Aeolian sands and buried soils in the Mecklenburg Lake District, NE Germany: Holocene land-use history and pedo-geomorphic response

Geomorphology 211 (2014) 64–76

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Aeolian sands and buried soils in the Mecklenburg Lake District, NE Germany: Holocene land-use history and pedo-geomorphic response Mathias Küster a,⁎, Alexander Fülling b, Knut Kaiser c, Jens Ulrich d a

University of Greifswald, Institute of Geography and Geology, Friedrich-Ludwig-Jahn-Straße 16, 17487 Greifswald, Germany Humboldt University of Berlin, Institute of Geography, Unter den Linden 6, 10099 Berlin, Germany German Research Centre for Geosciences, Telegrafenberg, 14473 Potsdam, Germany d State Archaeological Survey of Mecklenburg-Vorpommern, Domhof 4-5, 19055 Schwerin, Germany b c

a r t i c l e

i n f o

Article history: Received 4 July 2011 Received in revised form 11 December 2013 Accepted 18 December 2013 Available online 6 January 2014 Keywords: Aeolian sands NE Germany Holocene Human impact Buried soils Aeolian morphology

a b s t r a c t The present study is a pedo-geomorphic approach to reconstructing Holocene aeolian sand dynamics in the Mecklenburg Lake District (NE Germany). Stratigraphical, sedimentological and soil research supplemented by morphogenetic interpretations of the genesis of dunes and aeolian sands are discussed. A complex Late Holocene aeolian stratigraphy within a drift sand area was developed at the shore of Lake Müritz. The results were confirmed using palynological records, archaeological data and regional history. Accelerated aeolian activity was triggered by the intensification of settlement and land-use activities during the 13th and in the 15th to 16th century AD. After a period of stability beginning with population decline during the ‘Thirty Years War’ and continuing through the 18th century, a final aeolian phase due to the establishment of glassworks was identified during the 19th century AD. We assume a direct link between Holocene aeolian dynamics and human activities. Prehistoric Holocene drift sands on terrestrial sites have not been documented in the Mecklenburg Lake District so far. This might be explained either by erosion and incorporation of older aeolian sediments during younger aeolian phases and/or a lower regional land-use intensity in older periods of the Holocene. The investigated drift sands are stratigraphically and sedimentologically characterised by a high degree of heterogeneity, reflecting the spatial and temporal variability of Holocene human impact. © 2014 Elsevier B.V. All rights reserved.

1. Introduction The nature, timing and intensity of erosional processes as a result of Holocene environmental changes are mainly attributed to climatic variation and changes in human activity in the landscape. However, based on the results of various case studies dealing with palaeoenvironmental changes in Central Europe, no significant relationship of regional cause– effect complexes is emphasised, preventing the definition of a dominant control mechanism (Zolitschka et al., 2003). Starting in the Early Holocene, forests are the characteristic potential natural vegetation of northern Central Europe (Lang, 1994). Thus, under natural conditions, forest would dominate the vegetation cover except in specific locations (Ellenberg, 1996). If one requires vegetation as a stabilising factor, the opening of a closed vegetation cover through human activity may cause an interruption of the potential Holocene surface stability. This results in soil erosion either by water or wind, which can thus be closely linked to the settlement and land-use history (Bork et al., 1998; Niller, 1998; Schatz, 2000; Dreibrodt et al., 2010). This is mainly discussed in terms of timing, type and intensity of human impact as determining factors. While some studies stress the simultaneous occurrence of human ⁎ Corresponding author. E-mail address: [email protected] (M. Küster). 0169-555X/$ – see front matter © 2014 Elsevier B.V. All rights reserved. http://dx.doi.org/10.1016/j.geomorph.2013.12.030

influence and atmospheric conditions as critical factor of erosional processes (Bateman and Godby, 2004; Dreibrodt, 2005; Starkel, 2005; Clemmensen et al., 2007), other investigations emphasise the different regional land use or its change as the driving factor (Castel et al., 1989; Macklin and Lewin, 2003; Oldfield and Dearing, 2003; Reiß et al., 2009). Therefore, to reconstruct geomorphic response to Holocene human impact, archaeological information about land-use practices and intensity must be taken into consideration, providing a multi-proxy geoarchaeological perspective (Kalis et al., 2003). Aeolian sediment sequences offer the possibility to reconstruct the relief dynamics of large landscape segments due to expansive genetic processes during sediment deflation, transport and accumulation (Bagnold, 1941; Stengel, 1992; Hassenpflug, 1998; Goossens and Gross, 2002). Along the so called ‘European sand belt’ and adjacent areas, stratigraphic studies provide long-term conceptual model data for the timing of aeolian phases in northern Central Europe from the Late Pleniglacial up to the present (Kozarski, 1978; Manikowska, 1991; Schirmer, 1999; Hilgers, 2007; Tolksdorf and Kaiser, 2012). Several papers deal primarily with the Pleni- to Late Glacial process–response system in terms of sedimentology, palaeopedology, chronostratigraphy as well as palaeoenvironmental and climatic reconstructions based on the chronostratigraphy (Vandenberghe, 1985; Terberger et al., 2004; Kasse et al., 2007; Kaiser et al., 2009). Far less research of this type has

M. Küster et al. / Geomorphology 211 (2014) 64–76

been carried out for the Holocene, and only at a very coarse spatial resolution (e.g., Pyritz, 1972; Alisch, 1995; Dulias, 1999; Müller, 1999). Local dune areas in the Netherlands, NW Germany and Poland are well described. In these locations mainly morphogenetic and lithofacial approaches on Holocene dune formation were discussed, with chronological classifications hitherto based on palynological and only a few AMS and OSL datings (Castel et al., 1989; Kozarski and Nowaczyk, 1991; Koster et al., 1993; Mauz et al., 2005). In NE Germany aeolian sands mainly occur associated with icemarginal valleys, outwash plains and large glaciolacustrine basins. They are rare on till plains and in ice-marginal zones. With respect to settings, timing, distribution pattern, morphogenetic implications and

65

driving factors (natural and/or anthropogenic) however, the understanding of Holocene aeolian dynamics is still in an early stage (e.g., Teschner-Steinhardt and Müller, 1994; Bussemer et al., 1998; Brande et al., 1999; Küster and Preusser, 2009). Recent comprehensive stratigraphical research in NE Germany has mainly focused on dating aspects alongside the ice-marginal valleys of the Wechselian glaciation, providing a first regional dataset of absolute (OSL) dating of Holocene aeolian activity phases (Hilgers, 2007). This paper deals with the stratigraphy, sedimentology and pedology of a dune area in NE Germany at Lake Müritz. The results are discussed with respect to palynological records, archaeological data and regional historical knowledge, providing a chronological and genetic link

Fig. 1. Map of the study area at Lake Müritz showing topography, dunes, archaeological/historical sites and analysed profiles (adapted from Kaiser et al. (2002) and data from the State Archaeological Survey of Mecklenburg-Vorpommern, unpublished material); A. Small map of local geology; B.

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between human impact and the resulting pedo-geomorphic response. Furthermore our data provide morphostratigraphical and sedimentological implications for Holocene drift sand areas in Central Europe. 2. Study area The study area is located east of Lake Müritz (117 km2), the largest lake in the North German Plain (Fig. 1). Geological knowledge of the study site is based primarily on overview mapping during the 1950s– 1960s, and a few genetic landscape investigations from this period (Hurtig, 1954/1955; Schmidt, 1962; Meinke et al., 1967). The area is widely built up of morainic sediments. In the eastern part of the study area the sediments comprise tills, sands and erratics from the maximum advance of the Pomeranian Phase (W2 max., ca. 20 kyr, Lüthgens and Böse, 2011). Pleistocene basin sands form the sediments in the west and the intermediate plateau sands of the proximal outwash plain are covered by aeolian sands. Periglacial surface features have not been found in the study area (Dieckmann and Kaiser, 1998). In addition to the predominant morainic ridge, reaching a maximum altitude of 94 m a.s.l., dunes of various sizes and shapes are the most distinctive morphological elements. The sandy plains are subdivided by closed peat-filled depressions and where they border on lake basins with aggradational peat fringes there is either a smooth geomorphic transition or a lake terrace. This terrace has an average height of 1 m above lake level, described at various sites and reflecting significant historical hydrological changes at Lake Müritz (Kaiser, 1998; Lampe et al., 2009). In the dry outwash plain the surface soils are mainly classified as Arenosols and podzolised Arenosols (IUSS Working Group, 2006) under predominantly pine forest vegetation. These soils reflect rather young soil formation whereas only sporadically occurring welldeveloped (Gleyic) Podzols reflect a longer soil genesis. At till plain sites, Luvisols and Cambisols/brunic Arenosols form the potential soil mosaic under today's pine and beech forest with relic oak stands (Dieckmann and Kaiser, 1998). Wet sites are covered by willow and alder and are used as meadows and pastures. Corresponding soils are anthropogenically drained Histosols and Gleysols. Due to its forest cover, the use as military training area until the mid1990s, and restrictions due to its status as a nature reserve, a comprehensive archaeological exploration within the study area has been very difficult so far. Thus, the number of the documented archaeological sites is very small and largely based on random surface observations (Fig. 1). Comparing the find density in the study area with sparsely forested areas around Lake Müritz (Schoknecht et al., 1999; Kaiser et al., 2002), a significantly higher number of archaeological sites can potentially be expected. Nevertheless, recent discoveries provide a qualitative overview of the local Holocene settlement history. 3. Material and methods 3.1. Field methods After an initial survey comprising first soil and pollen analyses as well as 14C datings (profiles: Boek 1, Boeker Moor; Kaiser et al., 2002) the extensive sampling of the study area took place in 2008–2009. After cartographical identification of sub-areas, hand drillings were carried out with a Pürckhauer-auger consisting of 1 m segments with a diameter of 30 mm. The aim was to obtain an overview of soil and sediment stratigraphies and structures reflecting the relief development and to find representative profiles for certain areas (e.g., Billwitz, 2000). Nine soil pits were excavated to a depth of between 1 and 2.20 m, measured from the upper boundary of the mineral soil. The reference faces were recorded (incl. CaCO3 field-test) following the guidelines of the German soil survey (Ad-hoc-AG Boden, 2005, “KA5”). Soil horizons and soil types were classified afterwards according to the IUSS Working Group WRB (2006). The profiles were documented in photographs and scaled sketches. Colours were determined

according to Munsell (1994). A total of 80 pedological samples were taken from the soil pits (Table 1). To determine the onset of aeolian activity phases, 15 OSL samples were collected in undisturbed sediment layers not penetrated by roots above buried soil horizons (Fig. 2). A radiocarbon sample (peat) was taken from the buried organic horizon in Profile Sh 1 (3Ahb1, Table 2). 3.2. Laboratory methods Grain-size distribution was determined by laser diffractometry of fine sediments. The organic matter content was estimated by loss on ignition (LOI) at 550 °C for 2 h after crushing and drying each sample. Soil pH was determined potentiometrically in 0.01 M CaCl2. No calcareous sediments were detected in field testing, thus laboratory analysis was omitted. The radiocarbon sample was dated by accelerator mass spectrometry (AMS) at Erlangen Laboratory, Germany. Two further radiocarbon ages on aeolian stratigraphies from the study area are available from an earlier study (Kaiser et al., 2002; Table 2). The radiocarbon ages are calibrated by using CALIB 5.0.1 (Stuiver and Reimer, 1993; Stuiver et al., 2005). OSL ages were determined at the luminescence dating laboratory at Humboldt University, Berlin (Table 3). All OSL laboratory procedures were conducted under subdued red light to avoid any resetting of the latent luminescence signal stored in the minerals. After separating the coarse-grained sediment fraction by sieving (90–200 μm), carbonates and organic material were removed using hydrochloric acid (10 and 30%) and hydrogen peroxide (10 and 30%), respectively. Quartz was extracted by density separation using heteropolytungstate heavy liquid (LST, 2.75 and 2.62 g/cm3). The outer layer of the prepared quartz grains was then removed by etching with hydrofluoric acid (40%, 60 min) to eliminate the influence of short-range α-irradiation. After renewed sieving (90 μm), the quartz grains were mounted on aluminium cups using silicon spray as an adhesive (aliquot size 5 mm). The OSL measurements were performed on a Risø TL-DA 15 reader following the single-aliquot regenerative dose (SAR) protocol (Murray and Wintle, 2000). The prepared quartz samples were optically stimulated with blue LEDs (λ = 470 ± 30 nm) at 125 °C for 40 s, and the OSL signals were recorded through a Hoya U340 filter (λ = 330 ± 40 nm). The pre-heat temperature was set to 180 °C (10 s), the test dose cutheat temperature to 160 °C. These settings were verified performing a dose recovery test on sample HUB-0003. After resetting the luminescence signal (blue stimulation for 200 s), 24 aliquots were irradiated with a beta dose of 1.15 Gy and subsequently measured applying the SAR protocol (varying preheat temperatures from 180 to 240 °C for 10 s, cut-heat of 160 °C, six aliquots per temperature point). The recovered doses ranged from 1.17 ± 0.02 Gy (180 °C) to 1.23 ± 0.05 Gy (240 °C). The sediment dose rates were estimated by measuring the contents of uranium, thorium and potassium applying high-resolution gamma spectrometry. The cosmic ray dose rates were estimated from geographic position, elevation and burial depths (Prescott and Hutton, 1988). 4. Results 4.1. Pedo-geomorphic field findings 4.1.1. General aeolian morphology Aeolian (positive) morphology within the study area is characterised by flat sand sheets with a minimum thickness of 0.03 m up to dune bodies with a maximum thickness of 12 m. Most of the dunes have a hummocky shape with an oval to round base, regionally classified as a ‘Kuppen-/Kupstendüne’ (e.g., Pyritz, 1972; Louis and Fischer, 1979). Other dune forms are linear dunes of several hundred metres length, parabolic dunes and intermediate structures showing transitional features. Dunes occur on sandy plateau sites of the outwash plain, at the ice-marginal zone and, conspicuously, on the border to peat and lake

M. Küster et al. / Geomorphology 211 (2014) 64–76

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Table 1 Sedimentological and pedological parameters of profiles at Lake Müritz. Profile FO 1–2

Northing

53°24′40.2″

Easting

12°48′26.5″

Depth

Horizon

Horizon

Colour

pH

LOI

Clay

Silt

F.-Sand

M.-Sand

C.-Sand

Mean

Median

[%]

[%]

[%]

[%]

[%]

[%]

[μm]

[μm]

0.9 0.9 1.0 0.9 0.9 0.7 0.9 1.4 1.2 0.9 1.9 0.7

2.0 1.2 1.2 0.8 2.3 1.0 1.1 4.3 2.3 1.4 12.3 0.6

50.7 54.3 56.0 41.6 45.6 24.3 42.1 59.9 59.1 44.5 33.4 35.4

42.4 40.4 38.6 51.5 46.8 57.2 50.0 32.0 35.4 46.5 42.2 56.3

3.9 3.3 3.2 5.1 4.5 16.9 5.8 2.4 2.1 6.7 10.3 7.0

195 189 185 225 207 319 225 163 172 220 202 249

191 184 181 220 204 326 218 162 170 211 211 243

0.84 0.80 0.78 0.85 0.89 0.98 0.88 0.85 0.77 0.93 1.69 0.85

Sorting

[cm]

(KA-5)

(WRB)

(Munsell)

CaCl2

10 15 25 61 74 98 116 118 130 187 194 220

Oh-Ahe Bsh-ilCv fAeh ilCv-fBsh fAeh fBs-ilCv ilCv fAih-ilCv fBv-ilCv ilCv IIfBv IIIilCv

AhO CBsh Ahb BshCb Ahb CBsb C CAhb CBwb C 2Bwb 3C

10YR6/1 10YR7/6 10YR5/2 7.5YR6/6 10YR6/1 10YR6/6 2.5Y7/3 2.5Y6/3 10YR6/4 2.5Y7/4 10YR4/6 2.5Y7/3

3.5 3.6 3.9 4.4 4.3 4.4 4.5 5.0 5.4 5.2 4.6 5.3

3.1 1.3 0.8 0.4 0.9 0.5 0.3 0.4 0.3 0.3 3.1 0.3

Sorting

Profile FO 1–3

Northing

53°24′40.6″

Easting

12°48′30.1″

Depth

Horizon

Horizon

Colour

pH

LOI

Clay

Silt

F.-Sand

M.-Sand

C.-Sand

Mean

Median

[cm]

(KA-5)

(WRB)

(Munsell)

CaCl2

[%]

[%]

[%]

[%]

[%]

[%]

[μm]

[μm]

10 26 37 72 155 165 185 220

Oh-Aeh Bsh-ilCv fAeh fBsh-ilCv ilCv IIfAh fBv-ilCv ilCv

AhO CBsh Ahb CBshb C 2Ahb 2CBwb 2C

10YR6/1 10YR7/6 10YR7/1 10YR7/6 2.5Y7/2 10YR5/3 10YR6/6 2.5Y7/2

3.3 3.8 3.9 4.1 4.3 4.2 4.7 5.0

35.6 34.6 38.3 38.8 38.6 40.9 30.0 32.8

53.8 52.9 54.4 53.3 52.2 49.8 55.5 56.7

8.6 8.2 5.7 5.8 7.2 5.8 12.4 8.5

252 244 236 234 237 222 281 259

244 240 230 229 230 218 275 252

0.92 0.99 0.84 0.88 0.90 0.92 0.97 0.89

Sorting

2.8 0.9 1.0 0.6 0.3 0.5 0.4 0.3

0.7 0.9 0.7 0.9 0.9 1.1 0.8 0.8

1.2 3.4 0.9 1.2 1.2 2.5 1.3 1.2

Profile FO 1–8

Northing

53°24′45.7″

Easting

12°49′14.9″

Depth

Horizon

Horizon

Colour

pH

LOI

Clay

Silt

F.-Sand

M.-Sand

C.-Sand

Mean

Median

[cm]

(KA-5)

(WRB)

(Munsell)

CaCl2

[%]

[%]

[%]

[%]

[%]

[%]

[μm]

[μm]

10 26 60 92 115 120 145 155 180

Ah Ah-M M IIilCv Go Go-fAeh-ilCv IIInH1 nH2 IVGo

Ah Ah C 2C 2Cg 2CAhCgb 3H1 3H2 4Cg

10YR3/1 10YR4/1 10YR5/3 2.5Y7/2 10YR7/4 10YR5/4 10YR2/2 10YR2/1 10YR7/4

3.2 3.4 3.5 4.0 4.1 3.9 5.1 5.4 5.3

4.4 3.0 3.7 0.7 0.9 3.6 67.2 35.4 0.6

1.0 1.6 1.5 1.2 1.4 1.6 2.3 2.0 1.2

16.0 20.7 21.9 11.2 14.6 21.1 40.3 29.4 11.7

46.2 43.6 44.4 40.0 59.2 61.1 16.2 33.4 44.2

31.1 30.5 29.4 45.7 22.9 13.9 9.9 29.4 37.3

5.8 3.6 2.9 2.0 2.0 2.5 31.4 5.8 5.7

139 108 105 178 127 98 113 97 176

160 152 147 193 139 113 128 135 178

1.64 1.83 1.80 1.41 1.41 1.52 2.64 2.12 1.51

Sorting

Profile FO 3–7

Northing

53°24′18.7″

Easting

12°49′10.7″

Depth

Horizon

Horizon

Colour

pH

LOI

Clay

Silt

F.-Sand

M.-Sand

C.-Sand

Mean

Median

[cm]

(KA-5)

(WRB)

(Munsell)

CaCl2

[%]

[%]

[%]

[%]

[%]

[%]

[μm]

[μm]

3 7 15 22 66 72 136 146 164 172 190 210 220

Aeh Bsh fOh-Aeh fBsh ilCv fAih ilCv fAh ilCv IIfAh fBv fBv-ilCv rGo

Ah Bsh AhOb Bshb C Ahb C Ahb C 2Ahb 2Bwb 2CBwb 2Cg

10YR 5/2 10YR 4/4 10YR 5/3 10YR 5/6 2.5Y6/3 10YR 4/1 2.5Y7/4 10YR 4/1 2.5Y7/2 10YR 5/1 10YR 5/8 10YR 6/6 7.5YR6/8

3.5 3.5 3.6 3.7 4.2 4.2 4.3 4.4 4.5 4.5 4.5 4.5 4.6

1.4 1.5 1.6 1.6 1.5 1.5 1.5 1.9 1.7 2.1 1.9 1.7 1.4

17.0 19.3 21.8 18.6 16.2 17.4 16.3 15.9 13.7 16.7 14.9 14.5 10.2

43.2 43.7 43.9 48.0 38.8 38.7 39.2 58.3 67.2 42.4 38.3 42.1 10.0

36.4 33.3 29.9 31.0 42.2 40.6 42.1 22.3 16.5 36.4 43.4 40.0 58.2

2.1 2.3 3.0 0.9 1.3 1.9 0.9 1.7 0.9 2.4 1.5 1.7 20.2

128 95 91 84 101 100 98 108 122 121 140 137 325

161 156 144 149 177 173 178 138 134 164 183 175 396

1.74 2.00 2.02 2.02 2.05 2.12 2.05 1.60 1.33 1.83 1.73 1.64 1.71

Sorting

3.8 2.0 2.0 1.1 0.5 0.6 0.4 0.8 0.6 0.8 0.8 0.4 0.3

Profile Ba 1

Northing

53°24′26.2″

Easting

12°51′14.2″

Depth

Horizon

Horizon

Colour

pH

LOI

Clay

Silt

F.-Sand

M.-Sand

C.-Sand

Mean

Median

[cm]

(KA-5)

(WRB)

(Munsell)

CaCl2

[%]

[%]

[%]

[%]

[%]

[%]

[μm]

[μm]

7 15 33 43 100

Ahe + Ae ilCv-Bsh ilCv IIfBv IIIilCv

E/Ah BshC C 2Bwb 3C

10YR7/1 7.5YR5/6 2.5Y7/4 10YR4/4 2.5Y7/2

3.4 3.6 4.5 5.0 4.4

1.3 1.4 0.3 5.3 0.1

11.1 9.7 2.1 28.3 1.3

48.4 57.2 44.8 37.7 47.6

34.8 31.7 46.8 25.8 50.9

167 152 218 57 191

168 156 208 118 202

2.2 1.4 0.4 2.7 0.4

4.4 0.0 6.0 3.0 0.0

1.33 1.19 0.89 2.64 0.56

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M. Küster et al. / Geomorphology 211 (2014) 64–76

Table 1 (continued) Profile Ba 2

Northing

53°24′31.9″

Easting

12°51′28.3″

Depth

Horizon

Horizon

Colour

pH

LOI

Clay

Silt

F.-Sand

M.-Sand

C.-Sand

Mean

Median

[cm]

(KA-5)

(WRB)

(Munsell)

CaCl2

[%]

[%]

[%]

[%]

[%]

[%]

[μm]

[μm]

12 17 48 61 65 80 103 122 150

Ahe ilCv-Bhs ilCv fAeh ilCv IIfAeh fBsv fBv-ilCv ilCv

Ah BshC C Ahb C 2Ahb 2Bsv 2CBwb 2C

10YR6/1 10YR5/6 2.5Y7/6 2.5Y5/2 2.5Y7/6 2.5Y5/2 10YR5/6 10YR 6/6 2.5Y7/2

3.6 3.8 4.3 4.5 4.6 4.5 4.4 4.4 5

2.2 1.3 0.7 0.8 0.5 0.7 0.6 0.5 0.3

1.6 1.1 0.9 3.9 1.6 3.4 1.3 4.0 1.7

14.2 7.1 4.2 25.0 8.0 21.2 10.8 32.5 10.7

40.6 46.9 50.5 50.0 44.3 47.1 64.0 55.1 49.0

39.4 41.1 44.4 20.3 46.1 26.6 24.0 8.4 35.6

168 187 182 64 181 83 140 48 163

180 185 186 120 189 133 143 90 165

1.48 1.28 0.87 2.21 1.35 2.09 1.16 2.12 1.49

12°51′28.6″ Sorting

4.3 3.7 0.0 1.0 0.1 1.9 0.0 0.3 3.1

Sorting

Profile Ba 3

Northing

53°24′14.4″

Easting

Depth

Horizon

Horizon

Colour

pH

LOI

Clay

Silt

F.-Sand

M.-Sand

C.-Sand

Mean

Median

[cm]

(KA-5)

(WRB)

(Munsell)

CaCl2

[%]

[%]

[%]

[%]

[%]

[%]

[μm]

[μm]

1 3 5 33 45 60 130 153 200

Ah ilCv fOh-Aeh ilCv fOh-Ahe fBsh ilCv IIfBv-ilCv ilCv

Ah C AhOb C AhOb Bshb C 2CBwb 2C

10YR 3/1 10YR 6/2 10YR 3/2 10YR 6/2 10YR 7/1 10YR 6/6 2.5Y7/2 10YR 5/6 2.5Y7/2

3.6 3.7 3.4 3.9 3.5 4.0 3.4 4.0 3.3

1.8 0.9 2.3 0.9 1.4 0.8 0.4 1.0 2.3

1.1 1.3 1.1 1.3 1.6 1.6 1.4 1.4 1.4

10.4 10.7 12.9 12.3 15.2 15.8 10.8 12.5 16.5

42.4 41.9 41.1 39.9 42.5 43.5 46.9 38.0 42.4

36.9 40.7 38.0 41.3 35.1 32.7 37.8 42.1 34.8

196 188 181 185 142 136 172 189 135

187 187 182 188 170 166 173 193 167

1.64 1.51 1.61 1.56 1.79 1.84 1.43 1.59 1.79

12°49′54.8″ Sorting

9.2 5.4 6.9 5.3 5.6 6.5 3.1 6.0 5.0

Profile Sh 1

Northing

53°24′52.4″

Easting

Depth

Horizon

Horizon

Colour

pH

LOI

Clay

Silt

F.-Sand

M.-Sand

C.-Sand

Mean

Median

[cm]

(KA-5)

(WRB)

(Munsell)

CaCl2

[%]

[%]

[%]

[%]

[%]

[%]

[μm]

[μm]

25 71 75 110 115 140 150

Ah ilCv IIfAih ilCv IIIfAh1 fAh2 IVGr

Ah C 2Ahb 2C 3Ahb1 3Ahb2 4Gr

10YR 3/1 10YR 7/4 2.5Y5/2 2.5Y7/1 2.5Y/1 2.5Y3/1 2.5Y6/2

4.4 4.6 5.2 5.5 4.4 5.4 5.6

3.4 0.6 1.9 0.5 8.1 4.7 0.4

1.7 1.0 1.4 0.7 5.6 0.6 0.7

21.7 4.5 15.7 3.0 63.2 4.8 3.0

40.2 60.0 48.4 44.0 25.6 22.1 44.0

33.8 34.5 31.4 50.9 5.3 54.3 50.9

2.7 0.0 3.3 1.3 0.6 18.3 1.3

111 162 135 199 21 312 199

155 198 159 165 153 333 205

1.76 1.19 1.25 0.77 1.47 1.14 0.73

12°50′38.0″ Sorting

Profile Za 1′

Northing

53°22′19.8″

Easting

Depth

Horizon

Horizon

Colour

pH

LOI

Clay

Silt

F.-Sand

M.-Sand

C.-Sand

Mean

Median

[cm]

(KA-5)

(WRB)

(Munsell)

CaCl2

[%]

[%]

[%]

[%]

[%]

[%]

[μm]

[μm]

4 6 22 28 53 95 106 120

Aeh Bsh-ilCv ilCv fAh fBv ilCv IIfBv IIIilCv

Ah CBsh C Ahb Bwb C 2Bwb 3C

10YR5/1 10YR6/6 2.5Y7/4 2.5Y5/2 10YR5/6 2.5Y7/4 10YR5/6 2.5Y7/1

3.8 4.2 4.5 4.5 4.5 4.8 4.3 4.7

0.5 0.4 0.4 0.6 0.7 0.4 1.0 0.2

0.7 0.5 0.6 0.9 0.9 0.5 0.5 0.5

29.2 17.5 23.8 28.8 28.9 20.9 18.5 18.7

57.3 62.1 59.9 53.3 50.1 55.7 52.9 59.1

12.0 19.8 14.8 14.5 16.9 22.5 26.2 20.2

285 362 314 285 290 355 371 352

284 370 316 285 294 376 410 362

basins (Fig. 3). Erosional (negative) morphologies, like deflation hollows, are partly filled by younger aeolian sands or show a modified size and shape at the current surface. 4.1.2. Outwash plain at Zartwitz Profile Za 1 (Fig. 4) was excavated at the edge of a hummock-shaped dune close to the village Zartwitz. It consists of a composite section of four sedimentological units, two buried soils and the surface soil. Above basal glaciofluvial sands, the almost 10 cm-thick remnants of a periglacial cover bed were detected. According to German terminology the periglacial cover bed can be classified as ‘Geschiebedecksand’ (GDS), characterised by its typical content of pebbles especially at its base (Lembke, 1972; Bussemer, 2002; Küster and Preusser, 2009). The GDS coincides with a buried Bw horizon, often observed in NE Germany (Kopp, 1970; Bussemer, 2005; Bussemer et al., 2009), which can be

0.9 0.1 0.9 2.6 3.2 0.4 1.9 1.5

0.96 0.87 0.93 1.05 1.14 0.98 1.04 0.94

correlated with the so called Finow soil, first described by Schlaak (1993). This palaeosol has typical features and can be classified as palaeopedological marker horizon in northern Central Europe (Kaiser et al., 2009). As a diagnostic feature the strong rooting underlines its classification as a weathered horizon and therefore nutrient source for the present-day vegetation. The Finow soil is covered by a shallow sand unit, which is the parent material of a buried brunic Arenosol above. Degradation (deflation) of the brownish B horizon is obvious in some parts of the cross-section. Starting from the upper buried soil, a settlement pit interrupts the soil sequence down to the lower buried soil. Within the pit and the Ahb horizon pottery from the Bronze Age was recovered. The potsherd edges are smooth and steep. Only edge fragments are roughed up. Furthermore, pebbles and charcoal fill the pit. A thin aeolian sand unit is found at the surface of the profile, which changes northwards into a dune body with distinct hummocky

M. Küster et al. / Geomorphology 211 (2014) 64–76

69

Fig. 2. Simplified pedo-stratigraphical logs including luminescence, radiocarbon and archaeological datings.

Table 2 Radiocarbon data of investigated profiles. 14C ages are calibrated according to Stuiver and Reimer (1993) and Stuiver et al. (2005). Profile

Northing

Easting

Lab. nr.

Depth [cm]

б13C

Material

Age in yr BP

Cal. age 2σ BC/AD

Boek 1 Sh 1 Boeker Moor

53°24′37.3″ 53°24′52.4″ 53°23′58.74″

12°49′6.06″ 12°49′54.8″ 12°50′14.1″

Hv-19537 Erl-13099 Hv-22342

67–70 111–112 401–402

−29, 3 −23, 6 −26, 2

Bulk org. matter Bulk org. matter Peat

1370 ± 60 1224 ± 40 1495 ± 135

564–775 AD 685–890 AD 239–782 AD

Table 3 Optical dating results: dosimetry data, equivalent doses (ED) and OSL ages. Sample

Lab. No.

Depth [m]

Number of selected aliquotsa

U [ppm]b

Th [ppm]b

K [%]b

Za 1 Sh 1 Ba 1 Ba 2 Ba 3/1 Ba 3/2 FO 1–8 FO 3–7/1 FO 3–7/2 FO 3–7/3 FO 1–2/1 FO 1–2/2 FO 1–2/3 FO 1–3/1 FO 1–3/2

HUB-0001 HUB-0003 HUB-0005 HUB-0007 HUB-0033 HUB-0034 HUB-0035 HUB-0036 HUB-0037 HUB-0038 HUB-0039 HUB-0040 HUB-0041 HUB-0042 HUB-0043

0.50 0.70 0.25 0.50 0.23 1.20 1.08 0.58 1.30 1.56 0.12 0.55 1.10 0.23 1.50

22 21 20 21 15 14 13 17 13 20 18 17 11 14 10

0.98 0.74 1.15 0.82 0.90 0.82 1.18 0.60 0.70 0.60 1.02 0.91 0.82 0.99 0.93

2.28 1.98 3.38 2.28 2.62 2.55 3.08 1.81 1.77 1.60 2.86 2.55 2.44 2.88 2.64

0.92 1.01 1.07 1.04 1.01 1.08 1.04 0.98 0.96 1.09 1.01 1.01 1.04 0.98 0.99

a b c

± ± ± ± ± ± ± ± ± ± ± ± ± ± ±

24 aliquots per sample were measured. An error of ±5% was assumed for all samples. Arithmetic mean of selected aliquots with standard deviation.

0.05 0.04 0.06 0.04 0.05 0.04 0.06 0.03 0.04 0.03 0.05 0.05 0.04 0.05 0.05

± ± ± ± ± ± ± ± ± ± ± ± ± ± ±

0.11 0.10 0.17 0.11 0.13 0.13 0.15 0.09 0.09 0.08 0.14 0.13 0.12 0.14 0.13

± ± ± ± ± ± ± ± ± ± ± ± ± ± ±

0.05 0.05 0.05 0.05 0.05 0.05 0.05 0.05 0.05 0.05 0.05 0.05 0.05 0.05 0.05

Cosmic dose rate [Gy/kyr]

Water cont. [%]

Total dose rate [Gy/kyr]

Equivalent dose [Gy]c

OSL age [kyr]

0.20 0.20 0.20 0.20 0.21 0.19 0.19 0.20 0.19 0.19 0.21 0.20 0.19 0.21 0.19

3 3 3 3 3 3 3 3 3 3 3 3 3 3 3

1.44 1.47 1.72 1.54 1.55 1.58 1.66 1.40 1.39 1.47 1.60 1.55 1.54 1.56 1.53

1.08 0.99 1.32 1.18 – 1.11 1.00 0.65 0.72 1.05 0.18 0.70 1.03 0.26 0.80

0.75 0.68 0.77 0.77 – 0.70 0.60 0.47 0.52 0.72 0.11 0.46 0.67 0.16 0.52

± ± ± ± ± ± ± ± ± ± ± ± ± ± ±

0.01 0.01 0.01 0.01 0.01 0.01 0.01 0.01 0.01 0.01 0.01 0.01 0.01 0.01 0.01

± ± ± ± ± ± ± ± ± ± ± ± ± ± ±

2 2 2 2 2 2 2 2 2 2 2 2 2 2 2

± ± ± ± ± ± ± ± ± ± ± ± ± ± ±

0.06 0.06 0.07 0.06 0.06 0.06 0.06 0.06 0.06 0.06 0.06 0.06 0.06 0.06 0.06

± ± ± ±

0.05 0.05 0.07 0.06

± ± ± ± ± ± ± ± ± ±

0.06 0.05 0.03 0.05 0.05 0.03 0.03 0.05 0.04 0.04

± ± ± ±

0.04 0.04 0.05 0.05

± ± ± ± ± ± ± ± ± ±

0.04 0.04 0.03 0.04 0.04 0.02 0.03 0.04 0.03 0.03

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morphology. The surface soil is characterised by its mostly weak podzolisation and can be classified as a podzolised Arenosol, while only some parts of the cross-section show stronger podzolisation.

4.1.3. Ice-marginal zone and proximal outwash plain The sedimentological situation in the transition area of the outwash plain towards the top of the morainic ridge is represented by profile Ba 1. The basal portion shows the same pedo-stratigraphy as profile Za 1, comprising a periglacial cover bed, the GDS and the Late Glacial Finow soil, which shows a higher amount of silt. However a pedostratigraphically expected upper Late Glacial to Holocene soil is not detectable (e.g., Küster and Preusser, 2009). The podzolised Arenosol on the top shows an advanced differentiation into an eluvial and an illuvial horizon, reflecting the state of transformation to a Podzol.

On the morainic ridge of the ice-marginal zone deflation surfaces and accumulation areas, represented by profiles Ba 1 and Ba 2, alternate mosaically. Blocks and stones appear on the whole surface. Profile Ba 2 is situated next to a hummocky plateau dune at the upper slope of the morainic ridge in transition to the proximal outwash sediments. The profile consists of three sedimentological units including basal glaciofluvial sands and two upper units of aeolian origin. Pedologically the glaciofluvial sands are characterised by a podzolised brunic Arenosol. Within the following first thin aeolian unit (approx. 10 cm thickness) a weakly podzolised Arenosol has developed. However, the Arenosol in the aeolian layer (approx. 50 cm thickness) on top is more strongly podzolised reflecting a higher acidity. Profile Ba 3 was excavated within the culmination area of the morainic ridge. Its base is also made up of glaciofluvial sand, overlain by three aeolian sand layers which build up a hummocky plateau dune.

Fig. 3. Photos of selected sites investigated at Lake Müritz. (A) Profile Ba 1. (B) Profile Boek 1. (C) Profile Sh 1. (D) Hummocky dune at Zartwitz. (E) Dune at the edge of a peat-filled basin.

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Fig. 4. Pedological and sedimentological cross-section at the outwash plain close to the village Zartwitz. Pedological parameters of profile Za 1′ are given in Table 1. The simplified log of the dated profile Za 1 is given in Fig. 2.

Remarkable in this profile is the presence of a Bwb horizon which normally occurs only in fragmentary form in meltwater sands. This horizon has an abrupt upper boundary. An Ahb horizon is absent. Within the lower aeolian sand unit, especially near the lower boundary, isolated planar medium to coarse sand layers with slightly inclined bedding in slope direction appear. The unit is separated from the upper units by a podzolised Arenosol. The younger Arenosols are not podzolised. 4.1.4. Outwash plain at Boek and Fauler Ort In the area of the outwash plain (profiles: FO 1–2, FO 1–3, FO 3–7) and the adjacent transition zone to the (lake-) basins (profiles: Sh 1, FO 1–8) five profiles were analysed. Profile Sh 1 is situated on a 1 m terrace, which morphologically marks the boundary between the sandy plain and adjacent areas of organic aggradation at Lake Priesterbäker See (Fig. 1). Macroscopically, the basal part appears to consist of amorphous black peat. However, a relatively low LOI-value (8%) classifies the horizon as a buried minerogenic surface horizon (Ahb). It changes into pale lacustrine sands with incorporated thin organic layers. The lacustrine unit is separated from the aeolian sands above by a partly reworked humic horizon. Within the aeolian cover there is a fragmentary organic layer at a depth of 59–64 cm. Profile FO 1–8 is located in the footslope position of a dune and documents an aeolian coverage of a peat composed aggradational zone. The woody peat is mineralised at

its surface. Podzolic characteristics within the transition from peat to overlying sands occur. At the top, colluvial sand reflect local erosional slope processes. At the sandy plateau sites (profiles: FO 1–3, FO 3–7) degraded brunic Arenosols were found, which developed in basal glaciofluvial sands. However, profile FO 1–2 shows a typical Late Glacial stratigraphy with the Finow soil developed in GDS, and an overlying coversand unit with only a discontinuous, residual brownish B horizon of a former brunic Arenosol. In each profile, relief-forming drift sands separated by Arenosols or podzolised Arenosols are evident. 4.2. Laboratory data 4.2.1. Pedology and sedimentology To identify possible changes of sedimentary patterns during historical (past) aeolian phases, which might reflect changes of the aeolian regime (e.g., process intensity, sediment provenance, depletion of finer grain sizes over time; Bagnold, 1941; Pye and Tsoar, 1990; Castel, 1991; Clemmensen et al., 2007), the grain size parameters median and sorting were evaluated (Fig. 5). These samples are characterised by poor sorting with values between 0.8 and 2.1. The dunes have an average median grain size of 199 μm (fine sand, 64% of the samples yield values b 200 μm) ranging from 113 (fine sand) to 370 μm (medium

Fig. 5. Diagram illustrating sedimentary parameters using median and sorting values of samples of dated aeolian sand units. Both parameters are related to the timing of aeolian sedimentation.

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Fig. 6. Dating of aeolian sands at Lake Müritz. Main phases of aeolian activity are displayed by the probability density function (assuming equal relative age uncertainties for all samples).

sand). Sorting and median grain sizes show no clear pattern or tendency in relation to the time of aeolian sedimentation, neither within each sequence nor in comparison between locations. However, the southernmost profile Za 1 shows coarser grain size distributions, due to coarsegrained outwash plain material in this area. The Late Glacial palaeosols are characterised by a typical enrichment of silt, compared to the sand units below. The silt content ranges from 1.9 to 28.3%. The organic matter content of surface horizons varies between 0.5 and 4.4% (average 3.1% LOI), however LOI of buried humic horizons is lower (average 1.2%, range of 0.4 to 3.6%; horizons of profile Sh 1 are excluded). The pH values of surface A horizons range from 3.2 to 4.4, indicating very strong to strong soil acidity. Buried A horizons yield pH values ranging between 3.4 and 5.2 displaying very strong to moderate soil acidity (horizons of profile Sh 1 are excluded; Ad-hoc-AG Boden, 2005). 4.2.2. Geochronology The dated quartz showed good OSL dating properties typical for aeolian sediments. A set of 24 aliquots per sample was measured (Table 3). The resulting equivalent doses (ED) were mostly normally distributed, indicating that the dated quartz grains were well bleached during their last sedimentation cycle. HUB-0040 showed the lowest scatter within an aliquot set yielding a relative standard deviation (SD) of 4.8%. This value was also found applying the SAR protocol on an artificially irradiated aliquot set (dose recovery test of HUB-0003, SD: 4.7%). It is deduced, that a relative standard deviation of slightly below 5% describes the lowest scatter possible to reach for equivalent doses using quartz of the Boek dune field. However, some samples showed slightly broader distributions (HUB-0005, HUB-0039, HUB0041) or few outliers (HUB-0003, HUB-0005, HUB-0007, HUB-0034). Differential bleaching is the most probable explanation for this behaviour. To avoid age over-estimation, aliquots suspected to contain incompletely bleached grains were excluded from equivalent dose calculation. Following the approach of Fuchs and Lang (2001), individual ED values were added aliquot by aliquot beginning at the low end of any distribution until the target value of SD = 4.8% was reached or just exceeded. Only sample HUB-0033 (profile: Ba 3) showed clear evidence for insufficient resetting of the OSL signal during the last sedimentation cycle. The aliquots of HUB-0033 showed equivalent doses over a wide range between 1.73 and 9.74 Gy. Even the lowest ED would lead to an OSL age inversion in profile Ba 3. Moreover, no such high palaeodoses

were observed in any other sample from the Holocene dunes investigated in this study. One reason could be a mixing with poorly bleached moraine material found near the surface close to the profile. Hence, no results for equivalent dose and OSL age are given for HUB-0033 (Table 3). The water content of all samples was determined as percent of dry weight after oven drying at 105 °C for 24 h. The average moisture content was 1.8%, a standardised value of 3 ± 2% was chosen for dose rate calculation to account for seasonal variations and leakage of water during sample transport and storage. OSL datings on aeolian sands range from 0.77 ± 0.05 to 0.11 ± 0.02 kyr, representing ages in the Late Subatlantic. By means of a probability density function (Fig. 6) three well-defined phases of aeolian activity are visible in the late 13th century, the early 16th century and during the mid to late 19th century AD (Fig. 6). Radiocarbon ages ranging from 1495 ± 135 to 1224 ± 40 yr BP represent a humus accumulation on stable land surfaces (calibrated) between the 3rd and the late 9th century AD. These ages pre-date aeolian sedimentation on the outwash plain and lacustrine sedimentation at the lakeshore. However, a possible overestimation of age by older carbon in profile Boek 1 and sedimentological disturbances in profile Boeker Moor (Kaiser et al., 2002) as well as a possible contamination with younger carbon in profile Sh 1 must be taken into consideration. 5. Discussion 5.1. Holocene land use history and geomorphic response in the Mecklenburg Lake District Despite numerous archaeological sites in the study area reaching from the Mesolithic to the Slavonic Times (Fig. 1), there is no record of aeolian activity for that period, except for Zartwitz, where the pedostratigraphic bedding of pottery (profile Za 1) displays a former surface eroded by deflation due to settlement activities during the Bronze Age. Radiocarbon datings of peat and organic sands estimate stable surfaces from the Roman Iron Age to the Slavonic Times with deciduous forest vegetation, dominated by Fagus and Quercus (Kaiser et al., 2002; Fig. 7). Palynological data from various sites in the Lake Müritz region reflect a clear intensification of settlement activities during the Medieval period (13th to 14th century AD; Kaiser et al., 2002; Lampe et al., 2009). The 13th century AD is characterised by colonisation of Germans

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Fig. 7. Idealised landscape development of the dune area at Lake Müritz, comprising Late Holocene relief and soil formation, vegetation change and human impact.

in the whole region. Many settlements are mentioned in historic documents for the first time in this period (Voigtländer, 1982; Biermann and Mangelsdorf, 2004). Widespread forest clearance for settlement and land use resulted in deflation processes and accumulation of dunes. The deflation was so strong that Late Glacial and Holocene aeolian sediments were partly eroded down to the more resistant Late Glacial Finow soil, representing the Late Glacial surface. During the following accumulation of Medieval drift sands a secondary burying of the Finow soil occurred, which is reflected by a chrono-stratigraphic hiatus (e.g., profile: Ba 1). Several deserted settlement sites from the 14th century AD are recorded around Lake Müritz (Kaiser et al., 2002). The combined effect of socio-economic crises and negative feedbacks due to humaninduced environmental change is assumed to be the reason for this phenomenon. The decline of agricultural production during this period is explained, on the one hand, by nutrient loss or degradation of the

poor sandy soils, animal diseases as well as crop losses attributed to rainy years. On the other hand, increased flooding of agricultural land due to a striking increase of the lake level of Lake Müritz may have caused the abandonment of villages close to the lakeshore. In addition, plague epidemics and armed conflicts between the regions Mecklenburg and Brandenburg are documented (Voigtländer, 1982; Schoknecht et al., 1999; Kaiser et al., 2002; Biermann and Mangelsdorf, 2004). After these crises, a second distinct Late Medieval settlement phase occurred in the region during the 15th to 16th century AD (Schoknecht et al., 1999). The increasing food demand necessitated the renewed cultivation of previously abandoned fields and led to an expansion of agricultural land. This resulted in a second historical phase of increased aeolian activity. The drift sands reshaped the older dunes, primarily accumulated during the 13th century AD, and accentuated their morphology. During the second half of the Thirty Years War, the Müritz region experienced a second, very striking phase of desertion processes. The

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population declined by about 85% (Schoknecht et al., 1999). It increased until the beginning of the 18th century, but only reached one third of the pre-war level. The resulting low anthropogenic impact during the 17th and 18th centuries AD led to widespread reforestation with fastgrowing pioneer trees, such as pine. The topography was stabilised and a morphologically stable phase occurred until the establishment of glassworks in the early 19th century AD (Masurowski and Mombour, 2009). Firewood logging in the vicinity of the glassworks resulted in a final phase of aeolian activity, in which sands were deposited in the form of flat sand sheets covering existing dunes. After the glassworks closed due to economic constraints and governmental restrictions (also afforestation), the study area was increasingly forested. The topography has been stable since that time. The current vegetation consists mainly of pine forests. 5.2. Morphostratigraphical and sedimentological implications for drift sand areas In contrast to ice-marginal valleys, large river valleys and adjacent outwash plateau areas in Poland (Kozarski and Nowaczyk, 1991; Oczkowski et al., 2000) and in the Brandenburg region of NE Germany (Bussemer et al., 1998; Hilgers, 2007) as well as in NW Germany (Mauz et al., 2005; Tolksdorf et al., 2013), aeolian morphologies from the Early Holocene until the Late Subatlantic (older drift sands, according to Koster, 1982) have not been documented in the Mecklenburg Lake District so far (Dieckmann and Kaiser, 1998; Lorenz, 2007; Küster and Preusser, 2009; this study). In addition to this study, where a Bronze Age deflation surface has been detected, Küster et al. (2012) postulate aeolian minerogenic input into Lake Krummer See during the Bronze Age. This lake is located ca. 12 km southeast of Lake Müritz. Thus, in the region, prehistoric aeolian erosion processes especially during the Bronze Age can be assumed. In contrast, no corresponding aeolian deposits and morphologies could be detected on terrestrial sites so far. Undisturbed surfaces in NE Germany with long-term stable conditions from the Early Holocene to the Late Holocene are pedologically represented by podzolised brunic Arenosols, often covered by Late Subatlantic aeolian sand units and therefore protected from further degradation (e.g., Brande et al., 1999; this study). Since the transition from the Slavonic to the German Medieval up to the Modern Period (13th to 19th century AD), the aeolian dynamics at Lake Müritz led to accumulation of several aeolian units as a result of increased human impact. These aeolian deposits are separated by buried soils, which can be classified as Arenosols and podzolised Arenosols (IUSS Working Group WRB, 2006). The early stage of soil formation of these soils reflects rather short interim phases of stable surfaces between phases of aeolian activity (e.g., Behrendt et al., 2002). The widespread accumulation of the so-called younger drift sands (Koster, 1982) since the Medieval period represents the most distinctive spatial evidence of environmental change across all of Central Europe during the Late Subatlantic. These changes are caused by innovations in land use, for example the expansion of plaggen fertilising and agricultural areas in NW Europe (750 to 1200 AD; Behre, 1976; Castel et al., 1989; Alisch, 1995), the expansion of settlement and land use areas during the Medieval German Colonisation (after 1200 AD; Bork et al., 1998; Kaiser et al., 2002; Küster and Preusser, 2009) and mining in mountainous regions of Central Europe (Dulias, 1999). During the following Modern Times the chrono-spatially variable aeolian activity in NE Germany is significantly linked to human impact, induced either by wars (e.g., Thirty Years War) or economic pressures (Reinhard, 1953/ 1954; Janke, 1971; this study). The studied aeolian sequences at Lake Müritz consist of: (1) Late Glacial to Holocene, (2) multi-phase Late Subatlantic (composite dunes), and (3) single Late Subatlantic aeolian sand units, forming dune bodies of different shapes and heights. The individual units of a composite dune do not always have a relief forming character in contrast to the dune body as a whole. These morphologic–stratigraphic

features from the Late Subatlantic are a common phenomenon in NE Germany (e.g., Bussemer et al., 1998). The following sedimentation zones according to Castel et al. (1989) are spatially alternating: ‘blown-out’ (original soil has been eroded), ‘blown-over’ (sedimentation occurred on the original, not previously eroded surface) and ‘blown-on’ (sedimentation occurred on a previously blown-out surface). The formation of dunes at the edges of peat and lake filled basins was initiated by the local increase of ground roughness due to dense vegetation growing at these wet sites directly adjacent to agricultural fields. Previously accumulated sands, in contrast, are stabilised by a higher soil moisture leading to successive growth of dunes (e.g., Hassenpflug, 1998). The investigated drift sands are characterised by poorly sorted fine to medium grained sands. A general selection of grain sizes, by relative depletion of finer grain sizes over time, has not been found. Therefore, including morphological aspects of dune forms, their composition and structure, we assume multiple phases of patchy erosion and aeolian sand accumulation in our study area within a variable, open countryside. Sedimentary properties and stratigraphy of drift sands discussed in various studies throughout Europe, e.g. in the Netherlands (Koster et al., 1993), NW Germany (Pyritz, 1972; Alisch, 1995), NE Germany (Bussemer et al., 1998; Küster and Preusser, 2009; this study) and Poland (Kozarski and Nowaczyk, 1991) differ. So one can suggest that sedimentation of Holocene drift sands depends on the local sedimentary composition of the deflation (source) area, the chrono-spatial variability of the vegetation pattern (human disturbance) and finally the duration and intensity of aeolian processes.

6. Conclusions Despite numerous archaeological sites, no prehistoric Holocene aeolian sands have been recorded in the Mecklenburg Lake District so far. This can be explained either by the reactivation and incorporation of older drift sands during younger sedimentation processes and/or by the relatively low land-use intensity in the region from the Early to the Late Holocene. Since the Late Subatlantic, widespread and morphologically distinctive accumulation of younger drift sands has occurred. The Late Holocene chronology of aeolian activity can clearly be linked to the regional historical settlement/land-use history. Surfaces with short-term, weak soil formation are characterised by Arenosols and podzolised Arenosols. The studied aeolian sequences at Lake Müritz consist of (1) Late Glacial to Holocene, (2) multi-phase Late Holocene (composite dunes) and (3) single Late Holocene aeolian sand units. The alternating sequence of deflation and accumulation within drift sand areas is stratigraphically displayed by specific sedimentary zones (‘blown-out’, ‘blown-over’ and ‘blown-on’). The sedimentation of Holocene drift sands depends on the sedimentary composition of the deflation (source) area, the chrono-spatial variability of the vegetation pattern (human disturbances) and the duration and intensity of aeolian processes.

Acknowledgments First of all we would like to thank the Jost-Reinhold-Stiftung (Ankershagen) for the financial support of our research and the Müritz-Nationalpark for the administrative and logistic support. We are also very grateful to Jan Lentschke (Berlin), Matthias Schwabe (Hohenzieritz), many students from the Universities of Greifswald and Berlin (Humboldt University) for the participation and support during field work and Mabel Strecker (Fauler Ort) for the great service in our accommodation. Our research is embedded in the Virtual Institute of Integrated Climate and Landscape Evolution Analysis (ICLEA) and the TERENO initiative of the Helmholtz Association. We thank Christina Hierath for proofreading the English language. Finally we are grateful to two reviewers for their helpful comments on the manuscript.

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