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Quaternary Science Reviews 30 (2011) 1142e1154

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Quaternary Science Reviews

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

aChair of Physical Geography, Faculty of Sciences, University of Novi Sad, Trg D. Obradovi�ca 3, 21000 Novi Sad, SerbiabChair of Geomorphology, University of Bayreuth, D-95440 Bayreuth, GermanycCentre for Quaternary Research, Department of Geography, Royal Holloway, University of London, Egham, Surrey TW20 0EX, UKd Lamont-Doherty Earth Observatory of Columbia University, Rt. 9W, Palisades, NY 10964, USAe Institut für Geophysik, Department of Earth Sciences, CH-8093 Zürich, SwitzerlandfDepartment of Geosciences, University of Massachusetts, Amherst, MA 01003, USAgDepartment of Natural and Applied Sciences, Bentley University, Waltham, MA, USAhChair of Soil Physics, University of Bayreuth, D-95440 Bayreuth, Germany

a r t i c l e i n f o

Article history:Received 16 September 2010Received in revised form2 February 2011Accepted 9 February 2011Available online 9 March 2011

Keywords:LoessMagnetismPalaeoclimatePalaeosolAminostratigraphyPleistoceneMatuyama-BrunhesSerbiaStari Slankamen

* Corresponding author. Tel.: þ381 21 485 2837; faE-mail address: slobodan.markovic@dgt.uns.ac.rs (

0277-3791/$ e see front matter � 2011 Elsevier Ltd.doi:10.1016/j.quascirev.2011.02.004

a b s t r a c t

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 palaeopedocomplexes and can be considered to be one of the most important Quaternary sections in theCarpathian (Panonnian) basin. Here we present new magnetostratigraphic and aminostratigraphicevidence that demonstrates the importance of the site in terms of its age and the long-term palae-oclimatic record it preserves.

Directional palaeomagnetic data, obtained through alternating field demagnetization demonstratesthe presence of reversed polarity below a profile depth of 36 m indicating a Matuyama chron age of thisinterval. This interpretation is confirmed by new high resolution palaeomagnetic investigations (434oriented samples) from the lower part of the profile. The new magnetic susceptibility record and ami-nostratigraphy indicate a missing pedocomplex (V-S2), with an erosional unconformity represented bya distinct gravel layer. The combined new magnetostratigraphic and aminostratigraphic based age modelrequires 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 loesssequences. Hence, the sequence could form the basis of a continental scale stratigraphic scheme thatwould alleviate much current chronostratigraphic uncertainty and enable more broad-scale climaticreconstructions. The section also provides a rare opportunity to investigate detailed and long-termclimatic change over the Middle Pleistocene in a region influenced by air masses originating from highand middle latitudes, as well as the North Atlantic and Mediterranean. The changing relative importanceof these air masses through time provides insight into local and regional atmospheric systems and theirevolution through the last c.1 Ma. The section can thus be considered as one of the key climatic archivesin the Europe.

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1. Introduction

Loess deposits are considered to be some of themost detailed andlong-term records of late Caenozoic climate change (Porter, 2001).

x: þ381 21 459 696.S.B. Markovi�c).

All rights reserved.

Modern loess research effectively began with the pioneeringpalaeomagnetic investigation of the Red Hill (�Cerveny Kopec) loessexposure near to Brno in the Czech Republic (Bucha et al., 1969).While the Upper Pleistocene and part of the Middle Pleistocene havenow been removed after raw material exploitation, the sectionoriginally contained about 1 Ma of loess sediments and provided thechronostratigraphic 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 investigationswere made in the Danubian loess sequences (e.g. Fink and Kukla,1977), with the work of Heller and Liu (1982, 1984, 1986) the focussubsequently shifted to China where aeolian deposits potentiallyextend to the base of the Miocene (Guo et al., 2002). Initial investi-gations in China focused onpalaeomagnetic zonation of the c. 2.5MaLuochuan loess sequence, and on the record of magnetic suscepti-bility (MS) variations as one of the most sensitive loess proxies forpalaeoclimatic change. Many MS studies of Chinese, Central Asian,European, New Zealand and North and South American loessdeposits followed and made significant advances in the recon-struction of terrestrial Pleistocene environmental processes (e.g.Heller and Evans, 1995; Evans and Heller, 2001).

However, a persistent problem in loess research is the apparentabsence of a significant pre-Late Pleistocene record frommany of theloess belt areas, notably in Europe. The lack of such loess has previ-ously been explained as a consequence of recycling of previouslydeposited material during subsequent glacial periods (van Loon,2006), but in any case has severely limited understanding of Earlyand Middle Pleistocene climate in continental regions. The loesssequence at Stari Slankamen in northern Serbia comprises multiplecouplets of loess and palaeosol units in 40 m of sediments. Thisstrongly suggests a considerably longer record is preserved at the sitethan that in the majority of loess deposits (Singhvi et al., 1989).Despite this obvious significance, detailed chronostratigraphic andpalaeoclimatic investigations of the Stari Slankamen loess exposurehave so far been limited (Bronger, 1976, 2003; Singhvi et al., 1989).

A significant difficulty in analysing Middle Pleistocene palae-oclimate records obtained from loess deposits lies in the constructionof an accurate age model. Few independent dating techniques thatcover this age rangecanbeapplied to loess.Assuch,manystudieshavecorrelated sequences over long distances using soil stratigraphy(Kukla, 1975; Bronger, 2003). However, regional pedofacies changesand the possibility ofmissingor truncated soil or loess units limit suchage models. Magnetostratigraphic characterization is more objectiveand candetermine thebroad chronostratigraphyof a sequence, if longenough, but will not be suitable for differentiating between gla-cialeinterglacial cycleunits of theMiddlePleistocene, if onlymagneticpolarity stratigraphy is applied. However, amino acid geochronologyhas been successfully applied to Middle Pleistocene loess depositsthroughout Europe andChina and enables stratigraphic subdivisionofglacialeinterglacial units (Oches and McCoy, 2001). In particular, theratio of diastereoisomers D-alloisoleucine and L-isoleucine extractedfrom shells of fossil gastropods (notablyHelicopsis, Pupilla, Trichia andVallonia sp.) have the potential to provide relative chronologies forloess-palaeosol sequences of the Middle Pleistocene and have previ-ouslybeensuccessfullyapplied toSerbian loess (Markovi�c et al., 2004).A combination of these dating techniques has the potential to allowdevelopment of a detailed and long-term age model over multi-millennial timescales at Stari Slankamen.

Stari Slankamen is significant not only because of the age rangecovered by the loess, but also because it is influenced by air massesoriginating in both high and middle latitudes, as well as the NorthAtlantic and Mediterranean. The near-continental nature of theclimate at the site means that even small changes in precipitationassociated with the changing influence of these air masses shouldregister significant changes in the climate proxies (Duci�c andRadovanovi�c, 2005). Such information is certainly of regionalsignificance, but likely originates from wider scale shifts in atmo-spheric and oceanographic systems. Thus the record at Stari Slan-kamen has the potential to provide rare and significant insight intolocal- and broad-scale atmospheric-oceanographic changes andprovide insight into the long-term evolution of Middle and LatePleistocene climate in Europe.

Here, we apply magnetostratigraphic and amino acid racemi-zation (AAR) dating, together with litho- pedostratigraphic anal-yses to the Stari Slankamen exposure in order to ascertain the a) ageand b) potential palaeoclimatic significance of the site. The mag-netostratigraphy includes magnetic polarity as well as magneticsusceptibility stratigraphy (Opdyke and Channell, 1996; Hambachet al., 2008). The data presented in this study confirm andemphasize the antiquity of the sediments preserved in the sectionand demonstrate the significance of the detailed and relativelycomplete palaeoclimatic record they contain.

2. Sampling and methods

The exposure at Stari Slankamen is located in the southeasternpart of the Carpathian Basin (Fig.1) in the northeastern part of SremLoess Plateau, on the western bank of the Danube River, oppositethe Tisa confluence (45�0705800 N; 20�1804400 E) (Fig. 2).

Fifty nine oriented samples spanning a thickness of 40 m weretaken for palaeomagnetic analysis. The analyses were performed atthe palaeomagnetic Laboratory of the Institute of Geophysics at theETH Zürich, Switzerland. Directional palaeomagnetic data, wereobtained after alternatingfield (AF) demagnetization between5 and15 mT using a 2G cryogenic magnetometer with in line two axis AFdemagnetizer (Evans and Heller, 2001, 2003). In situ and laboratorymeasurements of low field initial magnetic susceptibility (MS)wereconducted at 10 cm intervals in palaeosol horizons and at 15 cmintervals in loess layers. MS variation in the lower part of the profile,below the loess layer V-L5, was measured in situ using a portableBartington MS2 susceptibility metre. At each level, 10 repeat read-ings were taken and averaged. Samples from the upper part of theexposureweremeasured on a Bartington susceptibilityMS2Bmetrewith a 36 mm opening at the Lamont-Doherty Geophysical labora-tory in Palisades, New York. Selected samples from the lower part ofthe profile were re-measured, which made it possible to cross-calibrate MS values obtained by different instruments.

In 2005, high resolution magnetostratigraphic sampling wasundertaken in the lower part of the profile. 434 samples werecollected from two parallel columns in steps of 5 cm. Orientedspecimens were taken using brass tubes and an orientation holder.Samples are cubes with an edge length of 2 cm, giving a volume of8 cm3. Full spatial orientation was provided by magnetic compassmeasurements.

Measurements of palaeo- and rock-magnetic parameters wereperformed in the Laboratory for Palaeo- and Environmental Magne-tism (PUM), University of Bayreuth. All specimens were subjected tostandard rock and palaeomagnetic laboratory procedures to revealtheir rock-magnetic characteristics and to decipher the directionaltrends of the Earth’s past magnetic field stored in the sediment(Hambach et al., 2008). The initial low field magnetic susceptibilitywas measured in an AC-field of 300 A/m at 875 Hz using the AGICOKLY-3-Spinner-Kappa-Bridge (AGICO, Brno, Czech Republic) and isgiven as mass specific susceptibility (c). Stepped demagnetisationand remanencemeasurementswere conducted employing anAGICOJR-6A spinner magnetometer and a Magnon AFD 300 (MAGNON,Dassel, Germany) demagnetiser. Full details of the palaeomagneticanalyses require a dedicated paper and will be presented in a futuresubmission. Here, an outline of the key results obtained is presented,sufficient to draw the chronostratigraphical conclusions relevant tothe multi-millennial timescales addressed in this paper.

Six bulk sediment samples were collected in 2002 from eachloess unit at Stari Slankamen (except V-L5), from which molluscshells were extracted after wet-sieving for measurement of aminoacid racemization. Gastropod shells of Pupilla, Helicopsis, Succinea,and Trichia genera were recovered in sufficient number for robustanalysis. The ratio of D to L isomers of various amino acids in

Fig. 1. Topographic map showing the locations of the main Middle Pleistocene loess sites in the Danube Basin: Stari Slankamen, Mo�sorin, Batajnica, Ruma, �Cerveny Kopec, Krems,Stranzendorf, Paks, Ljubenovo, Viatovo, Koriten, Mostistea, Mircea Voda, and Costinesti.

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gastropod shells can be obtained and correlated with valuesobtained from other loess-palaeosol units elsewhere in Europe inorder to independently assess chronostratigraphic interpretationsof loess profiles (Oches and McCoy, 2001). Rates of racemizationdiffer between genera, as well as among several amino acids andhence must be interpreted separately. The amount of the increasein D/L ratio from loess of one glacial cycle to the next decreases withincreasing age as the extent of racemization asymptoticallyapproaches an equilibrium value of 1.0 (w1.3 for AI). Thus theresolution of the method decreases with age and the methodgenerally cannot reliably discriminate glacial cycles older thanabout 700,000 years in the midlatitudes. Samples were preparedand analysed using the reverse-phase liquid chromatographymethod following the procedure of Kaufman and Manley (1998).

3. Results

3.1. Section description

Earlier descriptions of the Stari Slankamen exposure were madeby 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 analysisof two neighbouring exposures: a longer loess-palaeosol sequenceon the bank of the Danube (marked as A on Fig. 2) and a sequence ofapparently younger loess (Gorijanovi�c-Kramberger, 1921) 1.1 kmfrom the main section (B on Fig. 2). A further complicating factor isan erosion layer (labelled EL in Fig. 3) marked by gravel-sized rock

fragments and located in the loess below palaeosol V-S1 (forstratigraphic nomenclature see Fig. 3). Both the gravel layer and theoverlying 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 mainsection from the middle part of the loess layer V-L9 to the base iscurrently obscured by slumpmaterial. During the fieldwork in 2005,a trench was dug in this section, enabling detailed morphologicaldescription and collection of newhigh resolution samples for palaeo-and rock-magnetic analyses. The relationship between this datasetand an earlier one published inMarkovi�c et al. (2003) is presented inFig. 4. During the trench description, amore complicated structure ofthe loess-paleosol units below V-S8 thanwas presented in Markovi�cet al. (2003) was observed, identifying, relative to the neighbouringpedocomplexes, a weakly developed palaeosol V-S9 and the under-lying loess unit V-L10. Below V-L10 lies a complex of multiple butindistinguishable soils. In this study, the section (A) facing theDanubeis the main focus. The descriptions of the Stari Slankamen loess-palaeosol sequences are presented in Fig. 3 and Table 1.

3.2. Trends in directional palaeomagnetic data

One of the key control points in the chronostratigraphicalsubdivision of the Stari Slankamen sequence is the Matuyama-Brunhes palaeomagnetic boundary (MBB; 0.78 Ma according toCande and Kent, 1995). The directional palaeomagnetic dataobtained after AF demagnetization from the main section demon-strate the presence of reversed polarity below a profile depth of

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

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36 m indicating a Matuyama chron age of the lower part of thelowest loess layer V-L9 (Fig. 4). A transitional magnetic polarityinterval is visible just below the polarity change although this islikely to be a result of the interplay between chemical and detritalremanent magnetization and lock-in depth (e.g. Spassov et al.,2003; Liu et al., 2008). The observation of the MBB at Stari Slan-kamen is the first in the loess-palaeosol sequences of Serbia.

The new palaeomagnetic results from the lower part of thesection, from palaeosol V-S6 to the profile base, also reveal a tran-sition from normal, through mixed and fully reversed polarity(Fig. 5). These preliminary data are based on remanencemeasurements after AF-treatment in fields up to 40 mT. Exclusivelynormal polarity of the Brunhes Chronwas found at palaeosols V-S6,V-S7 and V-S8, as well as in loess units V-L7 and V-L8. A complexpattern of mixed polarity starts in the upper part of loess unit V-L9from about 5 m downward, with the transition to fully reversedpolarity of the Matuyama Chron in V-L10, just below V-S9. The shiftto clear reversed polarity starts in the middle of fossil soil V-S9(Hambach et al., 2009), at a similar profile depth to that indicatedby initial measurements (Markovi�c et al., 2003). A 2m thick intervalfrom the centre of V-S9 to the top of the basal pedocomplex showsalmost fully reversed polarity. The lowermost 1 m of the section,within the basal pedocomplex, exhibits an interval of normalpolarity, potentially indicating the Jaramillo Subchron (Hambachet al., 2009) (Fig. 5).

The results from detailed stepwise alternating field (AF)demagnetisation experiments are shown in Fig. 5. The inclinations

of the natural remanent magnetisation (NRM) vectors are shown asfunction of stratigraphy and AF-amplitude. The progressive changeof the NRM-inclinations with the field amplitude during AF-demagnetisation reveals normally overprinted reversed rema-nences in the lower half of the profile. As discussed above, thelowermost metre and the upper 6 m are clearly of normal polarity.The preliminary results demonstrate that AF-demagnetisation infields up to 40 mT is not enough to separate normal and reversedoverprints from primarily reversed or normal remanencesrespectively.

3.3. Magnetic susceptibility record

The low field initial MS variations in the Stari Slankamen loess-palaeosol sequence are hypothesised to reflect Middle and LatePleistocene palaeoclimatic fluctuations at the site, in particular,changes in humidity (Markovi�c et al., 2009). The coincident increaseinMSwith the occurrence of soils (Fig. 4) strongly suggests a similarmechanism to that found in loess on the Chinese Loess Plateau(Heller and Liu, 1984). Although there is a general decrease in MSvalues up section, the finer-scale variations clearly reflect thepedostratigraphy of the Stari Slankamen section (Fig. 4). MS valuesmeasured inpalaeosols (mean value 68.5�10�8m3 kg�1) are on theaverage more than twice as high as those in the loess units (meanvalue 31.7 � 10�8 m3 kg�1). The lowest value was measured in theloess unit below palaeosol V-S1 (10.3 � 10�8 m3 kg�1) whereas thehighest value is in palaeosol V-S8 (165.7 � 10�8 m3 kg�1). Similarresults were obtained from the re-sampled lower part of the section(Hambach et al., 2009). Comparisons between MS variations inpalaeosols V-S6, V-L7S1, V-S7, V-S8, and the basal pedocomplexprovide good agreement between old and new results (Fig. 4).ManyMS variations within loess units V-L7 and V-L9 are caused bystrongly bioturbated loess and humic infiltrations in pre-existingstrongly developed root channels, and therefore cannot be ascribedto changes in humidity. The only significant difference between oldand newmeasurements is related to palaeosol V-S9, which was notobserved before the trench was dug in 2005 (Fig. 4).

The cyclicity of alternating high and low MS values betweenpalaeosols and loess units reflects magnetic susceptibilityenhancement due to different degrees of paedogenesis betweenglacial and interglacial periods (Markovi�c et al., 2008, 2009; Buggleet al., 2009; Antoine et al., 2009), similar to that observed inChinese and Central Asian loess deposits (Heller and Liu, 1984,1986; Maher and Thomson, 1999). Importantly, one of the keyfeatures of the record is the decrease in interglacial MS valuesthrough time from the basal complex to V-S1 (Fig. 4).

3.4. Aminostratigraphy

Amino acid data from shells recovered from loess at Stari Slan-kamen show a general increase in D/L ratio with stratigraphic age(Table 2). Herewe report D/L ratios for glutamic acid (Glu) and valine(Val), and the ratio of alloisoleucine to isoleucine (AI) for the generaHelicopsis, Pupilla, and Succinea (Tables 2 and 3). Most of the datashow a clear discrimination of the upper five sampled loess units atStari Slankamen. However the variability in the ratios also generallyincreases and the resolution diminishes with depth (Table 2), withV-L9not clearlydistinct fromV-L7 in thePupilladata. In addition, thesingleHelicopsis shell fromV-L9 has anomalous D/L values. It may becontaminated or intruded into V-L9 from above, perhaps by animalburrows or along root channels. The youngest loess was not acces-sible at site A at the time of our field sampling and our sample fromV-L1 was taken from site B (Fig. 2). At that site the upper loess hasbeen eroded considerably and the Holocene and V-L1S1 soils aremissing. Despite this the data appear capable of distinguishing

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) withthermoluminescence ages after Singhvi et al. (1989); 4. Butrym et al. (1991); 5. Schmidt et al. (2010); Interpretation presented here, with legend.

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between glacialeinterglacial cycles when compared to otherregional aminostratigraphic data.

4. Discussion

4.1. Stratigraphic overview

There have been a number of stratigraphicmodels developed forthe Stari Slankamen loess, with differing nomenclature andnumbers of fossil soils (Fig. 3). In the initial stratigraphic interpre-tations of the Stari Slankamen sequence presented by Markovi�c-Marjanovi�c (1970, 1972), seven pedocomplexes were described inthe main exposure. Bronger (1976) described a regional (MiddleDanube Basin) pedostratigraphic sequence in which each fossil soilwas marked with the letter F and numbered in order of increasingage and depth. Later, Butrym et al. (1991) defined another strati-graphic model for the Stari Slankamen loess-palaeosol sequences,marking soils from a1 on the top of profile to the lowest exposedfossil soil at the time of their investigation,n3.Markovi�c et al. (2003)designated the loess-palaeosol unit names in north Serbia followingtheChinese loess stratigraphic system (e.g. Liu et al.,1985; Kukla andAn, 1989), but inserting the prefix “SL”, referring to the Stari Slan-kamen site as standard type section. However, to avoid confusiondue 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 loess-palaeosol stratigraphy in Vojvodina (Markovi�c et al., 2008). Thescheme therefore allows for information from the penultimateinterglacial to be included, based uponother sections (e.g. RumaandBatajnica; Markovi�c et al., 2006, 2009). Chinese L (loess) and S (soil)stratigraphic nomenclature has also recently been used in strati-graphic 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 ofthe Stari Slankamen loess-palaeosol sequence, and presents ourrevised chronostratigraphic model, based on the results presentedabove. The position of the MBB in the Stari Slankamenmain sectionoccurs in the lower part of a relatively thick loess unit V-L9 in ourmodel (MIS 22e24). An interval of reversed to unclear polarity isidentified below this, still within the V-L9 unit, as well as in loesslayer V-L10 and the upper part of Stari Slankamen basal pedo-complex. Below this, the apparent decrease in the MS of the basalcomplex coincides with occurrence of a normal polarity interval,probably related to the Jaramillo subchron (Fig. 6).

The detailed results from the new palaeomagnetic sampling in2005 reveal a trend of the directional palaeomagnetic data that weinterpret in terms of geomagnetic polarity. Taking into account the

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 (thelowermost 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 profileuncovered after field work in 2005 and arrows connect peaks from the two profiles.

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palaeosol-loess stratigraphy, MS variations with depth and thetentative polarity pattern, we interpret the double soil complexV-S7/V-S8 as the equivalent of MIS 19 and 21, corresponding to S7 andS8 in the Chinese loess stratigraphy. Lock-in, strong paedogenesisand root activity transferred the MBB to the V-L9 loess, whichcorresponds to L9 in China. Consequently, the normally magnetisedV-S10 complex at the base of the section is the amalgamatedequivalent 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 canbe assigned to the late Matuyama and early Brunhes Chrons.Although the directional record is ambiguous in some intervalswhere strong paedogenesis caused secondary magnetisations,evidence for late Matuyama geomagnetic excursions is present. Inthe upper half of V-S9 (equivalent to S9 in China; MIS 25) normalpolarity seems to be persistent (Fig. 5). This stable normal polaritymay represent the incomplete record of the so-called Kamikatsuraand Santa Rossa geomagnetic excursions occurring around 0.9 Ma.Furthermore, at the top of V-S6 two samples show a trend toreversed polarity during progressive AF-demagnetisation. Thisinterval may correspond to the so-called Stage 17 excursion, whichwould give an age of approximately 0.685 Ma (Channell et al.,2009).

The MBB at Stari Slankamen is located stratigraphically deeperthan in Chinese loess (Zhou and Shackleton, 1999). In China thelock-in of the magnetic signal in loess differs from that in marinecores where the MBB is found inwarm period MIS 19, the apparent

true age of the reversal, although probably also slightly offset. Thecontrasting processes of detrital and chemical remanent magnet-isation have been shown to interact in Chinese loess sequences toyield an alternating signature, even when the geomagnetic fieldmay not have varied (Spassov et al., 2003). Such processes mayaccount for some of the complexities seen here, in addition to theeffects of paedogenesis and root activity. Thus, although the truereversal took place during deposition of V-S7 (MIS 19), the eventwas only registered in underlying V-L9 due to complex lock-inprocesses. The lock-in effect seems to be greater than at Viatovo inBulgaria, which places the MBB within Viatovo loess unit L7(equivalent of MIS 20) (Jordanova et al., 2008), similar to that inChinese loess. However, at Stari Slankamen, strong root channelsstemming from palaeosol-complex V- S8 penetrate several metresdown into loess V-L9 and probably also influence the magneticproperties of these sediments. Despite this, the lowermost pedo-complex at Stari Slankamen provides a similar palaeomagneticrecord to the basal ‘red clay’ complex at Viatovo (Jordanova et al.,2008) with normal polarity at both possibly related to the Jar-amillo normal subchron. These interpretations suggest that thebasal pedocomplex was deposited and weathered over severalglacialeinterglacial cycles and is highly condensed.

Our detailed subdivision of the Brunhes Chron is based on theMS and amino acid data. In general, because of the high energies ofactivation of the reactions, the rates of amino acid racemizationwithin fossil gastropod shells contained in the loess are very muchgreater during warm interglacials than during cold glacials.Therefore, the extent of racemization of a particular amino acid

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

Unit/subunit Depth (cm) Description

V-S0 0e70 Recent soil Ah horizon partly erodedV-L1 V-L1L1 70e760 70e285 Porous loess with krotovinas

V-L1S1 285e545 Three layers of weak paedogenesis with krotovinas separated with thin porous loess layersV-L1L2 545e760 Light porous sandy loess

V-S1 760e980 Chernozem pedocomplex with several krotovinasV-L2 V-L2L1 1075e1400 Loess with many snails shells and hydromorphic features

L2S1 1075e1235 Weakly developed initial paedogenetic layer with hydromorphic featuresL2L2? 1235e1400 Loess with intensively developed hydromorphic features

Erosional layer 1400e1420 Pebbles and cobbles of local lithology up to 10 cm in diameterV-S3 1525e1680 Phaeozem (Degraded Chernozem) pedocomplex with krotovinas in upper partV-L4 1680e1805 Thin loess layer with humic infiltrations in former root channelsV-S4 1805e1905 Cambisol pedocomlex with krotovinas in the uppermost part.V-L5 1905e2110 LoessV-S5 2100e2285 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 porousBwt horizon is strongly developed.

V-L6 V-L6L1 2285e2680 Loess with large carbonate concretions (>20 cm in diameter)V-L6S1 Embryonic palaeosolV-L6L2 Thick loess

V-S6 2680e2910 Cambisol pedocomplexV-L7 V-L7L1 2910e3195 2910e3035 Thin loess layer with carbonate concretions and strongly developed humic infiltrations in former

root channels with many snail shells.V-L7S1 3030e3135 Chromic Cambisol palaeosol, more weakly developed than the V-S7 and V-S8 pedocomplexV-L7L2 3135e3195 Loess with carbonate concretions and strongly developed humic infiltrations in former root channels

V-S7 3195e3290 Chromic cambisolV-L8 3290e3330 Thin loess layer with carbonate concretions (5e15 cm) and humic infiltrations in strongly

developed former root channelsV-S8 3330e3435 Chromic cambisolV-L9 3435e3645 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).V-S9 3645e3750 Weakly developed cambisol with hydromorphic featuresV-L10 3750e3835 Loess with smaller humic infiltrations in former root channels with hydromorphic features.Basal complex 3835-4050? Cromic Luvisol pedocomplex with many relatively soft carbonate nodules and fossilized tree remains

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

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measured within fossil shells today generally does not vary muchbetween shells within loess of a single glacial cycle (from a limitedgeographical region), but does show marked increases in shellsfrom loess of successively older glacial cycles. Combined withexisting data from other nearby regions (Fig. 7) and MS records thedata can be used as an independent check on the palaeomagnetismresults and to provide more detailed stratigraphic subdivisions inthe Brunhes Chron.

The MS and amino acid variation in the upper part of the profilesuggests a correlation of palaeosols V-S1, V-S3, and V-S4 with MIS5, 9, and 11, respectively. Sample 020701e6 was taken from about1 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 glacial-cycle loess (V-L1L2). Helicopsis from sample 020701e6 has AIvalues of 0.18 � 0.02 (Table 2) which overlaps with values from theL1L2 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 tothose of Pupilla from L1L2 loess at Petrovaradin (0.09 � 0.01;Markovi�c et al., 2008). Somewhat lower AI ratios (0.06e0.08) aretypically recorded from shell samples taken from loess above theL1S1 soil at other sites in Vojvodina (Markovi�c et al., 2008). AI ratiosfrom V-L1 at Stari Slankamen are consistent with the AI ratios fromsamples taken from L1 loess below the interstadial soils in Vojvo-dina and as such we correlate the sampled loess at Stari Slankamenwith V-L1L2.

We have no shell samples from loess at Stari Slankamen thathave D/L ratios similar to L2 loess elsewhere in Vojvodina (Table 3;Fig. 7). The difference in D/L ratios between the upper two sampledloess units at Stari Slankamen is remarkable and is much greaterthan is seen between loess units of the last two glacial cycles

throughout Europe (Fig. 7). These two units are separated bya gravel layer approximately 20 cm thick in the loess belowpalaeosol V-L2S1, comprising poorly sorted rounded cobble andgravel clasts up to 10e15 cm in diameter. In fact, the D/L ratios inloess from directly below the gravel layer at Stari Slankamen aresimilar to those found in the L3 loess elsewhere in Vojvodina.Markovi�c et al. (2006) report AI ratios in Helicopsis shells from thelower part of L3 at Ruma as 0.34� 0.11. A resampling of the L3 loessthere yields more consistent Helicopsis AI ratios of 0.34 � 0.01(unpublished data: FAL953). These values compare closely to the0.36 � 0.03 AI ratios for Helicopsis from V-L3 at Stari Slankamen(Table 2). Furthermore, the D/L ratios from V-L3 at Stari Slankamenare similar to those that would be expected for loess of glacial cycleD in Vojvodina based on data from other parts of Europe (Fig. 7). Forexample, the Pupilla AI ratios from V-L3 at Stari Slankamen(0.27� 0.03) are slightly higher than, but overlap with, those foundin 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 Vojvodinaare expected due the w1 �C higher current mean annual temper-atures there.

We can also compare D/L ratios in Succinea from V-L3 (belowthe erosion layer) at Stari Slankamen with those from Succineafrom the L2 loess at Petrovaradin, located about 40 km east-northeast of Stari Slankamen (Table 3). The sites are close enoughand have a sufficiently similar present-day climate that D/L ratiosfor 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 Slanka-men are consistently much greater than those from the L2 loess atPetrovaradin, indicating that V-L3 is considerably older and likelyto be from the previous glacial cycle. Therefore, given the bulk ofthe amino acid data, we judge it is likely that the loess found

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. Theinclinations of the natural remanent magnetisation (NRM) vectors are shown as function of stratigraphy and AF-amplitude. Inclination values are given as positive numbers whenthe vector is dipping downward. The progressive change of NRM-inclinations with the field amplitude during AF-demagnetisation reveals normally overprinted reversed rema-nences 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 separatenormal/reversed overprints from primarily reversed/normal remanences, respectively. Mass specific susceptibility vs. depth is displayed at the right. The thin dashed vertical linesindicate 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, assumingthat V-S7 corresponds to MIS 19.

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immediately below the gravel layer at Stari Slankamen is V-L3 andis 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 StariSlankamen and the apparent unconformity is marked by thegravel overlying V-L3.

Incomplete preservation of the loess record in the upper part ofthe Stari Slankamen loess-palaeosol sequence is also suggestedthrough correlation of the MS record with other data from nearbyloess sites in the Danube Basin (Fig. 6). In all comparable sections,the second pedocomplex from the top displays a distinct patter ofMS variation with two discrete peaks. However, these features arenot shown in theMS record at Stari Slankamen (Fig. 6). This missingunit is coincident with the appearance of the gravel layer.

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

Sample Unit Helicopsis

D/L Glu D/L Val AI

020701e6 V-L1 0.19 � 0.02 (4) 0.14 � 0.02 (4) 0.18 �020701e2 V-L3 0.43 � 0.05 (8) 0.32 � 0.04 (8) 0.36 �020701e3 V-L4 0.46 � 0.11 (3) 0.41 � 0.13 (3) 0.35 �020701e5 V-L6 e e e

020701e4 V-L7 0.51 � 0.06 (2) 0.56 � 0.06 (2) 0.49 �020701e1 V-L9 0.40 (1) 0.42 (1) 0.39 (

a Note that sample 020701e6 from unit V-L1 was taken from site B and the other sampvaline (Val). AI represents the ratio of alloisoleucine to isoleucine. The specified uncertaanalyzed subsamples is given in parentheses.

The next older loess at Stari Slankamen is V-L4 and is generallywell differentiated from other losses by the D/L ratios. However, thelarge variation in D/L ratios in the Helicopsis samples suggests thatthere may be some mixing of a reworked older shell and perhapsintrusion of a younger shell. The Pupilla data from the same sampleshows much less variation and are consistent with Pupilla AI datafrom glacial cycle E loess in Hungary, given the temperaturedifference between the two regions.

No shells were recovered from the V-L5 loess at Stari Slankamenand there is much less data from other sites with which to comparethe amino acid results for samples from V-L6, V-L7 and V-L9.However, the limited results and the MS data support the previoussuggestion that the strongly developed palaeosol V-S5 formed

Pupilla

D/L Glu D/L Val AI

0.02 (4) 0.19 (1) 0.10 (1) 0.10 (1)0.03 (8) 0.39 � 0.05 (5) 0.28 � 0.03 (5) 0.27 � 0.03 (5)0.12 (3) 0.43 � 0.00 (2) 0.37 � 0.01 (2) 0.35 � 0.02 (2)

0.49 � 0.01 (5) 0.37 � 0.02 (5) 0.41 � 0.01 (5)0.06 (2) 0.57 � 0.02 (4) 0.47 � 0.06 (4) 0.51 � 0.11 (4)

1) 0.60 � 0.02 (3) 0.53 � 0.03 (3) 0.52 � 0.03 (3)

les were taken from site A (see Fig. 2). D/L mean values are for glutamic acid (Glu) andinty is the sample standard deviation. The number of independently prepared and

Table 3Comparison 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 Glu D/L Val AI

Petrovaradin 020627e6 V-L2 0.32 � 0.04 (4) 0.22 � 0.02 (4) 0.24 � 0.03 (4)Stari Slankamen 020701e2 V-L3 0.47 � 0.02 (7) 0.37 � 0.02 (7) 0.43 � 0.03 (7)

a 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.

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during MIS 13e15 (Bronger and Heinkele, 1989; Bronger et al.,1998; Bronger, 2003). Bronger et al. (1998) suggested that thispalaeosol (F6 by their nomenclature) formed over a period severaltimes longer than the Holocene. This pedocomplex shows a muchgreater degree of pedochemical weathering and clay mineralformation than modern soils in this region and appears to bea characteristic feature of the middle part of all Brunhes loess-palaeosol sediments in Eurasia (Bronger, 2003).

We further suggest that palaeosol V-S6 probably formed duringMIS 17 although between this level and the MBB chronostrati-graphic subdivisions are more tentative. In any case, the wholelower part of the Stari Slankamen exposure suggests ratherdifferent palaeoenvironmental conditions compared to the upperpart of the sequence, possibly due to shallower ground water levelsat that time. These differences are typified by of the properties ofthin palaeosols V-L7S1, V-S7 and V-S8, probably equivalents of MIS18.3, 19 and 21 respectively.

The disparities between our chronostratigraphic interpretationsand previous ones (Table 4) are of the order of multiple gla-cialeinterglacial cycles. The reasons for these discrepancies prob-ably lie in the previous reliance on correlation to other incompletesequence where the absolute age of soils may be poorly con-strained, and probable age underestimation in previous thermo-luminescence dates (Roberts, 2008). Despite recent advances inluminescence dating techniques, including the application ofoptically stimulated luminescence (OSL) and infrared opticallystimulated luminescence (IRSL), the luminescence family of tech-niques is still generally acknowledged to have a normal upper agelimit of between 50 and 100 ka in loess deposits (Wintle andMurray, 2006; Roberts, 2008) and cannot be used for validgeochronologic assignments beyond these limits. However, recentadvances using post-IR IRSL may extend this to c. 250 ka (Thielet al., in press) and recently, Schmidt et al. (2010) obtained post-IR IRSL and IRSL dating results from loess units V-L1 and V-L2 thatsupport our chronostratigraphic model. Luminescence data fromlast glacial loess unit V-L1 yield ages of approximately 25e65 ka.These results are similar to recent IRSL or OSL dating for the lastglacial loess at other investigated sites in the Vojvodina regionreported in recent papers (Markovi�c et al., 2007, 2008; Fuchs et al.,2008; Bokhorst et al., 2009; Ujvari et al., 2010; Stevens et al., inpress). Further, dates from loess unit V-L2 yield minimum ages ofbetween 100 and 193 ka, supporting our suggestion of a penulti-mate glacial age (Fig. 3).

Table 4Chronostratigraphic models proposed for the Stari Slankamen loess-palaeosol sequence.

Bronger (1976) Singhvi et al. (1989) Butrym et al.

Palaeosol Alpine sudivision MIS PalaeosolF2 Würm 5a dF3 palaeosols 5e Not observedF4 W gF5 ReW iF6 lF7 n1F8 n2F9F10F11

MIS refers to marine Oxygen Isotope Stage.

Thus, the new age-data presented in this study and comparisonswith other long Danube sections and recently published OSL/IRSLdating on Serbian loess demonstrate the need for a serious revisionof the earlier interpretations of the Stari Slankamen loess-palaeosolsequence. Many previous interpretations appear to have severelyunderestimated the age of the exposed units, and the number ofdiffering and conflicting stratigraphic models has caused confusion.

4.2. Correlation with other loess sites of the Danube Basin

The chronostratigraphic model presented above covers theperiod of the Middle Pleistocene climatic transition (Ruddimanet al., 1989; Heslop et al., 2002) and has the potential to broadenunderstanding of this period in continental settings. However, theconsiderable confusion over both the age and nomenclature ofMiddle Pleistocene Serbian loess stratigraphy (Table 4) is furthercompounded by numerous other chronostratigraphic models fromneighbouring countries in the Danube Basin that utilize differingnomenclature. A unified stratigraphic scheme for the region wouldalleviate much of this confusion and would enable direct testing ofthe equivalence of palaeosols between different parts of the Dan-ube Basin and allow broad-scale climatic interpretations to bemade.

The proposed age interpretations of the Stari Slankamensequence, outlined above with reference to other loess-palaeosolsites, allows for the development of a unified stratigraphic schemefor the Danube Basin. As many of the previously studied MiddlePleistocene Danubian loess sequences are either incomplete or nolonger accessible (e.g. Red Hill), Stari Slankamen is unique in havingnear-complete preservation of every loess and palaeosol unitassociated with a glacial or interglacial period through the Middleand Lower Pleistocene. The missing palaeosol V-S2 can be accom-modated with reference to nearby sites. Further, the relatively aridclimate at the site has ensured that only major climatic ameliora-tions are recorded in the pedostratigraphy, in a manner similar tomuch of the Chinese Loess Plateau. As such, a relatively simpledelineation of glacialeinterglacial cycles can be derived from thestratigraphy, backed up by absolute dating. Many other sites in theDanube Basin experienced a more humid climate and showa complicated stratigraphy towards the middle and base of theMiddle Pleistocene, such as Paks in Hungary, or have apparentlygreatly reduced resolution in the lower Middle Pleistocene, asindicated by pedocomplex S6 at Bulgarian and Romanian sites such

(1991) Bronger (2003) Model presented here

MIS Palaeosol MIS Palaeosol MIS5a F2 5a V-S1 5

F3 5e Not observed5c F4 7 V-S3 95e F5 9 or 11 V-S4 117 F6 13e15 V-S5 13e159 V-S6 179 V-L7S1 18.3

V-S7 19V-S8 21basal complex 25-?

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) andother 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), Mostistea(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 pedocomplexacross the Danube loess belt. Dotted lines represent correlations between the palaeomagnetic records.

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as Ljubenovo, Viatovo, Koriten, and Mircea Voda, limiting inter-pretations over this interval. The chronostratigraphy outlined inTable 4, based on the stratigraphic position and inferred timing ofthe MBB, the relative intensity of principal MS peaks,

Fig. 7. Total acid hydrolosate D-alloisoleucine/L-isoleucine aminostratigraphy of uppertwo samples from Stari Slankamen (V-L1L2, V-L3). As the uppermost Stari Slankamensample was taken from below V-L1S1, the values are compared to other Europeanlocalities 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 theterrestrial land snail Pupilla. SS ¼ Stari Slankamen, VJ ¼ other sites in Vojvodina, H ¼Hungary, A ¼ Austria, SK ¼ Slovakia, UA ¼ Ukraine, D ¼ Germany and CZ ¼ CzechRepublic (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 Vojvo-dina data have been measured using reverse-phase liquid chromatography (RPLC),rather than cation-exchange HPLC, which was used to obtain the other data. Analysisof standards shows that RPLC A/I ratios are about 4% higher than those obtained usingHPLC. This figure has not been adjusted to account for this offset but doing so wouldresult in an imperceptible change. Countries are presented in approximate order ofdecreasing mean annual temperature.

pedostratigrapic features and amino acid geochronology, is suffi-ciently complete to support a chronostratigraphic model to beproposed that can be applied as a type for the region. Testing of thismodel should be conducted using OSL and post-IR IRSL dating onthe upper parts of the section, and using this and other chrono-logical tools on other sites in the Danube Basin.

Fig. 6 shows the correlation between this Stari Slankamen chro-nostratigraphy and the main Middle Pleistocene sections of theDanube loess area. A broad-scale correlation with the SPECMAPmodel (Lisiecki andRaymo, 2005) andpalaeomagnetic zonationuptothe Jaramillo subchron is also proposed. The zonation correlates wellwith the record obtained from the northeastern Bulgarian loess-palaeosol sequence at Viatovo (Jordanova et al., 2008). Here theuppermost reversal recorded in loess unit L7 at Viatovo is attributedto the MBB geomagnetic polarity transition. Two normal magneto-zoneswere also found in the underlying “red clay” complex, probablycorresponding to the Jaramillo and Olduvai subchronozones of theMatuyama chron. This new chronostratigraphic model can also betied 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 StariSlankamen loess-palaeosol chronostratigraphic sequence andsequences inboththeupperand lowerDanubeBasin (Jordanovaetal.,2007; Buggle et al., 2009) (Fig. 6) and at the Black Sea coast (Tsatskinet al.,1998;Balescuetal., 2010), aswell as thewell preservednatureofthe record, opens up the possibility for a transcontinental correlationof European, Central Asian (Ding et al., 2002; Dodonovand Baizugina,1985; Machalett et al., 2008) and Chinese loess records (Liu et al.,1985; Kukla and An, 1989), using a standardised nomenclature andchronostratigraphic model.

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4.3. Broad climatic evolution at Stari Slankamen

The strongly rubified interglacial soils (Table 1) exposed in theyoungest Early Pleistocene and older-midMiddle Pleistocene (basalpedocomplex, pedocomplexes V-S7 and V-S8) and the strongestdeveloped pedocomplex at the profile (V-S5) are clearly differentfrom the temperate forest soils (V-S6 and V-S4) of the mid-lateMiddle Pleistocene and the steppe like interglacial soils of the laterMiddle and Late Pleistocene (V-S3, V-S1) (Fig. 4). These lowermostsoils in the sequence display characteristics associated withsubtropical soils (Bronger, 1976), in contrast to the temperate forest(V-S6 and V-S4) or steppe environments that appear to have beenresponsible for the formation of the middle and upper soils. Thesepalaeopedological observations have been confirmed by employingquantitative geochemical weathering proxies and a soil colourrubification index (Buggle et al., 2008, in press) and supports theprevious assertion (Bronger, 1976) that interglacial climate over thePleistocene has become progressively more arid in the region(Fig. 4).Assuming the signal to be reflective of climate, this gener-alised trend to decreased weathering up-section in interglacialunits contrasts with both the general understanding of globaltrends in Quaternary climate, as expressed in the marine record(Lisiecki and Raymo, 2005) and ice core records (EPICA, 2004), andalso regional climate proxies from lacustrine archives in south-eastern Europe (Tzedakis et al., 2006). The last of these recon-structions also suggests a smaller range of interglacial climatechanges than the succession of interglacials recorded in Serbianloess, ranging from subtropical to steppe.

However, the approximate timing of the main change in inter-glacial environments preserved at Stari Slankamen broadly coin-cides with the occurrence of warmer and shorter post Mid-BruhnesEvent (MBE) interglacials recorded in EPICA ice core deuteriumrecords (EPICA, 2004). They also correspond to the timing ofqualitative vegetation change observed in the Tenaghi Philipponpollen record, such as increasing dominance of drought-toleranttaxa such as Quercus and Carpinus after MIS 16 (Tzedakis et al.,2006). In addition, Vidi�c et al. (2004) have shown similar, albeitslightly less pronounced, decreases in rubification during theMiddle to Late Pleistocene at Jiaodao on the Chinese Loess Plateau.If taken as evidence of changing interglacial conditions during theMiddle Pleistocene, this 1) highlights the importance of obtaininglong-term regional records before conclusions over general climatictrends in specific regions are made from more hemispheric/globalarchives and 2) suggests that the pattern of long-term climaticdevelopment during the Pleistocene is more complicated andregionally variable than is implied bymany climatic global archives.

Of additional interest is palaeosol V-S4 (Fig. 2; Table 1). This unitcorrelates with MIS 11, previously hypothesised to be a longinterglacial and a potential analogue of Holocene insolationconditions (Berger and Loutre, 2002). However, V-S4 appears to beone of the least developed soils in the profile and is not excep-tionally thick, in contrast to what would be expected from themarine record. Further investigation of this soil promises to provideevidence concerning the climatic regime in eastern Central Europeover this interval. A further interesting aspect is the apparentlength of time covered by pedocomplex V-S5 and the basal pedo-complex. These strongly developed pedocomplexes may representextremely slow dust accumulation during prolonged interglacia-tions from MIS 13 to MIS 15 and over the late Early Pleistocene,probably MIS 27 to MIS 31 at least. Indeed, MIS 13e15 is expressedas 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 pedocomplexS5 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 stronglydeveloped pedocomplex S5 in Chinese loess may indicate relativelystrong summer monsoon conditions in East Asia (Yin and Guo,2008; Yin et al., 2008; Guo et al., 2009). However, explanation inSerbia is likely to be a prolonged period of low accumulation overMIS 13 to 15, where the probable reduced presence of ice sheetsand cold climate conditions for long periods lowered the produc-tion of dust that would form loess, reducing accumulation andprolonging exposure to the weathering front.

The multi-stage pedocomplex at the base of section may alsorepresent prolonged but extremely slow dust accumulation duringthe Early Pleistocene, pushing back the age of the onset of loessdeposition in the region by hundreds of thousands of years.According to Lisiecki and Raymo (2005), the benthic d18O patternduring the period coincident with the formation of the stronglydeveloped pedocomplex V-S5 appears similar to the interval fromMIS 27 to MIS 31, the probable time-equivalents of the basalpedocomplex. Both periods are characterised by smaller amplitudeoscillations between minimal and maximal d18O values, andpresumably by smaller differences between temperate glacial andinterglacial climates. The strongly developed paedological forma-tions were therefore also presumably formed under significantlylower rates of dust deposition. The temperate glacial and inter-glacial periods in the region, which is currently the driest part of theCarpathian Basin, presumably were humid enough to form stronglydeveloped fossil pedocomplexes without interbedded loess layers.

Stari Slankamen lies at the boundary of a number of different airmasses originating from the high and middle latitudes, as well asthe maritime Atlantic and Mediterranean (Duci�c and Radovanovi�c,2005). The influence of these air masses changed over glacial-interglacial cycles, as well as through the Pleistocene. As the recordat Stari Slankamen is at a boundary of these competing climaticinfluences, it will be sensitive to changes in their strength andrelative influence. Thus, the site can be regarded as a sensitiveindicator of the dynamics of continental scale climatic systems, aswell as regional climate, and the trend towards aridification at thesite may not only be a local signature, but reflect a relative reduc-tion in the influence of moisture-bearing systems over the course ofthe Middle Pleistocene during interglacials. The cause of thisreduction may in part be due to the increasing influence of conti-nental air masses, or indeed the migration northwards of moisture-bearing westerly flow. While this reduction is not expressed atmany other more maritime western or central European sites(Kukla, 1975; Haesaerts, 1990), these sites are closer to the mainmoisture sources and will be less sensitive to small changes inprecipitation. According to this hypothesis, decreased humidityduring the Pleistocene should be expressed most strongly from themiddle Danube Basin to the Black Sea coast, where small changes inmoisture will be most acutely felt.

5. Conclusions

Stari Slankamen is the first Serbian loess site with a detailedmulti-approach age model and, apart from the latest part of theMiddle Pleistocene, is one of the most complete continentalpalaeoclimatic sequences in Europe. Palaeomagnetic measure-ments of the Stari Slankamen sequence provide evidence of theMatuyama-Bruhnes Boundary in the lower part of loess unit V-L9.Based on these aminostratigraphic and magnetostratigraphic datawe propose a new interpretation of the existing chronostrati-graphic models that suggests a mostly upward revision of previ-ously published age determinations. Further, due to the uniquelength and completeness of the Stari record, and the cleardistinction of the loess and palaeosol units, the site provides anopportunity to assign a Danube Basin-wide chronostratigraphic

S.B. Markovi�c et al. / Quaternary Science Reviews 30 (2011) 1142e1154 1153

scheme that can further be used to develop transcontinentalcorrelations across the Eurasian loess belt.

The detailed magnetic susceptibility and soil stratigraphicrecord of the Stari Slankamen loess-palaeosol sequence alsoprovides new insight into paedogenic processes driven by climaticchange in the latest part of the Early Pleistocene and most of theMiddle and Late Pleistocene. Correlation with MS records fromother key loess sites in the Danube Basin confirms the absence ofpalaeosol V-S2. Except for this erosional unconformity, the StariSlankamen loess-paleosol record of glacial and interglacial cyclesgenerally correlates well with the global pattern of Middle Pleis-tocene climate changes and palaeoenvironmental evolution.However, there is a trend to increased aridification in interglacialclimate that is not matched in intensity in global and many otherEuropean records, although some evidence suggests some warmerinterglacials in the early-Middle Pleistocene of maritime Europeand potentially wetter MIS 11 conditions (Candy et al., 2006; Preeceet al., 2007). While the full implications of these results remain tobe explored the length and detail of the Stari Slankamen recordmake it one of the most important sequences for understandingMiddle Pleistocene palaeoclimatic evolution in Central and South-eastern Europe. The new agemodel and preliminary palaeoclimaticinterpretations presented here further add to the weight ofevidence that European interglacial conditions contrast with thegeneralised pattern of many global marine records.

Acknowledgements

We thank Mladjen Jovanovi�c, Tivadar Gaudenyi, Neboj�saMilojkovi�c and Tin Luki�c for their help during the field and labo-ratory work. This research was supported by Project 176020 of theSerbian Ministry of Science. Two anonymous referees are thankedfor their valuable input which significantly enhanced this paper.

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