (m); 4. Contourpoints; 5. Roads.

36 m indicating a Matuyama chron age of the lower part of the lowest loess layer V-L9 (Fig. 4). A transitional magnetic polarity interval is visible just below the polarity change although this is likely to be a result of the interplay between chemical and detrital remanent magnetization and lock-in depth (e.g. Spassov et al., 2003; Liu et al., 2008). The observation of the MBB at Stari Slankamen is the first in the loess-palaeosol sequences of Serbia. The new palaeomagnetic results from the lower part of the section, from palaeosol V-S6 to the profile base, also reveal a transition from normal, through mixed and fully reversed polarity (Fig. 5). These preliminary data are based on remanence measurements after AF-treatment in fields up to 40 mT. Exclusively normal polarity of the Brunhes Chron was found at palaeosols V-S6, V-S7 and V-S8, as well as in loess units V-L7 and V-L8. A complex pattern of mixed polarity starts in the upper part of loess unit V-L9 from about 5 m downward, with the transition to fully reversed polarity of the Matuyama Chron in V-L10, just below V-S9. The shift to clear reversed polarity starts in the middle of fossil soil V-S9 (Hambach et al., 2009), at a similar profile depth to that indicated by initial measurements (Markovi
c et al., 2003). A 2 m thick interval from the centre of V-S9 to the top of the basal pedocomplex shows almost fully reversed polarity. The lowermost 1 m of the section, within the basal pedocomplex, exhibits an interval of normal polarity, potentially indicating the Jaramillo Subchron (Hambach et al., 2009) (Fig. 5). The results from detailed stepwise alternating field (AF) demagnetisation experiments are shown in Fig. 5. The inclinations

The low field initial MS variations in the Stari Slankamen loesspalaeosol sequence are hypothesised to reflect Middle and Late Pleistocene palaeoclimatic fluctuations at the site, in particular, changes in humidity (Markovi
c et al., 2009). The coincident increase in MS with the occurrence of soils (Fig. 4) strongly suggests a similar mechanism to that found in loess on the Chinese Loess Plateau (Heller and Liu, 1984). Although there is a general decrease in MS values up section, the finer-scale variations clearly reflect the pedostratigraphy of the Stari Slankamen section (Fig. 4). MS values measured in palaeosols (mean value 68.5  108 m3 kg1) are on the average more than twice as high as those in the loess units (mean value 31.7  108 m3 kg1). The lowest value was measured in the loess unit below palaeosol V-S1 (10.3  108 m3 kg1) whereas the highest value is in palaeosol V-S8 (165.7  108 m3 kg1). Similar results were obtained from the re-sampled lower part of the section (Hambach et al., 2009). Comparisons between MS variations in palaeosols V-S6, V-L7S1, V-S7, V-S8, and the basal pedocomplex provide good agreement between old and new results (Fig. 4). Many MS variations within loess units V-L7 and V-L9 are caused by strongly bioturbated loess and humic infiltrations in pre-existing strongly developed root channels, and therefore cannot be ascribed to changes in humidity. The only significant difference between old and new measurements is related to palaeosol V-S9, which was not observed before the trench was dug in 2005 (Fig. 4). The cyclicity of alternating high and low MS values between palaeosols and loess units reflects magnetic susceptibility enhancement due to different degrees of paedogenesis between glacial and interglacial periods (Markovi
c et al., 2008, 2009; Buggle et al., 2009; Antoine et al., 2009), similar to that observed in Chinese and Central Asian loess deposits (Heller and Liu, 1984, 1986; Maher and Thomson, 1999). Importantly, one of the key features of the record is the decrease in interglacial MS values through time from the basal complex to V-S1 (Fig. 4). 3.4. Aminostratigraphy Amino acid data from shells recovered from loess at Stari Slankamen show a general increase in D/L ratio with stratigraphic age (Table 2). Here we report D/L ratios for glutamic acid (Glu) and valine (Val), and the ratio of alloisoleucine to isoleucine (AI) for the genera Helicopsis, Pupilla, and Succinea (Tables 2 and 3). Most of the data show a clear discrimination of the upper five sampled loess units at Stari Slankamen. However the variability in the ratios also generally increases and the resolution diminishes with depth (Table 2), with V-L9 not clearly distinct from V-L7 in the Pupilla data. In addition, the single Helicopsis shell from V-L9 has anomalous D/L values. It may be contaminated or intruded into V-L9 from above, perhaps by animal burrows or along root channels. The youngest loess was not accessible at site A at the time of our field sampling and our sample from V-L1 was taken from site B (Fig. 2). At that site the upper loess has been eroded considerably and the Holocene and V-L1S1 soils are missing. Despite this the data appear capable of distinguishing

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Fig. 3. Comparison of the Stari Slankamen loess-palaeosol sequence descriptions of 1. Markovi
c-Marjanovi
c (1972); 2. Butrym (1974); 3. Lithology according to Bronger (1976) with thermoluminescence ages after Singhvi et al. (1989); 4. Butrym et al. (1991); 5. Schmidt et al. (2010); Interpretation presented here, with legend.

between glacialeinterglacial cycles when compared to other regional aminostratigraphic data. 4. Discussion 4.1. Stratigraphic overview There have been a number of stratigraphic models developed for the Stari Slankamen loess, with differing nomenclature and numbers of fossil soils (Fig. 3). In the initial stratigraphic interpretations of the Stari Slankamen sequence presented by Markovi
cMarjanovi
c (1970, 1972), seven pedocomplexes were described in the main exposure. Bronger (1976) described a regional (Middle Danube Basin) pedostratigraphic sequence in which each fossil soil was marked with the letter F and numbered in order of increasing age and depth. Later, Butrym et al. (1991) defined another stratigraphic model for the Stari Slankamen loess-palaeosol sequences, marking soils from a1 on the top of profile to the lowest exposed fossil soil at the time of their investigation, n3. Markovi
c et al. (2003) designated the loess-palaeosol unit names in north Serbia following the Chinese loess stratigraphic system (e.g. Liu et al.,1985; Kukla and An, 1989), but inserting the prefix “SL”, referring to the Stari Slankamen site as standard type section. However, to avoid confusion due to potential incompleteness in the youngest part of the Middle

Pleistocene loess-palaeosol sequence preserved at Stari Slankamen, the prefix ‘V’ is now used to refer to the standard Pleistocene loesspalaeosol stratigraphy in Vojvodina (Markovi
c et al., 2008). The scheme therefore allows for information from the penultimate interglacial to be included, based upon other sections (e.g. Ruma and Batajnica; Markovi
c et al., 2006, 2009). Chinese L (loess) and S (soil) stratigraphic nomenclature has also recently been used in stratigraphic studies of Bulgarian (Jordanova and Petersen, 1999; Jordanova et al., 2007, 2008) and Romanian loess (Panaiotu et al., 2001; Buggle et al., 2009; Balescu et al., 2010). Table 4 summarizes the existing chronostratigraphic models of the Stari Slankamen loess-palaeosol sequence, and presents our revised chronostratigraphic model, based on the results presented above. The position of the MBB in the Stari Slankamen main section occurs in the lower part of a relatively thick loess unit V-L9 in our model (MIS 22e24). An interval of reversed to unclear polarity is identified below this, still within the V-L9 unit, as well as in loess layer V-L10 and the upper part of Stari Slankamen basal pedocomplex. Below this, the apparent decrease in the MS of the basal complex coincides with occurrence of a normal polarity interval, probably related to the Jaramillo subchron (Fig. 6). The detailed results from the new palaeomagnetic sampling in 2005 reveal a trend of the directional palaeomagnetic data that we interpret in terms of geomagnetic polarity. Taking into account the

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Fig. 4. Magnetic susceptibility of the Stari Slankamen loess-paleosol exposure. 1) According to Markovi
c et al., (2003) modified (whole section), and 2) new data presented here (the lowermost part only). MS records are normalized (by average value). Pedostratigraphy is the same as shown in Fig. 3 (sequence 5). The grey line denotes the part of the profile uncovered after field work in 2005 and arrows connect peaks from the two profiles.

palaeosol-loess stratigraphy, MS variations with depth and the tentative polarity pattern, we interpret the double soil complexVS7/V-S8 as the equivalent of MIS 19 and 21, corresponding to S7 and S8 in the Chinese loess stratigraphy. Lock-in, strong paedogenesis and root activity transferred the MBB to the V-L9 loess, which corresponds to L9 in China. Consequently, the normally magnetised V-S10 complex at the base of the section is the amalgamated equivalent of S10 and S11 (equivalent to MIS 27 to 31) in China, which spans the Jaramillo subchron (e.g. Sun et al., 2006; Liu et al., 2008). Thus, the lower part of the loess section at Stari Slankamen can be assigned to the late Matuyama and early Brunhes Chrons. Although the directional record is ambiguous in some intervals where strong paedogenesis caused secondary magnetisations, evidence for late Matuyama geomagnetic excursions is present. In the upper half of V-S9 (equivalent to S9 in China; MIS 25) normal polarity seems to be persistent (Fig. 5). This stable normal polarity may represent the incomplete record of the so-called Kamikatsura and Santa Rossa geomagnetic excursions occurring around 0.9 Ma. Furthermore, at the top of V-S6 two samples show a trend to reversed polarity during progressive AF-demagnetisation. This interval may correspond to the so-called Stage 17 excursion, which would give an age of approximately 0.685 Ma (Channell et al., 2009). The MBB at Stari Slankamen is located stratigraphically deeper than in Chinese loess (Zhou and Shackleton, 1999). In China the lock-in of the magnetic signal in loess differs from that in marine cores where the MBB is found in warm period MIS 19, the apparent

true age of the reversal, although probably also slightly offset. The contrasting processes of detrital and chemical remanent magnetisation have been shown to interact in Chinese loess sequences to yield an alternating signature, even when the geomagnetic field may not have varied (Spassov et al., 2003). Such processes may account for some of the complexities seen here, in addition to the effects of paedogenesis and root activity. Thus, although the true reversal took place during deposition of V-S7 (MIS 19), the event was only registered in underlying V-L9 due to complex lock-in processes. The lock-in effect seems to be greater than at Viatovo in Bulgaria, which places the MBB within Viatovo loess unit L7 (equivalent of MIS 20) (Jordanova et al., 2008), similar to that in Chinese loess. However, at Stari Slankamen, strong root channels stemming from palaeosol-complex V- S8 penetrate several metres down into loess V-L9 and probably also influence the magnetic properties of these sediments. Despite this, the lowermost pedocomplex at Stari Slankamen provides a similar palaeomagnetic record to the basal ‘red clay’ complex at Viatovo (Jordanova et al., 2008) with normal polarity at both possibly related to the Jaramillo normal subchron. These interpretations suggest that the basal pedocomplex was deposited and weathered over several glacialeinterglacial cycles and is highly condensed. Our detailed subdivision of the Brunhes Chron is based on the MS and amino acid data. In general, because of the high energies of activation of the reactions, the rates of amino acid racemization within fossil gastropod shells contained in the loess are very much greater during warm interglacials than during cold glacials. Therefore, the extent of racemization of a particular amino acid

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Table 1 Morphological descriptiona of the Stari Slankamen loess-palaeosol sequences. Unit/subunit

Depth (cm)

V-S0 V-L1

0e70 70e760

V-L1L1 V-L1S1 V-L1L2

V-S1 V-L2

1400e1420 1525e1680 1680e1805 1805e1905 1905e2110 2100e2285

V-L6

2285e2680

V-S6 V-L7

V-L7L1

1075e1235 1235e1400

2680e2910 2910e3195

V-L7S1 V-L7L2

2910e3035 3030e3135 3135e3195

V-S7 V-L8

3195e3290 3290e3330

V-S8 V-L9

3330e3435 3435e3645

V-S9 V-L10 Basal complex

3645e3750 3750e3835 3835-4050?

a

70e285 285e545 545e760

760e980 1075e1400

V-L2L1 L2S1 L2L2? Erosional layer V-S3 V-L4 V-S4 V-L5 V-S5

V-L6L1 V-L6S1 V-L6L2

Description Recent soil Ah horizon partly eroded Porous loess with krotovinas Three layers of weak paedogenesis with krotovinas separated with thin porous loess layers Light porous sandy loess Chernozem pedocomplex with several krotovinas Loess with many snails shells and hydromorphic features Weakly developed initial paedogenetic layer with hydromorphic features Loess with intensively developed hydromorphic features Pebbles and cobbles of local lithology up to 10 cm in diameter Phaeozem (Degraded Chernozem) pedocomplex with krotovinas in upper part Thin loess layer with humic infiltrations in former root channels Cambisol pedocomlex with krotovinas in the uppermost part. Loess Cromic Luvisol pedocomplex. A few Krotovinas exist at the contact with loess V-L5. Carbonate concretions in previous root channels are developed in the upper part. A poorly porous Bwt horizon is strongly developed. Loess with large carbonate concretions (>20 cm in diameter) Embryonic palaeosol Thick loess Cambisol pedocomplex Thin loess layer with carbonate concretions and strongly developed humic infiltrations in former root channels with many snail shells. Chromic Cambisol palaeosol, more weakly developed than the V-S7 and V-S8 pedocomplex Loess with carbonate concretions and strongly developed humic infiltrations in former root channels Chromic cambisol Thin loess layer with carbonate concretions (5e15 cm) and humic infiltrations in strongly developed former root channels Chromic cambisol Loess with strong developed carbonate concretions and strongly developed humic and rubified soil material infiltrations in former root channels (up to 2 m into unit). Weakly developed cambisol with hydromorphic features Loess with smaller humic infiltrations in former root channels with hydromorphic features. Cromic Luvisol pedocomplex with many relatively soft carbonate nodules and fossilized tree remains

Descriptions are based on the WRB soil classification (FAO, 2006) and interpretations are modified from Bronger (1976).

measured within fossil shells today generally does not vary much between shells within loess of a single glacial cycle (from a limited geographical region), but does show marked increases in shells from loess of successively older glacial cycles. Combined with existing data from other nearby regions (Fig. 7) and MS records the data can be used as an independent check on the palaeomagnetism results and to provide more detailed stratigraphic subdivisions in the Brunhes Chron. The MS and amino acid variation in the upper part of the profile suggests a correlation of palaeosols V-S1, V-S3, and V-S4 with MIS 5, 9, and 11, respectively. Sample 020701e6 was taken from about 1 m above the resedimented upper part of the last-interglacial soil (V-S1) and is thought to be from the older part of the last glacialcycle loess (V-L1L2). Helicopsis from sample 020701e6 has AI values of 0.18  0.02 (Table 2) which overlaps with values from the L1L2 loess at Petrovaradin (0.16  0.01; unpublished data: FAL944) and at Ruma (0.16  0.01; unpublished data: FAL949 and FAL950). Pupilla from the same sample (Table 2) has AI values very close to those of Pupilla from L1L2 loess at Petrovaradin (0.09  0.01; Markovi
c et al., 2008). Somewhat lower AI ratios (0.06e0.08) are typically recorded from shell samples taken from loess above the L1S1 soil at other sites in Vojvodina (Markovi
c et al., 2008). AI ratios from V-L1 at Stari Slankamen are consistent with the AI ratios from samples taken from L1 loess below the interstadial soils in Vojvodina and as such we correlate the sampled loess at Stari Slankamen with V-L1L2. We have no shell samples from loess at Stari Slankamen that have D/L ratios similar to L2 loess elsewhere in Vojvodina (Table 3; Fig. 7). The difference in D/L ratios between the upper two sampled loess units at Stari Slankamen is remarkable and is much greater than is seen between loess units of the last two glacial cycles

throughout Europe (Fig. 7). These two units are separated by a gravel layer approximately 20 cm thick in the loess below palaeosol V-L2S1, comprising poorly sorted rounded cobble and gravel clasts up to 10e15 cm in diameter. In fact, the D/L ratios in loess from directly below the gravel layer at Stari Slankamen are similar to those found in the L3 loess elsewhere in Vojvodina. Markovi
c et al. (2006) report AI ratios in Helicopsis shells from the lower part of L3 at Ruma as 0.34  0.11. A resampling of the L3 loess there yields more consistent Helicopsis AI ratios of 0.34  0.01 (unpublished data: FAL953). These values compare closely to the 0.36  0.03 AI ratios for Helicopsis from V-L3 at Stari Slankamen (Table 2). Furthermore, the D/L ratios from V-L3 at Stari Slankamen are similar to those that would be expected for loess of glacial cycle D in Vojvodina based on data from other parts of Europe (Fig. 7). For example, the Pupilla AI ratios from V-L3 at Stari Slankamen (0.27  0.03) are slightly higher than, but overlap with, those found in the glacial cycle D loess in Hungary (0.23  0.02) and Slovakia (0.23  0.03) (Oches et al., 2000). The higher values at Vojvodina are expected due the w1  C higher current mean annual temperatures there. We can also compare D/L ratios in Succinea from V-L3 (below the erosion layer) at Stari Slankamen with those from Succinea from the L2 loess at Petrovaradin, located about 40 km eastnortheast of Stari Slankamen (Table 3). The sites are close enough and have a sufficiently similar present-day climate that D/L ratios for loess of equivalent glacial cycles are expected to be the same. However, the D/L ratios in shells in the V-L3 loess at Stari Slankamen are consistently much greater than those from the L2 loess at Petrovaradin, indicating that V-L3 is considerably older and likely to be from the previous glacial cycle. Therefore, given the bulk of the amino acid data, we judge it is likely that the loess found

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Fig. 5. Results from detailed stepwise alternating field (AF) demagnetisation experiments on samples taken in 2005 at the lowermost part of the profile A at Stari Slankamen. The inclinations of the natural remanent magnetisation (NRM) vectors are shown as function of stratigraphy and AF-amplitude. Inclination values are given as positive numbers when the vector is dipping downward. The progressive change of NRM-inclinations with the field amplitude during AF-demagnetisation reveals normally overprinted reversed remanences in the lower half of the profile. The lowermost metre and the upper 6 m have normal polarity. AF-demagnetisation in fields up to 40 mT is not enough to clearly separate normal/reversed overprints from primarily reversed/normal remanences, respectively. Mass specific susceptibility vs. depth is displayed at the right. The thin dashed vertical lines indicate the inclination of the today’s geomagnetic axial dipole field at the site (GAD). The grey horizontal dashed line marks the expected stratigraphic level of the MBB, assuming that V-S7 corresponds to MIS 19.

immediately below the gravel layer at Stari Slankamen is V-L3 and is correlative with loess of glacial cycle D in other parts of Europe. V-S2 and parts of V-L2 and V-L3 were apparently eroded at Stari Slankamen and the apparent unconformity is marked by the gravel overlying V-L3. Incomplete preservation of the loess record in the upper part of the Stari Slankamen loess-palaeosol sequence is also suggested through correlation of the MS record with other data from nearby loess sites in the Danube Basin (Fig. 6). In all comparable sections, the second pedocomplex from the top displays a distinct patter of MS variation with two discrete peaks. However, these features are not shown in the MS record at Stari Slankamen (Fig. 6). This missing unit is coincident with the appearance of the gravel layer.

The next older loess at Stari Slankamen is V-L4 and is generally well differentiated from other losses by the D/L ratios. However, the large variation in D/L ratios in the Helicopsis samples suggests that there may be some mixing of a reworked older shell and perhaps intrusion of a younger shell. The Pupilla data from the same sample shows much less variation and are consistent with Pupilla AI data from glacial cycle E loess in Hungary, given the temperature difference between the two regions. No shells were recovered from the V-L5 loess at Stari Slankamen and there is much less data from other sites with which to compare the amino acid results for samples from V-L6, V-L7 and V-L9. However, the limited results and the MS data support the previous suggestion that the strongly developed palaeosol V-S5 formed

Table 2 Mean D/L amino acid ratios of total acid hydrolosates of samples from Stari Slankamen.a Sample

Unit

Helicopsis D/L

020701e6 020701e2 020701e3 020701e5 020701e4 020701e1

V-L1 V-L3 V-L4 V-L6 V-L7 V-L9

Glu

0.19 0.43 0.46 e 0.51 0.40

 0.02 (4)  0.05 (8)  0.11 (3)  0.06 (2) (1)

Pupilla D/L

Val

0.14 0.32 0.41 e 0.56 0.42

 0.02 (4)  0.04 (8)  0.13 (3)  0.06 (2) (1)

AI 0.18 0.36 0.35 e 0.49 0.39

D/L

 0.02 (4)  0.03 (8)  0.12 (3)  0.06 (2) (1)

Glu

0.39 0.43 0.49 0.57 0.60

    

D/L

0.19 0.05 0.00 0.01 0.02 0.02

(1) (5) (2) (5) (4) (3)

Val

0.28 0.37 0.37 0.47 0.53

    

AI 0.10 0.03 0.01 0.02 0.06 0.03

(1) (5) (2) (5) (4) (3)

0.27 0.35 0.41 0.51 0.52

    

0.10 0.03 0.02 0.01 0.11 0.03

(1) (5) (2) (5) (4) (3)

a Note that sample 020701e6 from unit V-L1 was taken from site B and the other samples were taken from site A (see Fig. 2). D/L mean values are for glutamic acid (Glu) and valine (Val). AI represents the ratio of alloisoleucine to isoleucine. The specified uncertainty is the sample standard deviation. The number of independently prepared and analyzed subsamples is given in parentheses.

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Table 3 Comparison of amino acid D/L ratios in Succinea shells from V-L2 at Petrovaradin with those from V-L3 at Stari Slankamen.a Locality

Sample

Unit

D/ L

Petrovaradin Stari Slankamen

020627e6 020701e2

V-L2 V-L3

0.32  0.04 (4) 0.47  0.02 (7)

a

Glu

D/L

Val

AI

0.22  0.02 (4) 0.37  0.02 (7)

0.24  0.03 (4) 0.43  0.03 (7)

Layout is as in Table 2. The Petrovaradin data is partly from Markovi
c et al. (2005) and includes unpublished lab data for Glu and Val.

during MIS 13e15 (Bronger and Heinkele, 1989; Bronger et al., 1998; Bronger, 2003). Bronger et al. (1998) suggested that this palaeosol (F6 by their nomenclature) formed over a period several times longer than the Holocene. This pedocomplex shows a much greater degree of pedochemical weathering and clay mineral formation than modern soils in this region and appears to be a characteristic feature of the middle part of all Brunhes loesspalaeosol sediments in Eurasia (Bronger, 2003). We further suggest that palaeosol V-S6 probably formed during MIS 17 although between this level and the MBB chronostratigraphic subdivisions are more tentative. In any case, the whole lower part of the Stari Slankamen exposure suggests rather different palaeoenvironmental conditions compared to the upper part of the sequence, possibly due to shallower ground water levels at that time. These differences are typified by of the properties of thin palaeosols V-L7S1, V-S7 and V-S8, probably equivalents of MIS 18.3, 19 and 21 respectively. The disparities between our chronostratigraphic interpretations and previous ones (Table 4) are of the order of multiple glacialeinterglacial cycles. The reasons for these discrepancies probably lie in the previous reliance on correlation to other incomplete sequence where the absolute age of soils may be poorly constrained, and probable age underestimation in previous thermoluminescence dates (Roberts, 2008). Despite recent advances in luminescence dating techniques, including the application of optically stimulated luminescence (OSL) and infrared optically stimulated luminescence (IRSL), the luminescence family of techniques is still generally acknowledged to have a normal upper age limit of between 50 and 100 ka in loess deposits (Wintle and Murray, 2006; Roberts, 2008) and cannot be used for valid geochronologic assignments beyond these limits. However, recent advances using post-IR IRSL may extend this to c. 250 ka (Thiel et al., in press) and recently, Schmidt et al. (2010) obtained postIR IRSL and IRSL dating results from loess units V-L1 and V-L2 that support our chronostratigraphic model. Luminescence data from last glacial loess unit V-L1 yield ages of approximately 25e65 ka. These results are similar to recent IRSL or OSL dating for the last glacial loess at other investigated sites in the Vojvodina region reported in recent papers (Markovi
c et al., 2007, 2008; Fuchs et al., 2008; Bokhorst et al., 2009; Ujvari et al., 2010; Stevens et al., in press). Further, dates from loess unit V-L2 yield minimum ages of between 100 and 193 ka, supporting our suggestion of a penultimate glacial age (Fig. 3).

Thus, the new age-data presented in this study and comparisons with other long Danube sections and recently published OSL/IRSL dating on Serbian loess demonstrate the need for a serious revision of the earlier interpretations of the Stari Slankamen loess-palaeosol sequence. Many previous interpretations appear to have severely underestimated the age of the exposed units, and the number of differing and conflicting stratigraphic models has caused confusion. 4.2. Correlation with other loess sites of the Danube Basin The chronostratigraphic model presented above covers the period of the Middle Pleistocene climatic transition (Ruddiman et al., 1989; Heslop et al., 2002) and has the potential to broaden understanding of this period in continental settings. However, the considerable confusion over both the age and nomenclature of Middle Pleistocene Serbian loess stratigraphy (Table 4) is further compounded by numerous other chronostratigraphic models from neighbouring countries in the Danube Basin that utilize differing nomenclature. A unified stratigraphic scheme for the region would alleviate much of this confusion and would enable direct testing of the equivalence of palaeosols between different parts of the Danube Basin and allow broad-scale climatic interpretations to be made. The proposed age interpretations of the Stari Slankamen sequence, outlined above with reference to other loess-palaeosol sites, allows for the development of a unified stratigraphic scheme for the Danube Basin. As many of the previously studied Middle Pleistocene Danubian loess sequences are either incomplete or no longer accessible (e.g. Red Hill), Stari Slankamen is unique in having near-complete preservation of every loess and palaeosol unit associated with a glacial or interglacial period through the Middle and Lower Pleistocene. The missing palaeosol V-S2 can be accommodated with reference to nearby sites. Further, the relatively arid climate at the site has ensured that only major climatic ameliorations are recorded in the pedostratigraphy, in a manner similar to much of the Chinese Loess Plateau. As such, a relatively simple delineation of glacialeinterglacial cycles can be derived from the stratigraphy, backed up by absolute dating. Many other sites in the Danube Basin experienced a more humid climate and show a complicated stratigraphy towards the middle and base of the Middle Pleistocene, such as Paks in Hungary, or have apparently greatly reduced resolution in the lower Middle Pleistocene, as indicated by pedocomplex S6 at Bulgarian and Romanian sites such

Table 4 Chronostratigraphic models proposed for the Stari Slankamen loess-palaeosol sequence. Bronger (1976) Palaeosol F2 F3 F4 F5 F6 F7 F8 F9 F10 F11

Alpine sudivision Würm palaeosols W ReW

MIS refers to marine Oxygen Isotope Stage.

Singhvi et al. (1989)

Butrym et al. (1991)

Bronger (2003)

MIS 5a 5e

Palaeosol d Not observed g i l n1 n2

Palaeosol F2 F3 F4 F5 F6

MIS 5a 5c 5e 7 9 9

Model presented here MIS 5a 5e 7 9 or 11 13e15

Palaeosol V-S1 Not observed V-S3 V-S4 V-S5 V-S6 V-L7S1 V-S7 V-S8 basal complex

MIS 5 9 11 13e15 17 18.3 19 21 25-?

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Fig. 6. Correlation of magnetic susceptibility (MS) of the Stari Slankamen sequences (Markovi
c et al., 2003) with the marine oxygen isotope record (Lisiecki and Raymo, 2005) and other loess sites in the Danube loess area: Paks (Sartori et al., 1999), Ruma (Markovi
c et al., 2006), Batajnica (Markovi
c et al., 2009), Koriten (Jordanova and Petersen, 1999), Mostis¸tea (Panaiotu et al., 2001). c denotes mass specific low field initial susceptibility (MS). The grey shading denotes the inter-profile correlation of the MS pattern of the MIS 7 pedocomplex across the Danube loess belt. Dotted lines represent correlations between the palaeomagnetic records.

as Ljubenovo, Viatovo, Koriten, and Mircea Voda, limiting interpretations over this interval. The chronostratigraphy outlined in Table 4, based on the stratigraphic position and inferred timing of the MBB, the relative intensity of principal MS peaks,

Fig. 7. Total acid hydrolosate D-alloisoleucine/L-isoleucine aminostratigraphy of upper two samples from Stari Slankamen (V-L1L2, V-L3). As the uppermost Stari Slankamen sample was taken from below V-L1S1, the values are compared to other European localities for the older part of the B glacial cycle (i.e. below V-L1S1/PK1 or equivalent; probably MIS 4), as well as glacial cycles C (MIS 7e6) and D (MIS 9e8) for the terrestrial land snail Pupilla. SS ¼ Stari Slankamen, VJ ¼ other sites in Vojvodina, H ¼ Hungary, A ¼ Austria, SK ¼ Slovakia, UA ¼ Ukraine, D ¼ Germany and CZ ¼ Czech Republic (Oches and McCoy, 1995a, b, c, 2001; Oches et al., 2000; Markovi
c et al., 2008). Data from Hungary are unpublished. The Stari Slankamen and other Vojvodina data have been measured using reverse-phase liquid chromatography (RPLC), rather than cation-exchange HPLC, which was used to obtain the other data. Analysis of standards shows that RPLC A/I ratios are about 4% higher than those obtained using HPLC. This figure has not been adjusted to account for this offset but doing so would result in an imperceptible change. Countries are presented in approximate order of decreasing mean annual temperature.

pedostratigrapic features and amino acid geochronology, is sufficiently complete to support a chronostratigraphic model to be proposed that can be applied as a type for the region. Testing of this model should be conducted using OSL and post-IR IRSL dating on the upper parts of the section, and using this and other chronological tools on other sites in the Danube Basin. Fig. 6 shows the correlation between this Stari Slankamen chronostratigraphy and the main Middle Pleistocene sections of the Danube loess area. A broad-scale correlation with the SPECMAP model (Lisiecki and Raymo, 2005) and palaeomagnetic zonation up to the Jaramillo subchron is also proposed. The zonation correlates well with the record obtained from the northeastern Bulgarian loesspalaeosol sequence at Viatovo (Jordanova et al., 2008). Here the uppermost reversal recorded in loess unit L7 at Viatovo is attributed to the MBB geomagnetic polarity transition. Two normal magnetozones were also found in the underlying “red clay” complex, probably corresponding to the Jaramillo and Olduvai subchronozones of the Matuyama chron. This new chronostratigraphic model can also be tied to the chronostratigraphy of Middle Pleistocene Czech and Aus trian exposures at Cerveny Kopec, Krems and Stranzendorf (Kukla, 1975; Kukla and Cilek, 1996). The similarities between the Stari Slankamen loess-palaeosol chronostratigraphic sequence and sequences in both the upper and lower Danube Basin (Jordanova et al., 2007; Buggle et al., 2009) (Fig. 6) and at the Black Sea coast (Tsatskin et al.,1998; Balescu et al., 2010), as well as the well preserved nature of the record, opens up the possibility for a transcontinental correlation of European, Central Asian (Ding et al., 2002; Dodonov and Baizugina, 1985; Machalett et al., 2008) and Chinese loess records (Liu et al., 1985; Kukla and An, 1989), using a standardised nomenclature and chronostratigraphic model.

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4.3. Broad climatic evolution at Stari Slankamen The strongly rubified interglacial soils (Table 1) exposed in the youngest Early Pleistocene and older-mid Middle Pleistocene (basal pedocomplex, pedocomplexes V-S7 and V-S8) and the strongest developed pedocomplex at the profile (V-S5) are clearly different from the temperate forest soils (V-S6 and V-S4) of the mid-late Middle Pleistocene and the steppe like interglacial soils of the later Middle and Late Pleistocene (V-S3, V-S1) (Fig. 4). These lowermost soils in the sequence display characteristics associated with subtropical soils (Bronger, 1976), in contrast to the temperate forest (V-S6 and V-S4) or steppe environments that appear to have been responsible for the formation of the middle and upper soils. These palaeopedological observations have been confirmed by employing quantitative geochemical weathering proxies and a soil colour rubification index (Buggle et al., 2008, in press) and supports the previous assertion (Bronger, 1976) that interglacial climate over the Pleistocene has become progressively more arid in the region (Fig. 4).Assuming the signal to be reflective of climate, this generalised trend to decreased weathering up-section in interglacial units contrasts with both the general understanding of global trends in Quaternary climate, as expressed in the marine record (Lisiecki and Raymo, 2005) and ice core records (EPICA, 2004), and also regional climate proxies from lacustrine archives in southeastern Europe (Tzedakis et al., 2006). The last of these reconstructions also suggests a smaller range of interglacial climate changes than the succession of interglacials recorded in Serbian loess, ranging from subtropical to steppe. However, the approximate timing of the main change in interglacial environments preserved at Stari Slankamen broadly coincides with the occurrence of warmer and shorter post Mid-Bruhnes Event (MBE) interglacials recorded in EPICA ice core deuterium records (EPICA, 2004). They also correspond to the timing of qualitative vegetation change observed in the Tenaghi Philippon pollen record, such as increasing dominance of drought-tolerant taxa such as Quercus and Carpinus after MIS 16 (Tzedakis et al., 2006). In addition, Vidi
c et al. (2004) have shown similar, albeit slightly less pronounced, decreases in rubification during the Middle to Late Pleistocene at Jiaodao on the Chinese Loess Plateau. If taken as evidence of changing interglacial conditions during the Middle Pleistocene, this 1) highlights the importance of obtaining long-term regional records before conclusions over general climatic trends in specific regions are made from more hemispheric/global archives and 2) suggests that the pattern of long-term climatic development during the Pleistocene is more complicated and regionally variable than is implied by many climatic global archives. Of additional interest is palaeosol V-S4 (Fig. 2; Table 1). This unit correlates with MIS 11, previously hypothesised to be a long interglacial and a potential analogue of Holocene insolation conditions (Berger and Loutre, 2002). However, V-S4 appears to be one of the least developed soils in the profile and is not exceptionally thick, in contrast to what would be expected from the marine record. Further investigation of this soil promises to provide evidence concerning the climatic regime in eastern Central Europe over this interval. A further interesting aspect is the apparent length of time covered by pedocomplex V-S5 and the basal pedocomplex. These strongly developed pedocomplexes may represent extremely slow dust accumulation during prolonged interglaciations from MIS 13 to MIS 15 and over the late Early Pleistocene, probably MIS 27 to MIS 31 at least. Indeed, MIS 13e15 is expressed as a series of relatively cool periods in marine oxygen isotope (Lisiecki and Raymo, 2005) and Antarctica deuterium records (EPICA, 2004) and the well-developed Chinese loess pedocomplex S5 has also been correlated with this time interval (Rutter et al., 1990). However, enhanced humidity over a shorter timescale may

have a similar effect and it is also been suggested that the strongly developed pedocomplex S5 in Chinese loess may indicate relatively strong summer monsoon conditions in East Asia (Yin and Guo, 2008; Yin et al., 2008; Guo et al., 2009). However, explanation in Serbia is likely to be a prolonged period of low accumulation over MIS 13 to 15, where the probable reduced presence of ice sheets and cold climate conditions for long periods lowered the production of dust that would form loess, reducing accumulation and prolonging exposure to the weathering front. The multi-stage pedocomplex at the base of section may also represent prolonged but extremely slow dust accumulation during the Early Pleistocene, pushing back the age of the onset of loess deposition in the region by hundreds of thousands of years. According to Lisiecki and Raymo (2005), the benthic d18O pattern during the period coincident with the formation of the strongly developed pedocomplex V-S5 appears similar to the interval from MIS 27 to MIS 31, the probable time-equivalents of the basal pedocomplex. Both periods are characterised by smaller amplitude oscillations between minimal and maximal d18O values, and presumably by smaller differences between temperate glacial and interglacial climates. The strongly developed paedological formations were therefore also presumably formed under significantly lower rates of dust deposition. The temperate glacial and interglacial periods in the region, which is currently the driest part of the Carpathian Basin, presumably were humid enough to form strongly developed fossil pedocomplexes without interbedded loess layers. Stari Slankamen lies at the boundary of a number of different air masses originating from the high and middle latitudes, as well as the maritime Atlantic and Mediterranean (Duci
c and Radovanovi
c, 2005). The influence of these air masses changed over glacialinterglacial cycles, as well as through the Pleistocene. As the record at Stari Slankamen is at a boundary of these competing climatic influences, it will be sensitive to changes in their strength and relative influence. Thus, the site can be regarded as a sensitive indicator of the dynamics of continental scale climatic systems, as well as regional climate, and the trend towards aridification at the site may not only be a local signature, but reflect a relative reduction in the influence of moisture-bearing systems over the course of the Middle Pleistocene during interglacials. The cause of this reduction may in part be due to the increasing influence of continental air masses, or indeed the migration northwards of moisturebearing westerly flow. While this reduction is not expressed at many other more maritime western or central European sites (Kukla, 1975; Haesaerts, 1990), these sites are closer to the main moisture sources and will be less sensitive to small changes in precipitation. According to this hypothesis, decreased humidity during the Pleistocene should be expressed most strongly from the middle Danube Basin to the Black Sea coast, where small changes in moisture will be most acutely felt. 5. Conclusions Stari Slankamen is the first Serbian loess site with a detailed multi-approach age model and, apart from the latest part of the Middle Pleistocene, is one of the most complete continental palaeoclimatic sequences in Europe. Palaeomagnetic measurements of the Stari Slankamen sequence provide evidence of the Matuyama-Bruhnes Boundary in the lower part of loess unit V-L9. Based on these aminostratigraphic and magnetostratigraphic data we propose a new interpretation of the existing chronostratigraphic models that suggests a mostly upward revision of previously published age determinations. Further, due to the unique length and completeness of the Stari record, and the clear distinction of the loess and palaeosol units, the site provides an opportunity to assign a Danube Basin-wide chronostratigraphic

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scheme that can further be used to develop transcontinental correlations across the Eurasian loess belt. The detailed magnetic susceptibility and soil stratigraphic record of the Stari Slankamen loess-palaeosol sequence also provides new insight into paedogenic processes driven by climatic change in the latest part of the Early Pleistocene and most of the Middle and Late Pleistocene. Correlation with MS records from other key loess sites in the Danube Basin confirms the absence of palaeosol V-S2. Except for this erosional unconformity, the Stari Slankamen loess-paleosol record of glacial and interglacial cycles generally correlates well with the global pattern of Middle Pleistocene climate changes and palaeoenvironmental evolution. However, there is a trend to increased aridification in interglacial climate that is not matched in intensity in global and many other European records, although some evidence suggests some warmer interglacials in the early-Middle Pleistocene of maritime Europe and potentially wetter MIS 11 conditions (Candy et al., 2006; Preece et al., 2007). While the full implications of these results remain to be explored the length and detail of the Stari Slankamen record make it one of the most important sequences for understanding Middle Pleistocene palaeoclimatic evolution in Central and Southeastern Europe. The new age model and preliminary palaeoclimatic interpretations presented here further add to the weight of evidence that European interglacial conditions contrast with the generalised pattern of many global marine records. Acknowledgements We thank Mladjen Jovanovi
c, Tivadar Gaudenyi, Nebojsa Milojkovi
c and Tin Luki
c for their help during the field and laboratory work. This research was supported by Project 176020 of the Serbian Ministry of Science. Two anonymous referees are thanked for their valuable input which significantly enhanced this paper. References Antoine, P., Rousseau, D.D., Fuchs, M., Hatté, C., Gautier, C., Markovi
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