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West-european malacofauna from loess deposits of the Weichselian Upper Pleniglacial : Compilation and preliminary analysis of the database

Malacofaunes des loess du Pléniglaciaire weichselien supérieur d’Europe de l’Ouest : compilation et analyse préliminaire de la base de données.
Olivier Moine
p. 11-29

Résumés

Les mollusques terrestres sont des organismes utiles dans la reconstitution des paléoenvironnements glaciaires grâce à leur forte sensibilité écologique et à leur richesse dans les dépôts de lœss. Une banque d’assemblages malacologiques a donc été compilée pour les dépôts lœssiques du Pléniglaciaire supérieur weichselien de la partie ouest de la Grande Plaine européenne pour compléter les données périglaciaires disponibles et pallier le manque d’enregistrements polliniques ainsi que d’autres indicateurs paléoenvironnementaux biologiques. Pour chaque site, l’âge des échantillons a été vérifié précisément. La composition de la banque de données révèle un potentiel sous-exploité de la malacofaune terrestre en tant qu’indicateur paléoenvironnemental. La composition des assemblages a permis la distinction d’un domaine homogène froid, humide, peu végétalisé et associé à un permafrost riche en glace autour de la Manche et en Belgique, qui s’oppose à un domaine hétérogène, plus végétalisé, associé à un permafrost pauvre en glace, localisé en Allemagne. L’analyse de nouvelles séquences malacologiques est maintenant nécessaire à une meilleure définition des domaines environnementaux, à l’étude de l’évolution de leur extension au cours du temps et à l’obtention de reconstitutions paléoenvironnementales à l’échelle millénaire pour le domaine lœssique de la Grande Plaine européenne.

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Texte intégral

This work has been supported by the European Community - Marie Curie Grant (MOIF-CT-2004-509918). The author thanks Tom Meijer, who provided a more general reference list about European Quaternary and Tertiary malacology (Meijer, 2006) that was enriched by the bibliographical compilation done during this work. The author also thanks Jean-Pierre Lautridou, Jean-Laurent Monnier, and Pierre Antoine for stratigraphic information concerning several French sites, Pierre Antoine once again who helped with the drawing of Figure 2. The manuscript benefited the careful reviews of Pierre Antoine and Nicole Limondin-Lozouet, and of William McCoy for the English. Finally, I thank all librarians of Bayreuth University who contributed to the efficiency and the quickness of the bibliographical compilation.

1 - Introduction

1For the last twenty years, the reconstruction of European palaeoenvironmental changes of the last climatic cycle rose in importance, especially since the first characterisation of Heinrich Events in the North Atlantic Ocean sediments (Heinrich, 1988) and Dansgaard Oeschger cycles in Greenland ice‑cores (Dansgaard et al., 1993). The linkage of these phenomena with millennial-timescale global climatic changes led to the study of numerous high-resolution records in polar, oceanic and continental archives (See reviews by Voelker (2002) and Rohling et al. (2003) to understand their dynamics and mechanisms and to reconstruct associated millennial-timescale environmental changes on the continents. Palaeoenvironmental reconstructions or paleodatasets are required (1) by modellers to test the robustness of both functioning and outputs of climatic and vegetation models for conditions different than modern ones, like during the Last Glacial Maximum, before attempting the simulation of future changes (Prentice et al., 1998; Alfano et al., 2003; Huntley et al., 2003; Jost et al., 2005; Kageyama et al., 2006; Braconnot et al., 2007a; Braconnot et al., 2007b; Hargreaves et al., 2007; Roche et al., 2007; Wu et al., 2007), and (2) by archaeologists to study the distribution dynamics of Upper Pleistocene human populations on the continent (Bocquet-Appel & Demars, 2000a, 2000b; Demars, 2002; Bocquet-Appel et al., 2005; Demars, 2006).

2The European Great Plain is particularly interesting, as it was, during the last glaciation, a transition area between permanently occupied southern regions and almost unoccupied northern territories. In western Europe, the temporary presence of human settlements has been noted by compiling and dating open air sites (Haesaerts, 1978; Otte, 1979; Monnier, 1980; Otte, 1984; Haesaerts, 1994; Locht, 2004; Floss, 2006; Lautridou & Cliquet, 2006; Otte & Noiret, 2006). It suggests that human populations might have been forced by inhospitable conditions to move temporarily southwards, despite their ability to adapt to harsh climates and environments. However, the relative sparsity of large mammals (Antoine, 1991), and thus of game, suggests a poor vegetation cover and might also explain the difficult subsistence of human populations, especially during the Weichselian Upper Pleniglacial (Antoine et al., 2003).

3Most palaeoenvironmental reconstructions in Europe come from palynological sequences. Indeed, compared with other biological environmental proxies, i.e. molluscs, ostracods, diatoms, insects, small and large mammals, phytoliths and plant macro-fossils, pollen is preserved in various deposits, and often provides long, continuous or sub-continuous records (See review studies by Guiot (1993), Watts et al. (1996), Peyron et al. (1998), Allen & Huntley (2000), Caspers & Freund (2001), Guiter et al. (2003), Müller et al. (2003), Preusser (2004) and Sánchez Goñi (2006)). Concerning the last climatic cycle, many palynological sequences precisely recorded vegetation changes during the Eemian interglacial. On the contrary, pollen records of the last glaciation are often incomplete or show a lower resolution, especially for the Weichselian Upper Pleniglacial (~ Oxygen Isotope Stage 2 (OIS 2) (tab. 1). Most of them are also located outside the former periglacial domain of the European Great Plain, where eolian sedimentation was dominant (fig. 1). The same limitations affect the few available isotopic records from Belgian and French speleothems (Quinif et al., 1994; Genty et al., 2003).

4In Benelux countries, England and the Alpine area, palynological records are discontinuous and come from organic levels occurring in otherwise pollen-sterile deposits (fig. 1; tab. 1). The reconstruction of the regional vegetation evolution was based on pollen samples dated with 14C and reported on a chronological scale (Zagwin, 1961, 1974; Behre & van der Plicht, 1992). However, some gaps remain and the chronology of environmental changes is still approximate in levels older than the technical limits of the 14C dating method (Allen et al., 2000; Müller et al., 2003). In central France and in the Mediterranean domain, long and almost complete records have been obtained due to the nearly continuous sedimentation of drilled sites (seas, lakes and peat-bogs) (fig. 1; tab. 1). However, only the Füramoos record and several others from the Mediterranean domain show well-characterised millennialtimescale changes correlated with global climatic fluctuations recorded in Greenland ice-cores (Allen et al., 1999, 2000; Sánchez Goñi et al., 2000, 2002; Müller et al., 2003; Sánchez Goñi, 2006). In loess deposits, between both groups, pollen-based palaeoenvironmental reconstructions are limited or biased by both quantity and reliability of preserved material (Zelikson, 1995; Tomescu, 2000). As most other biological proxies mentioned above rarely provide continuous records throughout loess sequences, sedimentological, pedological and mineralogical indicators are preferentially used to reconstruct palaeoenvironmental changes (Huijzer & Vandenberghe, 1998).

5Consequently, after the successful characterisation of millennial-timescale environmental changes in the Nussloch loess section (Rhine Valley, Germany) based on the study of the terrestrial mollusc fauna (Moine et al., 2002; Moine, 2003; Moine et al., 2005) in the frame of a multi-proxy approach (Antoine et al., 2001; Hatté et al., 2001; Rousseau et al., 2002; Hatté & Guiot, 2005), the aim is now to evaluate whether or not molluscan records may fill in the lack of palaeoenvironmental data and allow the analysis of rapid environmental changes during the last glaciation in the loess domain. A first compilation of molluscan records of the last glaciation was performed by Rousseau et al. (1990) to strengthen the palaeoclimatic interpretation of a comparison between long loess sequences and associated molluscan records of Achenheim (France) and 0ervený Kopec (Czech Republic). The goal of the present work is to create a dataset of Weichselian Upper Pleniglacial molluscan records from Western Europe, as this time span is characterised by the thickest loess deposits (Haesaerts, 1985; Frechen, 1999; Antoine et al., 2001; Frechen et al., 2003). This compilation and appraisal of the data have thus been performed to evaluate the potential of available molluscan records.

Fig. 1: Location of last-glaciation pollen records in Europe.

Fig. 1: Location of last-glaciation pollen records in Europe.

Records located in northern continental Europe and in the Alps are discontinuous, whereas in France and in the Mediterranean domain most of the records are long and continuous. Records with the best time resolution are located in the Mediterranean domain except the Füramoos sequence located north of the Alps.

Tab1: Pollen records of the last glaciation and of the Weichselian Upper Pleniglacial.

Tab1: Pollen records of the last glaciation and of the Weichselian Upper Pleniglacial.

These records may be complete (+), incomplete (±) or absent (-) and millennial-time scale vegetation changes may be absent (-), present(±) or present and correlated with ice-core global climatic records from Greenland (+).

2 - West-european chronostratigraphic framework of the molluscan data

6This is a compilation of about one hundred publications from the last 120 years dealing with Quaternary malacology in loessic environments, or including malacological analyses.

7The quality of molluscan data relies on good identifications but also on the precision of their chronostratigraphic framework. In this study, I conduct a detailed checking of the Weichselian Upper Pleniglacial age of selected samples on the basis of absolute datings and stratigraphy. All ages are given as originally mentioned in the quoted publications.

8In the chosen reference sequence, i.e. Nussloch, the Weichselian Upper Pleniglacial is represented by about 10 m of loess alternating with gleys (tundra soils) deposited above the Lohne soil (Antoine et al., 2001). The Lohne soil marks the end of the Middle Pleniglacial in loess deposits from South Germany (Frechen, 1999), and has been dated at 27,2-31,3 ka cor. BP (top) and 28,4-31,4 ka cor. BP (base) by 14C dating (Hatté et al., 2001) and at 34 ± 3,2 ka BP (top) and 33,1 ± 5,2 ka BP (base) by OSL (Lang et al., 2003). Antoine et al. (2001) thus proposed to correlate the Lohne soil with both the Denekamp and GRIP IS-8 interstadials on the basis of absolute datings. The correlation between the Nussloch loess/gley alternation and GRIP interstadials IS-2 to IS-8 has been strengthened by the correlation between the loess grain size index in Nussloch and the dust concentration in the GRIP ice-core (Rousseau et al., 2002) and by the synchronicity between the molluscan abundance in Nussloch and δ18O record in the GRIP ice-core (Moine, 2003).

9In northwestern France, the main units constituting the Weichselian Upper Pleniglacial stratigraphy are from the base to the top: the Mesnil‑Esnard/Bonsecourt soil, the Lower Recent Loess, the Nagelbeek horizon and the Upper Recent Loess (Lautridou, 1985; Antoine et al., 1998). They overlie the Saint-Acheul soil complex, which represents the Weichselian Middle Pleniglacial in this area. According to the framework of stratigraphic correlations across northwestern Europe (fig. 2), the Lohne soil would be synchronous with the Les Vaux soil dated at 33050 ± 850 yr BP in Wezembeek Oppen (Belgium) (Haesaerts, 1985) and with the upper part of the Saint-Acheul soil complex (Antoine et al., 2001). The Nagelbeek horizon yields 14C ages of 22,270 ± 380 years BP in Kesselt (Belgium), and 22,190 ± 130 years BP in Lixhe (Belgium) (Haesaerts, 1985), and a TL age of 24 ± 2,7 ka BP in Achenheim (France) (Rousseau et al., 1998). The top of the Saint Acheul soil complex yields a TL age of 35,45 ± 3,7 ka BP in Villers‑Adam (France) (Locht et al., 2003). In Achenheim, a TL age of 34,1 ± 4,3 ka BP has also been obtained 0.7 m above a level of large ice‑wedges (Rousseau et al., 1998) correlated with the Middle/Upper Pleniglacial transition (Rousseau & Puisségur, 1990). Consequently, I selected all molluscan records located above the Saint‑Acheul, Les Vaux and Lohne soils, or which have an age between ca. 34‑35 and 1516 ka BP, i.e. the age of the youngest Weichselian Upper Pleniglacial loess (Frechen, 1999).

Fig. 2: Correlation between regional composite chronostratigraphical frameworks in Western Europe for the Weichselian Upper Pleniglacial

Fig. 2: Correlation between regional composite chronostratigraphical frameworks in Western Europe for the Weichselian Upper Pleniglacial

All selected molluscan samples are located between the top of the basal soil, indicating the end of the Weichselian Middle Pleniglacial, and the base of Lateglacial deposits, i.e. between 35 ± 2 and ~ 15‑16 ka BP.

after Antoine et al.(2003) modified

3 - Results and discussion

10The compilation presented here (tab. 2; fig. 3) is representative of available well-dated molluscan data for the Weichselian Upper Pleniglacial. Weichselian Lower and Middle Pleniglacial samples have been removed. Weichselian/Würmian samples from old studies, without more precise chronological and stratigraphic information have also been removed. Except for samples analyzed by Mazenot and by Dubar in several studies performed in the Rhône Valley and in southeastern France, many of the removed sites were located in the same geographical areas than selected sites. Furthermore, the removed data often include only a single sample, which thus reduces the importance of their absence.

11The geographical distribution of selected sites is mainly dependent on the position of both natural exposures and brickearth quarries exploiting loess, which are often located along large fluvial systems, where deposits are particularly thick as they are closed to

Tab. 2: Sites that yielded molluscan data attributed to the Weichselian Upper Pleniglacial.

Tab. 2: Sites that yielded molluscan data attributed to the Weichselian Upper Pleniglacial.

.

Chronological data: AD = absolute dating; S = stratigraphy; UW and MW = Upper and Middle Weichselian

Fig.3: Location of selected Weichselian Upper Pleniglacial molluscan records (sites numbered according to the list presented in table 1).

Fig.3: Location of selected Weichselian Upper Pleniglacial molluscan records (sites numbered according to the list presented in table 1).

Many of these records are associated with brickearth quarries located in the thickest loess deposits, i.e. often along major fluvial systems. Indeed, fluvial systems provided large quantities of mineral particles to be transported and deposited by the wind and to form thick loess deposits in surrounding areas.

3.1 - Age validation of selected molluscan records

121: Port-Morvan (Brittany, France) (Monnier & Van Vliet-Lanoë, 1986)

13The molluscan samples come from level 1 of the Port-Morvan sequence (Monnier & Van Vliet-Lanoë, 1986), which became later level 3 of the Sables‑d’Or–Les-Pins formation in the regional stratigraphy (Monnier & Bigot, 1987). The uppermost calcareous level of this formation, close to level 3 of Port Morvan, yields a TL age of 18,2 ± 2,5 ka BP in Nantois (France) (Loyer et al., 1995).

142: Ot-Ar-Villiec (Brittany, France) (Monnier, 1980)

15As in Port-Morvan, the molluscan sample comes from level 3 of the Sables‑d’Or‑Les-Pins formation (Monnier, pers. comm.).

163: Sangatte (Nord Pas-de-Calais, France) (Antoine, 1989)

17A Weichselian age was attributed to the molluscan sample of unit X on stratigraphic criteria (Antoine, 1989). I confirm this age with the comparison of later amino acid analyses (Bates, 1993) with those of the database of Moore (2002). According to a recent review of the regional stratigraphy (Antoine et al., 1998), this molluscan sample probably belongs to the Upper Pleniglacial (Antoine, pers. comm.).

184: Achenheim (Alsace, France) (Puisségur, 1978; Rousseau, 1987)

19According to the correlation of the Achenheim loess sequence (Heim et al., 1982) with marine isotopic stages (Rousseau & Puisségur, 1990), I selected all samples located above the level of large ice-wedges correlated with the Middle/Upper Pleniglacial transition. A focus on the last glaciation is presented in Locht et al. (2003). The molluscan data are those of Rousseau (1987), which includes data from Puisségur (1978).

205: Schiltigheim (Alsace, France) (Puisségur, 1976)

21According to Wernert (1957) who helped with the molluscan sampling, and to most of the people who worked in this area, this sequence was deposited during the Würm (Puisségur, 1965). As the only other chronological information is the discovery of Upper Palaeolithic artefacts at the base of the Upper Younger Loess in unit 11 (Puisségur, 1976), I selected only two samples in the overlying loess layer.

226: Reculver (South-East, England) (Preece, 1990)

23Luminescence dating performed on the loess that yields the molluscan sample provide an age range of 17-23 ka BP (Parks & Rendell, 1988; Preece, 1990).

247: Portelet (Channel Islands) (Rousseau & Keen, 1989)

25According to the correlation established between the geliflucted soil overlying the molluscan samples and the Nagelbeek horizon recorded in Normandy, Rousseau and Keen (1989) suggested that the age of the molluscan assemblages should be close to the Middle/Upper Weichselian boundary. The latest synthesis of the stratigraphy of Jersey Island was established after the re-examination of two long sedimentary records (Keen et al., 1996). Its comparison with the stratigraphy of Normandy supports the attribution of the loess formation that yielded molluscan assemblages to the Weichselian Upper Pleniglacial.

268: Sandy (East, England) (Gao et al., 1998)

27The two samples come from lenses of silt and organic deposits located in a formation of sand and gravels. A 14C analysis performed on plant detritus yielded an age of 29,250 +460 –420 years BP for the lowest lens (Gao et al., 1998). The Weichselian Upper Pleniglacial age of this sequence is also supported by stratigraphic correlations and biostratigraphical indicators (Gao et al., 1998).

289: Woolpack Farm (East, England) (Gao et al., 2000)

29The molluscan sample comes from a silt level bracketed by two gravel formations, i.e. Hemingford Member and St. Ives Member (Gao et al., 2000), which are respectively dated at 43-18 ka BP and 18-10 ka BP by 14C (Gao, 1997).

3010: Halling (South-East, England) (Kerney, 1971)

31According to Kerney (1971), molluscan assemblages from Halling cannot have an Early Weichselian age as they show a “purely glacial” character and lack of thermophilous species having survived from the previous interglacial period unlike other records from the Cambridgeshire area. An age between 13 and 28 ka BP does not seem possible to the author as the poverty of organic remains in northwestern Europe for this interval suggest harsh climatic and environmental conditions that does not fit with the development of enough vegetation to support such molluscan populations. Hence, he proposed an age between 55 and 28 ka BP and argued that the central abundance increase suggests an interstadial period similar in magnitude to that of Denekamp or Hengelo. However, it is not possible to give a more precise age to these samples due to the lack of absolute ages and to the disappearance of the site. Consequently, as it is the most precise record of a part of the last glaciation available in England and that at least the upper part of it may be of Weichselian Upper Pleniglacial age, all samples have been selected. Moreover, the composition of all samples being almost the same, the selection of the totality or just a part of them will not strongly influence eventual statistic calculation or interpretations.

3211: Petit Saule/Villiers-Adam; 12: Chamesson/Villiers‑Adam (Ile de France, France) (Limondin-Lozouet & Gauthier, 2003)

33According to the precise knowledge of the regional stratigraphic framework (Antoine et al., 1998) and to luminescence analyses that yield TL ages of 35,45 ± 3,7 ka BP at the top of the Saint‑Acheul soil complex and 23,5 ± 2,1 and 23,1 ± 2,1 ka BP for the uppermost loess unit above the Nagelbeek horizon (Locht et al., 2003), I select all samples located in the loess above the Saint-Acheul soil complex.

3413: Achenheim; 14: Riedisheim; 15: Sierentz; 16: Pfastatt; 17: Eguisheim; 60: Brunstatt; 61: Wittenheim; 62: Blaesheim; 63: Mothern; 64: Schleithal (Alsace, France) (Mazenot, 1963)

35The chronostratigraphy of all these sites is based on Briquet (1930), Franc de Ferrière (1937) and Wernert (1957). Franc de Ferrière and Wernert helped Mazenot to sample and to locate samples in the exposures. Mazenot (1963) mentions that these three authors almost agree on sedimentological units that were deposited during the last glaciation. In their synthesis about the stratigraphy of the Achenheim sequence, Heim et al (1982) mention that the uppermost loess layer, named Last Loess by Wernert and Upper Younger Loess by Franc de Ferrière, represents the same stratigraphic unit and they attribute it to the Upper Pleniglacial, as well as the upper part of the Lower Younger Loess. The lower part of this latter unit represents both Lower and Middle Pleniglacial (Heim et al., 1982). Consequently, I select only samples from the Upper Younger Loess as those from the Lower Younger Loess may be of Lower or Middle Pleniglacial age.

3618: Gräselberg/Wiesbaden; 19: Hainerberg/Wiesbaden (Hesse, Germany); 20: Michelsberg; 21: Wallertheim (Rhineland-Palatinate, Germany) (Remy, 1969)

37In the Gräselberg and Hainerberg profiles, the stratigraphy was described by Semmel (1968). In both sequences of Wiesbaden, I selected samples located above the Hainerberg soil, which is the local equivalent of the Lohne soil. In Wallertheim, the stratigraphy of Remy (1969) and those of previous studies (Schmidtgen & Wagner, 1929; Fauler, 1938) does not help to identify precisely Weichselian Upper Pleniglacial deposits. In the middle of the loess unit, Remy (1969) identified a volcanic tuff that he named “Kärlicher Tuff”. However, Zöller (1995) mentioned two volcanic tuffs in the Upper Würm, i.e. the Rambacher and the Eltviller tuffs, the true Kärlicher Tuff being much older, i.e. around 396 ± 20 ka BP. Given the absence of tuff in Middle and Lower Pleniglacial deposits of Wallertheim and the position above the Lohne soil of both tuffs, I selected only four samples located around the single represented tuff. In Michelsberg, only one sample has been selected, the six others being attributed to the Late Pleniglacial (Remy, 1969).

3822 : Brühl ; 23 : Hennef in Sieg ; 24 : Bonn ; 29 : Römlinghoven ; 30 : Rodderberg ; 31 : Mehlem (North Rhine-Westphalia, Germany) ; 25: Rhens ; 26 : Remagen ; 27 : Moselweiss ; 28 : Weitersburg ; 36 : Biebelnheim ; 37 : Arzheim (Rhineland‑Palatinate, Germany) ; 32 : Schiersteinerstrasse in Wiesbaden; 33 : Kriftel quarry in Wiesbaden; 34 : Klüter quarry in Eltville ; 35 : Schick quarry in Wallertheim (Hesse, Germany); 38 : Grossostheim (Bavaria, Germany); 39 : Kesselt in Western Maastricht (Flanders, Belgium) (Remy, 1968)

39The chronostratigraphy of each site (Gullentops, 1954; Paas, 1962; Remy & Paas, 1959; Remy, 1960; Remy, 1968; Juvigné, 1996) is in agreement with modern concepts. All samples attributed to the Upper Würmian have thus been selected.

4040: Bötzingen (Baden-Württemberg, Germany) (Münzing, 1969)

41The upper loess formation was attributed to the Weichselian on a stratigraphic basis (Khodary Eissa, 1968). In the absence of more precise chronological information and according to the three-fold structure of this loess, I select only samples from the uppermost loess unit.

4241: Maisières-Canal (Wallonia, Belgium) (de Coninck, 1973)

43The stratigraphy of this site has been precisely described in Haesaerts (1978). A 14C age of 27,965 years BP has been obtained for the archaeological level including molluscan sample DC, and a 14C age of 30,780 years BP has been obtained for the basal humic soil of the sequence. According to Haesaerts (1985), this sequence is younger than the Les Vaux soil. All samples have thus been selected.

4442: Am Biedensteg/Bad Wildungen (Hesse, Germany) (Jacobshagen, 1963)

45The whole fauna indicates a Weichselian age for this two-fold loess sequence. In the absence of more precise chronological information, I selected only two samples from the uppermost loess unit attributed to the Upper Weichselian on the basis of the stratigraphy.

4643: Bad Kösen (Thuringia, Germany) (Mania & Altermann, 1970)

47The upper loess formation has been attributed to the Weichselian on the basis of a synthesis of the regional stratigraphy (Ruske & Wünsche, 1961). The occurrence of a weak soil formation distinguishes a lower loess unit with stratified and reworked structures and an upper eolian loess unit slightly or not perturbed (Mania & Altermann, 1970). A parallel made by the authors between this weak soil and the Stillfried B soil synchronous with the Lohne soil led me to select only samples from the upper loess unit.

4846: Böckingen/Heilbronn (Baden-Württemberg, Germany) (Rähle, 2004)

49According to the precise stratigraphy established by Bibus (2002), I selected all samples located above the Lohne soil.

5047: Schwalbenberg in Remagen (Rhineland-Palatinate, Germany) (Schiermeyer, 2000)

51The stratigraphic framework was established by Schirmer (1995). Schirmer (2000) then proposed a correlation between the Sinzig soil complex and interstadials IS-5 to IS-8 of Greenland ice-cores. This correlation is supported by 14C ages from the upper part of the Sinzig complex and which yielded ages of 27,890 ± 440 and 28,080 ± 530 years BP (App et al., 1987). Furthermore, unpublished TL ages from the Sinzig complex are around 30 ka BP (Schirmer, 2000). The upper part of the Sinzig soil complex also provided archaeological artefacts attributed to the Middle-to‑Upper‑Palaeolithic transition (Schirmer, 2000). Schirmer (2000) stated that the correlation between one of the three soils of the Sinzing complex with the Lohne soil upstream in the Rhine valley cannot be directly established. However, he mentioned that the lowest one, i.e. Sinzig soil 1, is also the most developed. According to the correlation established between the Lohne soil in Nussloch and the interstade 8 in GRIP (Antoine et al., 2001; Moine, 2003; Rousseau et al., 2002), the Sinzig soil 1 would be synchronous with the Lohne soil. Consequently, I selected molluscan samples located above the Sinzig soil 1.

5248: Nauberg; 49: Jahna-Aue; 50: Klosterbuch; 51: Golzern (Saxony, Germany) (Fuhrmann, 1973)

53In these Late Weichselian-Holocene sequences, the base of molluscan records show a continuous transition from glacial to interglacial conditions characterised by the progressive appearance of new species. The absence of significant gaps suggests that underlying deposits belong to the Upper Weichselian rather than to a previous glaciation or another glacial period. Consequently, I selected only the basal sample in each of these sequences.

5452: Nördlingen (Bavaria, Germany) (Hollaus, 1969)

55According to the stratigraphic framework of Würmian deposits in the area (Brunnacker, 1957), I selected only samples from the uppermost loess units in absence of other chronological information.

5653: Gönnersdorf, Neuwied (Rhineland-Palatinate, Germany) (Brunnacker et al., 1978)

57At this archaeological site, selected samples bracket the Eltviller Tuff, which was dated in Nussloch at 19,5 ± 2,3 and 19,2 ± 1,7 ka BP by OSL (Lang et al., 2003) and at 21,131-22,258 years cor. BP by 14C (Hatté et al., 2001).

5854: Wischlburg; 55: Schambach; 56: Niederwinkling; 57: Strasskirchen; 58: Pfelling (Bavaria, Germany) (Brunnacker & Brunnacker, 1956)

59The regional stratigraphy and the different facies of the Würmian loess in the area are well described by Brunnacker (1954; 1956). Full glacial deposits are generally made of two loess units separated by a tundra soil. In absence of more precise chronological information for this tundra soil, I selected only samples from the upper loess.

6059: Beckford (South-West, England) (Briggs etal., 1975)

61Selected molluscan samples come from a black silt layer including wood remains that yielded a 14C age of 27,650 ± 250 years BP.

6265: Wallstadt; 66: Grenzhof (Baden-Württemberg, Germany) (Münzing, 1985)

63In Grenzhof, wood remains located below the two upper most molluscan samples yielded 14C ages between 37 and 45 ka BP. I selected only the uppermost sample to be sure of its Weichselian Upper Pleniglacial age. In Wallstadt, I selected samples located between 14C ages of 27,080 ± 510 and 30,860 ± 500 years BP obtained on wood remains (Löscher et al., 1980).

6445: Plinz; 67: Mücheln; 68: Ascherslebener See (SaxonyAnhalt, Germany) (Mania & Stechemesser, 1969)

65The basal sample of the Late Weichselian-Holocene record of Ascherslebener See reflects full glacial conditions. According to 14C analyses (Mania & Stechemesser, 1970), it probably belongs to the Weichselian Upper Pleniglacial, and has thus been selected. In absence of other chronological information, the presence of an ice-cap in the region of Plinz and Mücheln during the Saalian glaciation (Grahmann, 1932) suggests a Weichselian age for loess formations underlying these Late Weichselian-Holocene sequences. As in Ascherslebener See, I thus selected the basal sample, characterizing full glacial conditions.

6644: Krumpa; 69: Möckerling (Saxony-Anhalt, Germany) (Mania et al., 1993)

67For these two Late Weichselian-Holocene sequences located in the same valley as Plinz and Mücheln, only the presence of the ice cap in the area during the Saalian glaciation suggests that underlying loess has a Weichselian Upper Pleniglacial age. I thus selected the basal sample of each sequence.

6870: Nussloch (Baden-Württemberg, Germany) (Moine, 2003)

69The Upper Weichselian molluscan record in Nussloch (Moine et al., submitted) is clearly identified at this site on the basis of precise stratigraphic data and numerous TL, OSL and 14C ages (Antoine et al., 2001; Hatté et al., 2001; Lang et al., 2003) as previously described in Data and Methods.

7071: Ascherslebener See (Saxony-Anhalt, Germany) (Mania, 1967)

71In this sequence, 14C ages on wood remains are : 11,300 ± 280, 10,940  ± 190 and 10,570 ± 180 years BP from the basis to the top of unit VII, 23,050 ± 750 years BP; for unit V, and 30,550 ± 2,600 years BP for unit IV (Mania & Stechemesser, 1970). According to these ages, I selected only samples from units V and VI that should belong to the Weichselian Upper Pleniglacial.

7272: Tancarville; 73: Gonfreville (Upper Normandy, France) (Lautridou, 1968, 1985)

73The single selected sample of each site is located above the Nagelbeek horizon.

7474: Rouelles (Lower Normandy, France) (Lechevalier, 1975)

75The single sample mentioned by Lechevalier (1975) belongs to the Lower Younger Loess according to Lautridou (1985).

7675: Mesnil-Esnard; 76: Roumare; 77: Epouville (Upper Normandy, France); 78 : Bréau ; 79 : Sergines (Burgundy, France) (Lautridou, 1985)

77At Mesnil-Esnard, Roumare and Epouville, the single selected sample or each site is located in and above the Mesnil-Esnard soil. At Bréau and Sergines, I selected samples from the Recent Loess.

7880: Luc-sur-Mer (Lower Normandy, France) (Coutard et al., 1970)

79The selected sample is located in a level of calcareous silt equivalent to the Lower Recent Loess (Lautridou, pers. comm).

3.2 - Representativeness and potential of molluscan data

80The second map (fig. 4) shows the distribution of molluscan records and the number of samples per site. The structure of the 80-site database (number of site number of samples per site) is as follows: 46-1; 14-2; 63; 3-4; 2-5; 1-7; 7-10/30; 1-96. With only eight sites including more than ten samples and only two 4-m thick records, the potential of terrestrial mollusc fauna is definitely underexploited in the reconstruction of millennial-timescale palaeoenvironmental changes. Indeed, according to both extent and thickness of loess deposits (Grahmann, 1932; Fink, 1969; Catt, 1985, Haesaerts, 1985; Frechen et al., 2003; Haase et al., 2007), if 2-to-9-m-thick loess sequences are sampled continuously every 5 cm for the 35-15 ka BP time span, molluscan records would have an average time resolution of 500-to-111-years per sample, which is enough to characterise the impact of millennial-timescale environmental changes. Among all compiled Weichselian Upper Pleniglacial records, only the Nussloch record fits these requirements. The study of more sequences is thus needed to fill in geographical gaps in loess areas (fig. 5) and to develop a network of high resolution molluscan sequences to tackle millennial-timescale environmental changes in the European Great Plain. For the Lower and Middle Weichselian Pleniglacial, even fewer molluscan data are presently available or can be precisely dated, but several loess sequences could also be sampled for mollusc shells at high-resolution, such as at Mainz-Weisenau (Bibus et al., 2002) and Nussloch (Moine et al., 2005).

Fig.4: Number of molluscan samples available at selected sites.

Fig.4: Number of molluscan samples available at selected sites.

Sites coloured in grey include ten or more samples, and represent only 10% of the sites. There construction of Weichselian Upper Pleniglacial palaeoenvironmental changes on the basis of terrestrial mollusc assemblages is thus strongly limited by available data.

Fig.5: Location of Weichselian Upper Pleniglacial molluscan records and contours of loess depositareas.

Fig.5: Location of Weichselian Upper Pleniglacial molluscan records and contours of loess depositareas.

See Catt (1985) and Haase et al. (2007) for more precise legends about loess types and thickness in England and continental Europe respectively.

3.3 - Palaeoenvironmental information

81As a first approximation, the Weichselian Upper Pleniglacial was considered as a single entity without subdivisions due to the heterogeneity of available data for this time interval. The composition of West-European molluscan populations shows a distinct opposition between a “western domain” surrounding the Channel and extending to eastern Belgium, which includes only one to five taxa of the following group (Columella columella, Pupilla muscorum, Succinea oblonga, Trichia hispida, slugs), and a “central domain” located around the Rhine Valley and extending to the East of Germany, which includes a larger pool of 39 taxa (fig. 6).

82In a study of the relationship between loess formation and associated molluscan populations from glacial times, including less data but spread all over the Great Plain, Ložek (1965) mentioned a general homogeneity of glacial malacofaunas from France to Ukraine, but even then noted regional differences in their composition. He differentiated three types of assemblages based on taxa presence/absence and relative abundances (see Ložek (1990) for their precise description): the Columella-fauna, the Pupilla-fauna and the Helicopsis striata-fauna. In this order, they reflect a gradient from cold-humid to cold-dry conditions. The composition of the malacofauna can shift gradually in space or time from one type of fauna to another depending on regional and continental climatic and environmental changes.

83According to assemblage types defined by Ložek (1990), the “western domain” is characterised by poor Columella-faunas and poor malacofaunas including only core species of loess assemblages, whereas Columella-faunas, Pupilla-faunas, and intermediate transitional faunas, mainly occur in the “central domain”. The more contrasted topography of the “central domain” has probably benefited the persistence of diversified and more vegetated microenvironments and of a richer diversity of taxa besides the core species Pupilla muscorum, Succinea oblonga and Trichia hispida, which are common in the whole studied area, and live now over most of the temperate zone of Eurasia.

84Ložek characterised several large biogeographical domains at the scale of Europe, and at the regional scale for Czech Republic, Slovakia and surroundings areas. However, geographical taxonomic distributions are rarely discussed for given time intervals, except for several taxa presenting a particular biostratigraphical interest. Ložek (1972) only mentioned a certain resemblance between poor malacofaunas from France and those from humid loess areas in Central Europe. Later, Rousseau et al. (1990) analysed a set of molluscan data from the last glaciation for Western and Central Europe, including newer data for France, and compared them with both periglacial features of loess deposits and climatic modelling results. They concluded (1) that the “western domain” was characterised by thick permafrost and increased cloudiness, atmospheric moisture and precipitation, and (2) that the composition of molluscan populations reflects a climatic gradient between oceanic conditions around the Channel and continental conditions in Central Europe.

85First, the four species identified for Weichselian Upper Pleniglacial loess deposits of the “western domain” are characteristic of cold, humid and poorly vegetated environments with either a mosaic aspect or a seasonal shift of environmental conditions, according to slightly different ecological preferences (compiled from several atlases) and optimal life temperature ranges (Sümegi, 2005) of the taxa: Columella columella (cold, humid, vegetated, 5-15oC); Pupilla muscorum (open, dry-humid, sunny, 10-22oC); Succinea oblonga (open, humid-swampy, 13-19oC); and Trichia hispida (everywhere except too dry, 10-20oC). Nevertheless, optimal life temperature ranges from Russian material and data must be considered with caution since geographical distributions of species in the former USSR (Likharev & Rammel’meier, 1962) are still not well constrained due to sampling gaps and to the use, for a long time, of a different taxonomic system than used in Europe. Optimal life temperature ranges given in Sümegi (2005) are originally based on Russian material identified with the European taxonomic system (Sümegi, 1989).

86Second, according to Murton & Lautridou (2003), the mapping of permafrost distribution during the Weichselian is limited by the precise dating of periglacial structures, the climatic instability, the lack of data, and the palaeoclimatic significance of many periglacial structures. This led to the realisation of many different permafrost distribution maps in the last fifty years (Poser, 1948; Kaiser, 1960; Maarleveld, 1976; Velichko, 1982 (all four redrawn in Vandenberghe & Pissart (1993), Van Vliet-Lanoë, 1989; Huijzer & Vandenberghe, 1998; Van Vliet-Lanoë & Hallégouët, 1998; Renssen & Vandenberghe, 2003). A comparison has thus been attempted with the geographical distribution of Last Glacial Maximum ice-wedge casts, which are used as periglacial indicators of the presence of permafrost (Karte, 1987; Van Vliet-Lanoë & Hallégouët, 1998). Most of the malacological “western domain” is included within the area of highest density of icewedge casts and ice-rich loess deposits (fig. 7). The correspondence might have been even better if the site 42, located north-eastward of the Middle Rhine Valley (fig. 3), and including a lower sample with Pupilla muscorum, Succinea oblonga and slugs, and an upper sample with only Pupilla loessica, had also been considered as representative of the “western domain”. Furthermore, modern observations show that the seasonal thawing of an ice-rich permafrost causes large water releases that cannot always be used by the vegetation due to low temperature and high amounts of organic solutes (Pruitt, 1978). The thawing also disturbs the uppermost soil layer and perturbs vegetation by shifting the root zone (Shur et al., 2003). Moreover, if runoff is weak, waterlogging may take place, which limits vegetation development and enhance the thawing itself by warming the permafrost.

87The link between poor malacofaunas and the presence of permafrost in the “western domain” proposed by Rousseau et al. (1990) is thus confirmed for the Weichselian Upper Pleniglacial, as well as cold, poorly vegetated and more humid environmental conditions than in the “central domain”. Our new dataset, enriched in German molluscan records, also indicates the presence of poor molluscan samples in Bavaria (sites 53 to 58), in Saxony (sites 49 to 50), and also in the Rhine Valley, which are generally ice-poor loess areas, which poses the question of the limits between both biogeographical domains. Indeed, whereas rich malacofauna are absent from the “western domain”, poor westernlike malacofauna occurred in the “central domain”, mainly in low-elevation regions and at the northern edge of the German plateau region. On the one hand, the survival of the same most tolerant species as in the “western domain” may be due either to the predominant influence of the regionally flat topography on the loess ice content or to a locally higher loess ice content due to regional climatic conditions. Damp loesses from marginal zones of loess deposition are indeed often characterised by poor Columella-faunas, especially during the Weichselian Upper Pleniglacial (Ložek, 1990). On the other hand, these conditions may have also been temporary, but as most of the records are only made of a few samples, composition changes of the malacofauna during the Weichselian Upper

88Pleniglacial are poorly documented at many sites. Indeed, Rousseau et al. (1990) remarks that for each of the last four glaciations, molluscan populations at the loess section of Achenheim (Alsace, France) resembles either the poor malacofauna of the “western domain”, or the rich ones of the “central domain”. They concluded for the loessic domain (1) that changes in the position of the glacial climatic gradient probably accompanied changes in the extent of both Alpine and Scandinavian ice-sheets, and (2) that if the occurrence of pleniglacial malacofaunas was limited by low temperatures, their regional composition changes mainly resulted from different precipitation regimes.

89According to this result, it can be envisaged that occurrences of poor malacofauna in the “central domain” might also result from changes in the climatic gradient, and particularly from an eastward expansion of oceanic climatic conditions. Whereas Rousseau et al. (1990) highlighted such changes between successive glaciations, our future objectives will be to look for changes occurring within the last glaciation, and even, within the Weichselian Upper Pleniglacial. The position of ice-wedge casts in regional stratigraphic frameworks for the Weichselian Upper Pleniglacial also reflects temporary occurrences rather a permanent presence during this period, even in the “western domain”, which implies associated climatic changes (Lautridou & Sommé, 1981; Karte, 1987). However, even if the precise stratigraphic position of these ice-wedge casts is known, the reconstruction of the dynamics of environmental domains in response to Weichselian Upper Pleniglacial millennial-timescale climatic changes is still precluded by the quantity of data available per site. Only the Nussloch molluscan record has indeed a sufficient resolution to look for millennial-timescale environmental changes (Moine, 2003; Moine et al., 2002, 2005, accepted). Consequently, new high-resolution molluscan records are required in Western and Central Europe and must be analysed in parallel with sedimentological, lithological and periglacial features to better constrain the composition, the distribution, and the dynamics of biogeographical domains, and to determine and reconstruct the evolution of the most influential environmental and climatic factors.

Fig.6: Location of Weichselian Upper Pleniglacial molluscan records and number of taxa per site.

Fig.6: Location of Weichselian Upper Pleniglacial molluscan records and number of taxa per site.

White-coloured sites include taxa of the first group. Most of these sites are located around the Channel, except several ones located in the Rhine and Danube valleys, and in Eastern Germany. Grey‑coloured sites include taxa of the second group. These sites are mainly located in Germany and in the East of France, except a few ones located in the Parisian region and in Burgundy. The more contrasted topography of the central domain may explain the persistence of differentiated microenvironments and of a larger pool of taxa.

Fig. 7: Geographical distributions of types of molluscan assemblages defined for the Weichselian Upper Pleniglacial molluscan records (fig. 6) and of Last Glacial Maximum ice-wedge casts (black triangle) and isolated ice-wedges (white triangle) after Van Vliet-Lanoë & Hallégouët (1998) and Karte (1987).

Fig. 7: Geographical distributions of types of molluscan assemblages defined for the Weichselian Upper Pleniglacial molluscan records (fig. 6) and of Last Glacial Maximum ice-wedge casts (black triangle) and isolated ice-wedges (white triangle) after Van Vliet-Lanoë & Hallégouët (1998) and Karte (1987).

Annotations about loess ice content after Brunnacker (1958) for Franconia and Bavaria, Lieberoth (1963) for Saxony and Semmel (1968) for Hesse. The poor molluscan assemblages of the “western domain” (dashed line) are mainly located in areas of high ice content and ice-wedge density in loess (solid line).

4 - Conclusion

90The compilation of a regional database of molluscan records has been initiated to study the distribution of the vegetation cover in the European Great Plain and to fill in gaps of palynological records. This first step was focused on the Weichselian Upper Pleniglacial of Western Europe for which literature was easier to find and to use. With the selection phase accomplished, the analysis of the selected dataset shows that less than 10% of the 80 compiled molluscan records may be useful to study millennial-timescale environmental changes. According to both extent and thickness of shell-bearing loess deposits, the potential of terrestrial malacofauna as a palaeoenvironmental proxy appears to be underexploited. The extension of the molluscan records data base to Central and Eastern Europe and the analysis at high resolution of new molluscan records, as in Nussloch (Moine, 2003), will thus improve our knowledge of millennial-timescale environmental changes in the European Great Plain.

91This first analysis of the dataset already shows the existence of two domains. The first one located in northwestern Europe is characterised by poor malacofauna reflecting a cold, humid and poorly vegetated environment developed on an ice-rich permafrost in a flat lowland region, whereas the second one located in western Germany is characterised by richer malacofauna reflecting a more vegetated environment developed on an ice-poor permafrost in a topographycally more contrasted region. The future analysis of new records will allow a more precise definition of environmental domains in the European Great Plain and the study of their evolution and dynamics through time as already suggested by Ložek (1972). A better understanding of the local and regional ecological values of the taxa is also expected from such a geographical approach of European glacial malacofauna. It will be help ful for the palaeoenvironmental interpretation of molluscan records and provide new reconstructions to be discussed with LGM modelling results and the distribution of Palaeolithic human populations through comparisons with archaeological data and the remains of large mammal faunas.

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Bibliographie

ALFANO M.J., BARRON E.J., POLLARD D., HUNTLEY B., & ALLEN J.R.M., 2003 - Comparison of climate model results with European vegetation and permafrost during oxygen isotope stage three. Quaternary Research, 59, 97-107.

ALLEN J.R.M., BRANDT U., BRAUER A., HUBBERTEN H.W., HUNTLEY B., KELLER J., KRAML M., MACKENSEN A., MINGRAM J., NEGENDANK J.F.W., NOWACZYK N.R., OBERHÄNSLI H., WULF S., & ZOLITSCHKA B., 1999 - Rapid environmental changes in southern Europe during the last glacial period. Nature, 400, 740-743.

ALLEN J.R.M., WATTS W.A., & HUNTLEY B., 2000 - Weichselian palynostratigraphy, palaeovegetation and palaeoenvironment: the record from Lago Grande di Monticchio, southern Italy. Quaternary International, 73/74, 91-110.

ALLEN J.R.M., & HUNTLEY B., 2000 - Weichselian palynological records from southern Europe: correlation and chronology. Quaternary International, 73/74, 111-125.

ANTOINE P., 1989 - Stratigraphie des formations pléistocènes de Sangatte (Pas de Calais), d’après les premiers travaux du tunnel sous la Manche. Bulletin de l’Association Française pour l’Etude du Quaternaire, 37 (1), 5-17.

ANTOINE P., 1991 - Nouvelles données sur la stratigraphie du Pléistocène supérieur de la France septentrionale, d’après les sondages effectués sur le tracé du TGV Nord. Publications du Centre d’Etudes et de Recherches de l’Université de Lille, 3, 9-20.

ANTOINE P., AUGUSTE P., BAHAIN J.-J., COUDRET P., DEPAEPE P., FAGNART J.-P., FALGUÈRES C., FONTUGNE M., FRECHEN M., HATTÉ C., LAMOTTE A., LAURENT M., LIMONDIN-LOZOUET N., LOCHT J.-L., MERCIER H., MOIGNE A.-M., MUNAUT A.-V., PONEL P., & ROUSSEAU D.-D., 2003 - Paléoenvironnements pléistocènes et peuplements paléolithiques dans le bassin de la Somme (nord de la France). Bulletin de la Société Préhistorique Française, 100, 5-28.

ANTOINE P., CATT J., LAUTRIDOU J.-P., & SOMMÉ J., 2003 - The loess and coversands of northern France and Southern England. Journal of Quaternary Science, 18, 309-318.

ANTOINE P., LAUTRIDOU J.-P., SOMMÉ J., AUGUSTE P., AUFFRET J.-P., BAIZE S., CLET-PELLERIN M., COUTARD J.-P., DEWOLF Y., DUGUÉ O., JOLY F., LAIGNEL B., LAURENT M., LAVOLLÉ M., LEBRET P., LEFEBVRE D., LÉCOLLE F., LIMONDIN-LOZOUET N., MUNAUT A.-V., OZOUF J.-C., QUESNEL F., & ROUSSEAU D.-D., 1998 - Les formations quaternaires de la France du Nord Ouest : limites et corrélations. Quaternaire, 9 (3), 227-241.

ANTOINE P., ROUSSEAU D.-D., ZÖLLER L., LANG A., MUNAUT A.-V., HATTÉ C., & FONTUGNE M., 2001 - Highresolution record of the last Interglacial-glacial cycle in the Nussloch loess-paleosol sequences, Upper Rhine Area, Germany. Quaternary International, 76/77, 211-229.

BATES M., 1993 - Quaternary aminostratigraphy in Northwestern France. Quaternary Science Review, 12 (9), 793-809.

BEHRE K.-E., & VAN DER PLICHT J., 1992 - Towards an absolute chronology for the last glacial period in Europe: radiocarbon dates from Oerel, northern Germany. Vegetation History and Archaeobotany, 1, 111-117.

BIBUS E., 2002 - Zum Quartär im mittleren Neckarraum, Reliefentwicklung, Löß/Paläobodensequenzen, Paläoklima. Tübinger Geowissenschaftliche Arbeiten, Reihe D, 8, 1-236.

BIBUS E., RÄHLE W., & WEDEL J., 2002 - Profilbau, Molluskenführungen und parallelisierungs möglichkeiten des Altwürmabschnitts im Lössprofil Mainz-Weisenau. Eiszeitalter und Gegenwart, 51, 1-14.

BOCQUET-APPEL J.-P., & DEMARS P.-Y., 2000a - Neanderthal contraction and modern human colonization of Europe. Antiquity, 74, 544-552.

BOCQUET-APPEL J.-P., & DEMARS P.-Y., 2000b - Population Kinetics in the Upper Palaeolithic in Western Europe. Journal of Archaeological Science, 27, 551-570.

BOCQUET-APPEL J.-P., DEMARS P.-Y., NOIRET L., & DOBROWSKY D., 2005 - Estimates of Upper Palaeolithic metapopulation size in Europe from archaeological data. Journal of Archaeological Science, 32, 1656-1668.

BRACONNOT P., OTTO-BLIESNER B., HARRISON S., JOUSSAUME S., PETERCHMITT J.-Y., ABE-OUCHI A., CRUCIFIX M., DRIESSCHAERT E., FICHEFET T., HEWITT C.D., KAGEYAMA M., KITOH A., LAÎNÉ A., LOUTRE M.-F., MARTI O., MERKEL U., RAMSTEIN G., VALDES P., WEBER S.L., YU Y., & ZHAO Y., 2007a - Results of PMIP2 coupled simulations of the Mid-Holocene and Last Glacial Maximum - Part 1: experiments and large-scale features. Climate of the Past, 3, 261-277.

BRACONNOT P., OTTO-BLIESNER B., HARRISON S., JOUSSAUME S., PETERCHMITT J.-Y., ABE-OUCHI A., CRUCIFIX M., DRIESSCHAERT E., FICHEFET T., HEWITT C.D., KAGEYAMA M., KITOH A., LOUTRE M.-F., MARTI O., MERKEL U., RAMSTEIN G., VALDES P., WEBER S.L., YU Y., & ZHAO Y., 2007b - Results of PMIP2 coupled simulations of the Mid-Holocene and Last Glacial Maximum - Part 2: feedbacks with emphasis on the location of the ITCZ and mid- and high latitudes heat budget. Climate of the Past, 3, 279-296.

BRIGGS D.J., COOPE G.R., & GILBERTSON D.D., 1975 - Late Pleistocene terrace deposits at Beckford, Worcestershire, England. Geological Journal, 10, 1-16.

BRIQUET A., 1930 - Le Quaternaire de l’Alsace. Bulletin de la Société Géologique de France, 30 (4ème série), 977-1014.

BRUNNACKER K., 1954 - Löß und diluviale Bodenbildungen in Südbayern. Eiszeitalter und Gegenwart, 4/5, 83-86.

BRUNNACKER K., 1955 - Geologische Karte von Bayern 1:25000 Blatt Nr. 7142 Straßkirchen mit Erläuterungen.

BRUNNACKER K., 1956 - Regionale Bodendifferenzierungen während der Würmeiszeit. Eiszeitalter und Gegenwart, 7, 43-48.

BRUNNACKER K., 1957 - Die Geschichte der Böden im jüngeren Pleistozän in Bayern. Geologica Bavarica, 34, 1-95.

BRUNNACKER M., & BRUNNACKER K., 1956 - Die Molluskenfauna einiger Lößprofile im Donautal. Geologische Blätter für Nordost-Bayern und Angrenzende Gebiete, 6, 91-100.

BRUNNACKER K., BRUNNACKER M., KOCI A., LEROIGOURHAN A., & PUISSÉGUR J.-J., 1978 - Stratigraphie im Bereich der Gönnersdorfer Siedlung. In K. Brunnacker (ed.), Der Magdalénien Fundplatz Gönnersdorf. 4. Geowissenschaftliche Untersuchungen in Gönnersdorf. Franz Steiner, Wiesbaden, 3564.

CASPERS G., & FREUND H., 2001 - Vegetation and climate in the Early- and Pleni‑Weichselian in Northern Central Europe. Journal of Quaternary Science, 16, 31-48.

CATT J.A., 1985 - Soil particle size distribution and mineralogy as indicators of pedogenic history: examples from the loessial soils of England and Wales. In K.S. Richards, R.R. Arnett & S. Ellis (eds.), Geomorphology and Soils. Allen and Unwin, London, 202-218.

COUTARD J.-P., HELLUIN M., LAUTRIDOU J.-P., OZOUF J.-C., & PELLERIN J., 1970 - Les lœss de la campagne de Caen. Bulletin du Centre de Géormophologie de Caen, 8, 1-30.

DANSGAARD W., JOHNSEN S.J., CLAUSEN H.B., DAHLJENSEN D., GUNDESTRUP N.S., HAMMER C.U., HVIDBERG C.S., STEFFENSEN J.P., SVEINBJÖRNSDOTTIR A.E., JOUZEL J., & BOND G., 1993 - Evidence for general instability of past climate from a 250-kyr ice-core record. Nature, 364, 218220.

DE CONINCK J., 1973 - La faune du site paléolithique de Maisières-Canal. Mollusques fossiles. Mémoires - Institut Royal des Sciences Naturelles de Belgique, 172, 23-28.

DEMARS P.-Y., 2002 - Changements climatiques et occupation de l’espace. Les derniers chasseurs‑cueilleurs d’Europe face à la déglaciation. Quaternaire, 13, 289-296.

DEMARS P.-Y., 2006 - L’occupation de l’Europe par les chasseurs du Paléolithique supérieur : une question de climat. Mappemonde, 83, 1-12.

FINK J. (ed.), 1969 - La stratigraphie des lœss d’Europe. Bulletin de l’Association Française pour l’Etude du Quaternaire, Supplément, 1-176.

FLOSS H., 2006 - Le Paléolithique supérieur en Allemagne méridionale (2001-2005). Études et Recherches Archéologiques de l’Université de Liège, 115, 71-80.

FRANC DE FERRIÈRE P.J.J., 1937 - Géologie et pédologie. Contribution à l’étude des formations quaternaires de la plaine d’Alsace. Thèse de Doctorat, Université de Strasbourg, 157 p.

FRECHEN M., 1999 - Upper Pleistocene loess stratigraphy in Southern Germany. Quaternary Geochronology, 18, 243-269.

FRECHEN M., OCHES E.A., & KOHFELD K.E., 2003 - Loess in Europe-mass accumulation rates during the Last Glacial period. Quaternary Science Review, 22, 1835-1857.

FUHRMANN R., 1973 - Die spätweichselglaziale und holozäne Molluskenfauna Mittel- und Westsachsens. Freiberger Forschungshefte, Reihe C, 278, 1-121.

GAO C., 1997 - Sedimentology and stratigraphy of the River Great Ouse, Southern England. Ph. D. thesis, University of Cambridge.

GAO C., COOPE G.R., KEEN D.H., & PETTIT M.E., 1998 - Middle Devensian deposits of the Ivel Valley at Sandy, Bedfordshire, England. Proceedings of the Geologists’ Association, 109, 127‑137.

GAO C., KEEN D.H., BOREHAM S., COOPE G.R., PETTIT E., STUART A.J., & GIBBARD P.L., 2000 - Last Interglacial and Devensian deposits of the River Great Ouse at Woolpack Farm, Fenstanton, Cambridgeshire, UK. Quaternary Science Review, 19 (8), 787-810.

GENTY D., BLAMART D., OUAHDI R., GILMOUR M., BAKER A., JOUZEL J., & VAN‑EXTER S., 2003 - Precise dating of Dansgaard-Oeschger climate oscillations in Western Europe from stalagmite data. Nature, 421, 833-837.

GRAHMANN R., 1932 - Der Löß in Europa. Mitteilungen der Gesellschaft für Erdkunde zu Leipzig, 51, 5-24.

GUIOT J., BEAULIEU J.-L. de, CHEDDADI R., DAVID F., PONEL P., & REILLE M., 1993 - The climate in Western Europe during the last Glacial/Interglacial cycle derived from pollen and insect remains. Palaeogeography, Palaeoclimatology, Palaeoecology, 103, 73-93.

GUITER F., ANDRIEU-PONEL V., BEAULIEU J.-L. de, CHEDDADI R., CALVEZ M., PONEL P., REILLE M., KELLER T., & GOEURY C., 2003 - The last climatic cycles in Western Europe: a comparison between long continuous lacustrine sequences from France and other terrestrial records. Quaternary International, 111, 59-74.

GULLENTOPS F., 1954 - Contributions à la chronologie du Pléistocène et des formes du relief en Belgique. Mémoires de l’Institut géologique de l’Université de Louvain, 18, 125-252.

HAASE D., FINK J., HAASE G., RUSKE R., PÉCSI M., RICHTER H., ALTERMANN M., & JÄGER K.-D., 2007 - Loess in Europe - its spatial distribution based on a European Loess Map, scale 1:2,500,000. Quaternary Science Reviews, 26, 13011312.

HAESAERTS P., 1978 - Contexte stratigraphique de quelques gisements paléolithiques de plein air de Moyenne Belgique. Bulletin de la Société royale belge d’Anthropologie et de Préhistoire, 89, 115‑133.

HAESAERTS P., 1985 - Les lœss du Pléistocène supérieur en Belgique ; comparaisons avec les séquences d’Europe centrale. Bulletin de l’Association Française pour l’Etude du Quaternaire, 2/3, 105-115.

HAESAERTS P., 1994 - Chronostratigraphie et environnement climatique du Paléolithique supérieur en Belgique. In F.B. de Quirós (ed.), El cuadro geochronologico del Paleolitico superior inicial. Ministerio de cultura, Altamira, 131-141.

HARGREAVES J.C., ABE-OUCHI A., & ANNAN J.D., 2007 - Linking glacial and future climates through an ensemble of GCM simulations. Climate of the Past, 3, 77-87.

HATTÉ C., ANTOINE P., FONTUGNE M., LANG A., ROUSSEAU D.-D., & ZÖLLER L., 2001 - d13C of loess organic matter as a potential proxy for paleoprecipitation. Quaternary Research, 55, 33-38.

HATTÉ C., PESSENDA L.-C., LANG A., & PATERNE M., 2001 - Development of accurate and reliable 14C chronologies for loess deposits: application to the loess sequence of Nussloch (Rhine valley, Germany). Radiocarbon, 43, 611-618.

HATTÉ C., & GUIOT J., 2005 - Palaeoprecipitation reconstruction by inverse modelling using the isotopic signal of loess organic matter: application to the Nußloch loess sequence (Rhine Valley, Germany). Climate Dynamics, 25, 315-327.

HEINRICH H., 1988 - Origin and consequences of cyclic ice rafting in the Northeast Atlantic Ocean during the past 130,000 years. Quaternary Research, 29, 142-152.

HOLLAUS E., 1969 - Geologische Untersuchungen im Ries. Das Gebiet der Blätter Nördlingen-Ost und Nördlingen-West, mit besonderer Berücksichtigung der Pleistozän-Ablagerungen. Doctoral thesis, Ludwig-Maximilian-Universität, München, 85 p.

HUIJZER B.S., & VANDENBERGHE J., 1998 - Climatic reconstruction of the Weichselian Pleniglacial in Northwestern and Central Europe. Journal of Quaternary Science, 13, 391-417.

HUNTLEY B., ALFANO M.J., ALLEN J.R.M., POLLARD D., TZEDAKIS P., BEAULIEU J.-L. de, GRÜGER E., & WATTS B., 2003 - European vegetation during Marine Oxygen Isotope Stage-3. Quaternary Research, 59, 195-212.

JACOBSHAGEN E., 1963 - Eine Faunenfolge aus dem jungpleistozänen Löß bei Bad Wildungen. 1. Die Faunen und ihre Bindung an Klima und Umwelt. Abhandlungen des Hessischen Landesamtes für Bodenforschung, 44, 5-92.

JOST A., LUNT D., KAGEYAMA M., ABE-OUCHI A., PEYRON O., VALDES P. J., & RAMSTEIN G., 2005 - High-resolution simulations of the last glacial maximum climate over Europe: a solution to discrepancies with continental palaeoclimatic reconstructions? Climate Dynamics, 24, 577-590.

JUVIGNÉ E., HAESAERTS P., MESTDAGH H, PISSART A., & BALESCU S., 1996 - Révision du stratotype lœssique de Kesselt (Limbourg, Belgique). Comptes-Rendus de l’Académie des Sciences, Paris, 323, 801-807.

KAGEYAMA M., LAINÉ A., ABE-OUCHI A., BRACONNOT P., CORTIJO E., CRUCIFIX M., DE VERNAL A., GUIOT J., HEWITT C., KITOH A., KUCERA M., MARTI O., OHGAITO R., OTTO-BLIESNER B., PELTIER W., ROSELL-MELÉ A., VETTORETTI G., WEBER S., YU Y., & MARGO Project Members, 2006 - Last Glacial Maximum temperatures over the North Atlantic, Europe and Western Siberia: a comparison between PMIP models, MARGO sea-surface temperatures and pollen-based reconstructions. Quaternary Science Reviews, 25, 2082‑2102.

KARTE J., 1987 - Pleistocene periglacial conditions and geomorphology in North Central Europe. In J. Boardman (ed.), Periglacial processes and landform in Britain and Ireland. Cambridge University Press, Cambridge, 67-75.

KEEN D.H., VAN VLIET-LANOË B., & LAUTRIDOU J.-P., 1996 - Two long sedimentary records from Jersey, Channel Islands: stratigraphic and pedological evidence for environmental change during the last 200 kyr. Quaternaire, 7, 3-13.

KERNEY M.P., CAMERON R.A.D., & JUNGBLUTH, J.H., 1983 - Die Landschnecken Nord und Mitteleuropas. P. Parey, Hamburg and Berlin, 384 p.

KHODARY EISSA O., 1968 - Feinstratigraphische und pedologische Untersuchungen an Lößaufschlüssen im Kaiserstuhl (Südbaden). Freiburger Bodenkundliche Abhandlungen, 2, 1-149.

LANG A., HATTÉ C., ROUSSEAU D.-D., ANTOINE P., FONTUGNE M., ZÖLLER L., & HAMBACH U., 2003 - High resolutions chronologies for loess: comparing AMS-14C and optical dating results. Quaternary Science Reviews, 22 (10/13), 953‑959.

LAUTRIDOU J.-P., 1968 - Les formations superficielles de Saint‑Romain (Pays de Caux). Leur contribution à l’étude morphologique de la région. Thèse de Doctorat, Association des Publications de la Faculté des Lettres et Sciences Humaines de l’Université de Caen, 199 p.

LAUTRIDOU J.-P., 1985 - Le cycle périglaciaire pléistocène en Europe du Nord-Ouest et plus particulièrement en Normandie. Thèse de Doctorat d’Etat, Université de Caen, 908 p.

LAUTRIDOU J.-P., & CLIQUET D., 2006 - Le Pléistocène supérieur de Normandie et peuplements paléolithiques. Quaternaire, 17, 187-206.

LAUTRIDOU J.-P., & SOMMÉ J., 1981 - L’extension des niveaux repères périglaciaires à grandes fentes de gel de la stratigraphie du Pléistocène récent dans la France du Nord-Ouest. Biuletyn Peryglacjalny, 28, 179-185.

LECHEVALLIER C., 1975 - Plateau, vallées et littoral du Caux occidental. Etude morphologique. Thèse de Doctorat, Université Nanterre-Paris X, 264 p.

LIKHAREV I.M., & RAMMEL’MEIER E.S., 1962 - Terrestrial mollusks of the fauna of the U.S.S.R. Oldbourne Press, Jerusalem, 574 p.

LIMONDIN-LOZOUET N., & GAUTHIER A., 2003 - Biocénoses pléistocènes des séquences lœssiques de Villiers-Adam (Val d’Oise, France) : études malacologiques et palynologiques. Quaternaire, 14 (4), 237-252.

LOCHT J.-L., ANTOINE P., BAHAIN J.-J., DWRILA G., RAYMOND P., LIMONDIN-LOZOUET N., GAUTHIER A., DEBENHAM N., FRECHEN M., ROUSSEAU D.-D., HATTÉ C., HAESAERTS P., & METSDAGH H., 2003 - Le gisement paléolithique moyen et les séquences pléistocènes de Villiers-Adam (Val d’Oise). Chronostratigraphie, environnements et implantations humaines. Gallia Préhistoire, 45, 1-111.

LOCHT J.-L., 2004 - Le gisement paléolithique moyen de Beauvais (Oise). Contribution à la connaissance des modalités de subsistance des chasseurs de Renne du Pléniglaciaire inférieur du Weichsélien. Thèse de Doctorat, Université des Sciences et Techniques de Lille, 328 p.

LÖSCHER M., BECKER B., BRUNS M., HIERONYMUS U., MÄUSBACHER R., MÜNNICH M., MÜNZING K., & SCHEDLER J., 1980 - Neue Ergebnisse über das Jungquartär im Neckarschwemmfächer bei Heidelberg. Eiszeitalter und Gegenwart, 30, 89-100.

LOYER S., VAN VLIET-LANOË B., MONNIER J.-L., HALLEGOUËT B., & MERCIER N., 1995 - La coupe de Nantois (Baie de Saint-Brieuc, France) : datations par thermoluminescence (TL) et données paléoenvironnementales nouvelles pour le Pléistocène de Bretagne. Quaternaire, 6 (1), 21‑33.

LOŽEK V., 1964 - Quartärmollusken der Tschechoslowakei. Rozpravy Ustredniho ustuvu geologického, 31, 1-374.

LOŽEK V., 1965 - Das Problem der Lößbildung und die Lößmollusken. Eiszeitalter und Gegenwart, 16, 61-75.

LOŽEK V., 1972 - Le lœss et les formations assimilées ; corrélation entre l’Europe Centrale et la France par la faune de Mollusques. In M. Ters (ed.), Etudes sur le Quaternaire dans le Monde. VIIIe congrès INQUA, Paris, 1969. Supplément au Bulletin de l’Association Française pour l’Etude du Quaternaire, NE4-1971, Vol.2. CNRS, Paris, 597-606.

LOŽEK V., 1990 - Molluscs in loess, their paleoecological significance and role in geochronology - Principles and methods. Quaternary International, 7/8, 71-79.

MAGNIN F., 1992 - Variations de température en Provence pendant le Pléistocène supérieur (stades isotopiques 2 et 3) estimées d’après l’analyse d’associations de gastéropodes terrestres. Comptes‑Rendus de l’Académie des Sciences, Paris, 315, 231-237.

MANIA D., 1967 - Das Jungquartär aus dem ehemaligen Ascherlebener See im Nordharzvorland. Petermanns Geographische Mitteilungen, 111 (4), 257-273.

MANIA D., & STECHEMESSER H., 1969 - Eine weichselspätglaziale Molluskensuksession aus dem mitteleuropäischen Periglazialgebiet südlich der Elbe und ihre Bedeutung für die Landschaftsgeschichte. Petermanns Geographische Mitteilungen, 113, 1-15.

MANIA D., & STECHEMESSER H., 1970 - Jungpleistozäne Klimazyklen im Harzvorland. Petermanns Geographische Mitteilungen, Ergänzungsheft, 274, 39-55.

MANIA D., & ALTERMANN M., 1970 - Zur Gliederung des Jungund Mittelpleistozäns im mittleren Saaletal bei Bad Kösen. Geologie, 19 (10), 1161-1184.

MANIA D., SEIFERT M., & THOMAE M., 1993 – Spät und Postglazial im Geiseltal (mittleres Elbe-Saalegebiet). Eiszeitalter und Gegenwart, 43, 1-22.

MAZENOT G., 1963 - Recherches malacologiques sur les lœss et les complexes lœssiques d’Alsace. Bulletin du Service de la carte géologique d’Alsace et de Lorraine, 16 (1), 3-69.

MEIJER T., 2006 - Bibliography on European Pliocene and Quaternary mollusca. WMC Kwartair Consultants, Palaeomal report, 18, 169 p.

MOINE O., 2003 - Analyse des changements rapides de l’environnement à l’aide des faunes de mollusques terrestres durant la dernière période glaciaire en domaine continental européen. Thèse de Doctorat, Université Montpellier 2, 260 p.

MOINE O., ROUSSEAU D.-D., & ANTOINE P., 2005 - Terrestrial molluscan records of Weichselian Lower to Middle Pleniglacial climatic changes from the Nussloch loess series (Rhine Valley, Germany): the impact of local factors. Boreas, 34, 363-380.

MOINE O., ROUSSEAU D.-D., & ANTOINE P., accepted - The impact of Dansgaard-Oeschger cycles on the loessic environment and malacofauna of Nussloch (Germany) during the Upper Weichselian. Quaternary Research.

MOINE O., ROUSSEAU D.-D., ANTOINE P., & HATTÉ C., 2002 - Mise en évidence d’événements climatiques rapides par les faunes de mollusques terrestres des lœss weichséliens de Nussloch (Allemagne). Quaternaire, 13, 209-217.

MOINE O., ROUSSEAU D.-D., JOLLY D., & VIANEY-LIAUD M., 2002 - Paleoclimatic reconstruction using Mutual Climatic Range method on terrestrial mollusks. Quaternary Research, 57, 162-172.

MONNIER J.-L., 1980 - Le Paléolithique de la Bretagne dans son cadre géologique. Thèse de Doctorat d’Etat, Université Rennes 1, 607 p.

MONNIER J.-L., & VAN VLIET-LANOË B., 1986 - Les oscillations climatiques entre 125000 ans et le maximum glaciaire d’après l’étude des coupes du littoral de la baie de St-Brieuc. Apport de la lithologie, de la pédologie et de la malacologie. Bulletin de l’Association Française pour l’Etude du Quaternaire, 25/26 (1-2), 119-126.

MONNIER J.-L., & BIGOT B., 1987 - Stratigraphie des dépôts pléistocènes du nord de la Bretagne (France). Les formations de Port-Morvan et de la Haute-Ville. Bulletin de l’Association Française pour l’Etude du Quaternaire, 30 (2), 93-103.

MOORE, K. M., 2002 - Aminostratigraphy of the Late Pleistocene loess of Europe. Master thesis, University of South Florida, Tampa, 89 p.

MÜLLER U.C., PROSS J., & BIBUS E., 2003 - Vegetation response to rapid climate change in Central Europe during the past 140,000 yr based on evidence from the Füramoos pollen record. Quaternary Research, 59, 235-245.

MÜNZING K., 1969 - Quartäre Molluskenfaunen aus dem Kaiserstuhl. Jahreshefte des Geologischen Landesamtes in Baden‑Württemberg, 11, 87-115.

MÜNZING K., & LÖSCHER M., 1985 - Jungquartäre Molluskenfaunen aus der Umgebung von Heidelberg. Jahreshefte des Geologischen Landesamtes in Baden-Württemberg, 27, 93-112.

MURTON J.B., & LAUTRIDOU J.-P., 2003 - Recent advances in the understanding of Quaternary periglacial features of the English Channel coastlands. Journal of Quaternary Science, 18, 301-307.

OTTE M., 1979 - Le Paléolithique supérieur ancien en Belgique. Musées royaux d’Art et d’Histoire : Monographies d’Archéologie Nationale, 5, 684 p.

OTTE M., 1984 - Le Paléolithique supérieur en Belgique. In D. Cahen & P. Haesaerts (eds), Peuples chasseurs de la Belgique préhistorique dans leur cadre naturel. Patrimoine de l’Institut royal des sciences naturelles de Belgique, Bruxelles, 157-179.

OTTE M., & NOIRET P., 2006 - Le Paléolithique supérieur de Belgique. Recherches 2001-2005. Études et Recherches Archéologiques de l’Université de Liège, 115, 81-84.

PAAS W., 1962 - Rezente und fossile Böden auf niederrheinischen Terrassen und deren Deckschichten. Eiszeitalter und Gegenwart, 12, 165-230.

PEYRON O., GUIOT J., CHEDDADI R., TARASOV P., REILLE M., BEAULIEU J.-L. de, BOTTEMA S., & ANDRIEU V., 1998 - Climatic reconstruction in Europe for 18,000 yr B.P. from pollen data. Quaternary Research, 49, 183-196.

PREECE R.C., 1990 - The molluscan fauna from Late Devensian loess from Reculver, Kent. Journal of Conchology, 33, 295-297.

PRENTICE I.C., HARRISON S.P., JOLLY D., & GUIOT J., 1998 - The climate and biomes of Europe at 6000 yr BP: comparison of model simulations and pollen-based reconstructions. Quaternary Science Reviews, 17, 659-668.

PREUSSER F., 2004 -Towards a chronology of the Late Pleistocene in the northern Alpine Foreland. Boreas, 33, 195-210.

PRUITT W.O., 1978 - Boreal ecology. Studies in Biology, 91, 1-73.

PUISSÉGUR J.-J., 1965 - La terrasse de Schiltigheim (Alsace). Etude stratigraphique et malacologique. Bulletin de l’Association Française pour l’Etude du Quaternaire, 2, 66-77.

PUISSÉGUR J.-J., 1976 - Mollusques continentaux quaternaires de Bourgogne. Significations stratigraphiques et climatiques. Rapports avec d’autres faunes boréales de France. Mémoires géologiques de l’Université de Dijon, 3, 1-241.

PUISSÉGUR J.-J., 1978 - Les mollusques des séries lœssiques à Achenheim. Recherches géographiques Strasbourg, 7, 71-96.

QUINIF Y., GENTY D., & MAIRE R., 1994 - Les spéléothèmes : un outil performant pour les études paléoclimatiques. Bulletin de la Société Géologique de France, 165, 603-612.

RÄHLE W., 2004 - Mollusken aus zwei bedeutenden mittel und jungpleistozänen Lößprofilen des mittleren Neckarraumes (Baden-Württemberg) und ihre ökologisch-stratigraphisch Aussage. Tübinger geowissenschaftliche Arbeiten, Reihe D, 10, 219-240.

REMY H., 1960 - Der Löß am unteren Mittel und Niederrhein. Eiszeitalter und Gegenwart, 11, 107‑120.

REMY H., 1968 - Zur Stratigraphie und Klimaentwicklung des jüngeren Pleistozäns in Mittel und Westeuropa unter besonder Berücksichtigung des Lösses. Decheniana, 121 (1/2), 121-145.

REMY H., 1969 - Würmzeitliche Molluskenfaunen aus Lößserien des Rheingauesund der nördlichen Rheinhessens. Notizblatt des Hessischen Landesamtes für Bodenforschung zu Wiesbaden, 97, 98‑116.

RENSSEN H., & VANDENBERGHE J., 2003 - Investigation of the relationship between permafrost distribution in NW Europe and extensive winter sea-ice cover in the North Atlantic Ocean during the cold phases of the Last Glaciation. Quaternary Science Reviews, 22, 209-223.

ROCHE D.M., DOKKEN T.M., GOOSSE H., RENSSEN H., & WEBER S.L., 2007 - Climate of the Last Glacial Maximum: sensitivity studies and model-data comparison with the LOVECLIM coupled model. Climate of the Past, 3, 205-224.

ROHLING E.J., MAYEWSKI P.A., & CHALLENOR P., 2003 - On the timing and mechanism of milenial-scale climate variability during the last glacial cycle. Climate Dynamics, 20, 257-267.

ROUSSEAU D.-D., 1987 - Paleoclimatology of the Achenheim series (Middle and Upper Pleistocene, Alsace, France). A malacological analysis. Palaeogeography, Palaeoclimatology, Palaeoecology, 59, 293-314.

ROUSSEAU D.-D., & KEEN D.H., 1989 - Malacological records from the Upper Pleistocene at Portelet (Jersey, Channel Islands): comparisons with Western and Central Europe. Boreas 18, 61-66.

ROUSSEAU D.-D., PUISSÉGUR J.-J., & LAUTRIDOU J.-P.,1990 - Biogeography of the Pleistocene pleniglacial malacofaunas in Europe. Stratigraphic and climatic implications. Palaeogeography, Palaeoclimatology, Palaeoecology, 80, 7-23.

ROUSSEAU D.-D., & PUISSÉGUR J.-J., 1990 - A 350,000 years climatic record from the loess sequence of Achenheim, Alsace, France. Boreas, 19 (3), 203-216.

ROUSSEAU D.-D., 1991 - Climatic transfer function from Quaternary molluscs in European loess deposits. Quaternary Research, 36, 195-209.

ROUSSEAU D.-D., ZÖLLER L., & VALET J.-P., 1998 – Late Pleistocene climatic variations at Achenheim, France, based on a magnetic susceptibility and TL chronology of loess. Quaternary Research, 49, 255-263.

ROUSSEAU D.-D., ANTOINE P., HATTÉ C., LANG A., ZÖLLER L., FONTUGNE M., BEN OTHMAN D., LUCK J.M., MOINE O., LABONNE M., BENTALEB I., & JOLLY D., 2002 - Abrupt millenial climatic changes from Nussloch (Germany) Upper Weichselian eolian records during the Last Glaciation. Quaternary Science Reviews, 21 (14/15), 1577-1582.

RUSKE R., & WÜNSCHE M., 1961 - Löße und fossile Böden im mittleren Saale- und unteren Unstruttal. Geologie, 10 (1), 9-29.

SÁNCHEZ GOÑI M.F., TURON J.-L., EYNAUD F., & GENDREAU S., 2000 - European climatic response to millenialscale changes in the atmosphere-ocean system during the Last Glacial period. Quaternary Research, 54, 394-403.

SÁNCHEZ GOÑI M.F., CACHO I., TURON J.-L., GUIOT J., SIERRO F.J., PEYPOUQUET J.-P., GRIMALT J.O., & SHACKELTON N.J., 2002 - Synchroneity between marine and terrestrial responses to millenial scale climate variability during the Last Glacial period in the Mediterranean region. Climate Dynamics, 19, 95-105.

SÁNCHEZ GOÑI M.F., 2006 - Interactions végétation-climat au cours des derniers 425.000 ans en Europe occidentale. Le message du pollen des archives marines. Quaternaire, 17, 3-25.

SCHIRMER W., 1995 - Rhein Traverse. Stop 40: Schwalbenberg/Remagen. Middle Würmian. In W. Schirmer (ed.), Quaternary field trips in Central Europe. Inqua, München, 1, 530-532.

SCHIRMER W., 2000 - Rhein loess, ice cores and deep-sea cores during MIS 2-5. Zeitschrift der Deutschen Geologischen Gesellschaft, 151 (3), 309-332.

SEMMEL A., 1968 - Studien über den Verlauf jungpleistozäner Formung in Hessen. Frankfurter geographische Hefte, 45, 1-133.

SHUR Y., JORGENSON M.T., & PULLMAN E.R., 2003 - Widespread Degradation of Ice Wedges on the Arctic Coastal Plain in Northern Alaska in Response to the Recent Warmer Climate. Eos Transaction AGU, 84 (46), Fall Meeting Supplement, Abstract C11A-05.

SPARKS B.W., 1961 - The ecological interpretation of Quaternary non-marine mollusca. Proceedings of the Linnean Society of London, 172, 71-80.

SÜMEGI P., 1989 - A hajdúság felsö-pleisztocén fejlödéstörténete finomrétegtani (öslénytani, szedimentológiai, geokémiai) viszgálatok alapján. Egyetemi doktori értekezés thesis, Kossuth University, Debrecen, 96 p.

SÜMEGI P., 2005 - Loess and Upper Paleolithic environment in Hungary. Aurea, Nagykovácsi, 312 p.

VANDENBERGHE J., & PISSART A., 1993 - Permafrost changes in Europe during the Last Glacial. Permafrost and Periglacial Processes, 4, 121-135

VAN VLIET-LANOË B., 1989 - Dynamics and extent of the Weichselian permafrost in Western Europe (substage 5e to stage 1). Quaternary International, 3/4, 109-113.

VAN VLIET-LANOË B., & HALLEGOUËT B., 1998 - Cartographie ANDRA-CNF-INQUA 1999.

VOELKER A.H.L., 2002 - Global distribution of centennial-scale records for Marine Isotope Stage (MIS) 3: a database. Quaternary Science Reviews, 21, 1185-1212.

WATTS W.A., ALLEN J.R.M., & HUNTLEY B., 1996 - Vegetation history and paleoclimate of the Last Glacial period at Lago Grande di Monticchio, southern Italy. Quaternary Science Reviews, 15, 133-153.

WERNERT P., 1957 - Contribution à la stratigraphie paléontologique et préhistorique des sédiments quaternaires d’Alsace, Achenheim. Thèse de Doctorat, Université de Strasbourg. Mémoires du Service de la carte géologique d’Alsace et de Lorraine, 14, 262 p.

WU H., GUIOT J., BREWER S., & GUO Z., 2007 - Climatic changes in Eurasia and Africa at the Last Glacial Maximum and mid­‑Holocene : reconstruction from pollen data using inverse vegetation modelling. Climate Dynamics, 29, 211-229.

ZAGWIN W.H., 1961 - Vegetation, climate and radiocarbon datings in the Late Pleistocene of the Netherlands. Part I: Eemian and Early Weichselian. Mededelingen van de Geologische Stichting. Nieuwe Serie, 14, 15-45.

ZAGWIN W.H., 1974 - Vegetation, climate and radiocarbon datings in the Late Pleistocene of the Netherlands. Part II: Middle Weichselian. Mededelingen Rijks Geologische Dienst. Nieuwe Serie, 25, 101-111.

ZELIKSON E.M., 1995 - Methodology of loess palynology. Geojournal, 36, 223-228.

ZÖLLER L., 1995 - Würm und Rißlöß - Stratigraphie und Thermolumineszenz-Datierung in Süddeutschland und angrenzenden Gebieten. Habilitation thesis, Ruprecht-Karls-Universität, Heidelberg, 223 p.

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Table des illustrations

Titre Fig. 1: Location of last-glaciation pollen records in Europe.
Légende Records located in northern continental Europe and in the Alps are discontinuous, whereas in France and in the Mediterranean domain most of the records are long and continuous. Records with the best time resolution are located in the Mediterranean domain except the Füramoos sequence located north of the Alps.
URL http://journals.openedition.org/quaternaire/docannexe/image/1532/img-1.jpg
Fichier image/jpeg, 58k
Titre Tab1: Pollen records of the last glaciation and of the Weichselian Upper Pleniglacial.
Légende These records may be complete (+), incomplete (±) or absent (-) and millennial-time scale vegetation changes may be absent (-), present(±) or present and correlated with ice-core global climatic records from Greenland (+).
URL http://journals.openedition.org/quaternaire/docannexe/image/1532/img-2.jpg
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Titre Fig. 2: Correlation between regional composite chronostratigraphical frameworks in Western Europe for the Weichselian Upper Pleniglacial
Légende All selected molluscan samples are located between the top of the basal soil, indicating the end of the Weichselian Middle Pleniglacial, and the base of Lateglacial deposits, i.e. between 35 ± 2 and ~ 15‑16 ka BP.
Crédits after Antoine et al.(2003) modified
URL http://journals.openedition.org/quaternaire/docannexe/image/1532/img-3.jpg
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Titre Tab. 2: Sites that yielded molluscan data attributed to the Weichselian Upper Pleniglacial.
Légende .
URL http://journals.openedition.org/quaternaire/docannexe/image/1532/img-4.jpg
Fichier image/jpeg, 127k
Légende Chronological data: AD = absolute dating; S = stratigraphy; UW and MW = Upper and Middle Weichselian
URL http://journals.openedition.org/quaternaire/docannexe/image/1532/img-5.jpg
Fichier image/jpeg, 66k
Titre Fig.3: Location of selected Weichselian Upper Pleniglacial molluscan records (sites numbered according to the list presented in table 1).
Légende Many of these records are associated with brickearth quarries located in the thickest loess deposits, i.e. often along major fluvial systems. Indeed, fluvial systems provided large quantities of mineral particles to be transported and deposited by the wind and to form thick loess deposits in surrounding areas.
URL http://journals.openedition.org/quaternaire/docannexe/image/1532/img-6.jpg
Fichier image/jpeg, 49k
Titre Fig.4: Number of molluscan samples available at selected sites.
Légende Sites coloured in grey include ten or more samples, and represent only 10% of the sites. There construction of Weichselian Upper Pleniglacial palaeoenvironmental changes on the basis of terrestrial mollusc assemblages is thus strongly limited by available data.
URL http://journals.openedition.org/quaternaire/docannexe/image/1532/img-7.jpg
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Titre Fig.5: Location of Weichselian Upper Pleniglacial molluscan records and contours of loess depositareas.
Légende See Catt (1985) and Haase et al. (2007) for more precise legends about loess types and thickness in England and continental Europe respectively.
URL http://journals.openedition.org/quaternaire/docannexe/image/1532/img-8.jpg
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Titre Fig.6: Location of Weichselian Upper Pleniglacial molluscan records and number of taxa per site.
URL http://journals.openedition.org/quaternaire/docannexe/image/1532/img-9.jpg
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Titre Fig. 7: Geographical distributions of types of molluscan assemblages defined for the Weichselian Upper Pleniglacial molluscan records (fig. 6) and of Last Glacial Maximum ice-wedge casts (black triangle) and isolated ice-wedges (white triangle) after Van Vliet-Lanoë & Hallégouët (1998) and Karte (1987).
URL http://journals.openedition.org/quaternaire/docannexe/image/1532/img-10.jpg
Fichier image/jpeg, 78k
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Olivier Moine, « West-european malacofauna from loess deposits of the Weichselian Upper Pleniglacial : Compilation and preliminary analysis of the database »Quaternaire, vol. 19/1 | 2008, 11-29.

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Olivier Moine, « West-european malacofauna from loess deposits of the Weichselian Upper Pleniglacial : Compilation and preliminary analysis of the database »Quaternaire [En ligne], vol. 19/1 | 2008, mis en ligne le 01 mars 2005, consulté le 19 mars 2024. URL : http://journals.openedition.org/quaternaire/1532 ; DOI : https://doi.org/10.4000/quaternaire.1532

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Auteur

Olivier Moine

Lehrstuhl für Geomorphologie, Universität Bayreuth, 95440 Bayreuth. Deutschland Couriel : olivier.moine@uni-bayreuth.de; Laboratoire de Géographique Physique, UMR CNRS 8591, 1 place Aristide Briand, 92195 Meudon Cedex, France. Couriel : omoine39@yahoo.fr

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