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In the nineteenth century, two Neolithic axe-heads were reported from the Michelsberg enclosure system at Kapellenberg. The recent identification of an unusually large tumulus, from which the axe-heads were almost certainly once recovered, reveals that socio-political hierarchisation, linked to the emergence of high-ranking elites in Brittany and the Paris Basin during the fifth millennium cal BC, may have extended into Central Europe.

The Plio-Pleistocene expansion of Eastern Africa savanna ecosystems was a major driver for morphological and behavioral innovations in hominin evolution. Most evidence for hominin ecosystem reconstructions originates from the Eastern Rift in today's Somali-Masai Endemic Zone. We provide stable carbon (δ 13 C) and oxygen (δ 18 O) isotope data from 22 bovid, equid, suid, hippopotamid and elephant teeth from the southern part of the East African Rift and supplement these by δ 18 O values of present-day meteoric water. This region (Karonga Basin, Malawi) hosts remains of Homo rudolfensis and Paranthropus boisei . It is situated between hominin-bearing sites in Eastern and Southern Africa and therefore fills an important geographical gap for hominin evolution. Tooth enamel δ 13 C and δ 18 O data of 14 large-bodied mammalian herbivore species from Units 2 and 3 (ca. 4.3 to 0.6 Ma) in the Chiwondo Beds provide information about foraging strategies and vegetation patterns. Our stable isotope data reflect C 3 -dominated ecosystems that permitted access to open C 4 -environments for migratory mammals. Many analyzed taxa show evidence for mixed diets with high abundances of C 3 -biomass consumption; only selected bovids were specialized grazers. δ 18 O of present-day meteoric water reflects rainfall amount and seasonality, elevation, and lake evaporation. δ 18 O values of Karonga Basin herbivore enamel are generally low and cover values similar to present-day drinking water, indicating both, evaporated and freshwater sources. Comparison of δ 13 C values from the Karonga Basin with other Eastern African herbivore communities reveals significant differences in dietary patterns with much more generalized mixed C 3 /C 4 , and pure C 3 feeding behaviors in the Malawi Rift. Similarly, enamel δ 18 O values are lower than in most Plio-Pleistocene Eastern African herbivores, suggesting more humid conditions. Collectively, our data support models in which early hominin foraging activity included access to C 3 -dominated biomes, complicating traditional interpretations linking early human evolutionary innovations to a shift towards savanna habitats.

Landscape and soils around the prehistoric Bronze Age site of Kamennyi Ambar, southern Trans-Urals, have been studied. The topography of the Trans-Ural peneplain was formed by denudation during Mesozoic and Tertiary. The resulting gently undulating plain was subsequently dissected during Pleistocene under periglacial climatic conditions, and wide valleys with gentle slopes were formed. The saprolized pre-quaternary rocks are covered by thin layers of quaternary sediments, which are sometimes loess-containing. Deposits of in-situ loess are almost absent. Most probably, deluviation under periglacial conditions played the dominant role and prevented the formation of loess deposits. Thin loess deposits are preserved only in some flat watershed positions. The Quaternary layers sometimes contain strongly weathered coarse bedrock components indicating a solifluidal genesis of the cover beds on the slopes. The degree of weathering of the autochthonous components increases towards the water divide where the cover beds consist almost completely of pre-Quaternary saprolite. The slopes of the Karagaily Ajat valley are structured by numerous smaller tributary valleys which usually have a yellow-brown loam fill and show in their lower parts gully-like linear erosion features. Decalcified Haplic Chernozems are prevalent soils in the fills of the tributary valleys, at the lower slopes of the Karagaily Ajat-valley, and in the loams of the Lower Terrace. When clay cutans and coatings were observed in the subsoil the soils were identified as Luvic Chernozems. On the gentle slopes, Mollic Leptosols or Leptic Regosols (Mollic) are developed in thin cover beds. Up the slope, the depth of the humus horizons decreases. When examining the layer succession of the near surface underground and the associated soils along transects across the tributary valleys, it was found that the thickness of the cover beds on the slopes increases towards the valley floor. In the soils of the Lower Terrace varying salt contents can be found. Mollic Solonetz were identified therein. Within the excavation area in Kamennyi Ambar, Anthrosols and Solonetz were found in the compacted layers of the older Sintashta culture, while Haplic Chernozems (colluvic) with similar features like the virgin soils have developed in the fillings of younger pit houses.

The bedrock of the Spessart Mountains is covered by Pleistocene periglacial slope deposits (PPS- Ds). These slope deposits are supposed to have formed in a periglacial environment by a variety of processes. For this study soil profiles in the Spessart Mountains were analyzed with respect to features elucidating processes forming and transforming PPSDs. Field and laboratory analyses were complemented by micro- morphological investigations to gain more detailed information. The results verify aeolian sedimentation, solifluction and cryoturbation as most important formation processes. Furthermore, several findings sug- gest the influence of additional genetically active processes. PPSDs provide the parent material for Holocene soil formation. In addition, they experience alteration by bioturbation and anthropogenic influence on relief and soil. Pedogenic transformation is dependent on the PPSDs material composition. Particularly the content of silt-sized allochthonous material controls the efficacy of silicate weathering and depth of soil development. The coincidence of pedogenic boundaries and layers often reported in the literature is partly falsified: Eluviation and illuviation of clay is not separated at the boundary between upper and intermediate layer. PPSDs experience strong alteration by bioturbation: This process may transform characteristics that could point to formation processes. Furthermore, thin sec- tion analyses support the distinction of Holocene colluvium and PPSDs.

Anthropogenic impact in prehistoric settlements results in a considerable alteration of soil microbial communities depending on intensity and the character of human activities. This paper present a case study from a Late Bronze Age settlement located in the high-mountain part of the North Caucasus (Russia). The site represents a community, which presumably specialized in intensive livestock herding. Samples from settlement soils anthropogenically affected in the past and unmodified background soils were taken and studied. Of particular interest were divergences in soil microbial communities, expected to indicate different activities and animal presence in the site. The total microbial biomass, their respiratory activity, the biomass of fungal mycelium and the proportion of dark-colored hyphae were determined, as well as the quantitative state of keratinophilic fungi. The microbial characteristics vary considerably within the settlement locations, and contrast sharply with the reference soils exterior to the archaeological site. The cultural layer has higher percentage of active metabolizing microorganisms, whereas the total microbiological biomass is considerably lower than in the unmodified soils from the surroundings. A determining factor to transform the respiratory activity of microorganisms, in both qualitative and quantitative aspects, is the composition of the organic material which has been accumulated in the ground as a result of various human activities in the past. The cultural layers contain microorganisms, which can be reactivated when glucose is added. In the anthropogenically unmodified soils surrounding the prehistoric settlement, in contrast, 97% of the cells cannot be reactivated. Based on the mycological characteristics of the studied cultural layers and unmodified soils, in particular with regard to the total biomass of fungi mycelium, the dark pigmented fungal biomass, and the existence of keratin-decomposing soil fungi, detailed information about activity areas and their specific usage is given. The use of bio-indicators allows not only diagnosing anthropogenic impact in soils as such, but also significantly complements description of cultural layers of activity areas in the settlement, specifying their purpose. The paper presents the microbiological analyses applied and, moreover, discusses the potential of this approach as a non-destructive prospecting method on archaeological sites.

stacking of periglacial layers: A differentiation of eluvial (E-) and illuvial (Bt-) horizon is already developed within the upper layer. The intermediate layer carries the main argillic horizon of those profi les whereas the within the upper layer. The intermediate layer carries the main argillic horizon of those profi les whereas the basal layer is only marginally affected by soil formation. By the help of soil micromorphology it was possible basal layer is only marginally affected by soil formation. By the help of soil micromorphology it was possible to identify numerous fragments of paleosol material within the intermediate layer (2Bt-horizon) accountto identify numerous fragments of paleosol material within the intermediate layer (2Bt-horizon) accounting for large proportions of the total clay content of this horizon. While the formation of the upper layer, ing for large proportions of the total clay content of this horizon. While the formation of the upper layer, parts of the intermediate layer were reworked and incorporated into the newly formed slope deposit. As a parts of the intermediate layer were reworked and incorporated into the newly formed slope deposit. As a result, the lower part of the upper and the whole intermediate layer contained large amounts of clay before result, the lower part of the upper and the whole intermediate layer contained large amounts of clay before the onset of Holocene pedogenesis. Recent lessivation, evidenced by undisturbed clay illuviations, affected the onset of Holocene pedogenesis. Recent lessivation, evidenced by undisturbed clay illuviations, affected the profi le. Consequently this soil formation masks prior differences in clay content due to included paleosol the profi le. Consequently this soil formation masks prior differences in clay content due to included paleosol material. Soil formation is dominated by the paleosol remnants and therefore elucidates the impact of late material. Soil formation is dominated by the paleosol remnants and therefore elucidates the impact of late glacial conditions on Holocene soils. glacial conditions on Holocene soils. Besides, a Luvisol was identifi ed which was not formed in periglacial slope deposits but in Holocene colBesides, a Luvisol was identifi ed which was not formed in periglacial slope deposits but in Holocene colluvium. In this case paleosol remnants were totally absent. Hence, a precise reconstruction of Luvisol-genesis luvium. In this case paleosol remnants were totally absent. Hence, a precise reconstruction of Luvisol-genesis is enormously improved by micromorphological analyses. is enormously improved by micromorphological analyses.

The vegetation of the northern Upper Rhine Graben (southwestern Germany) is reconstructed for the end of the Lateglacial and the Holocene by means of palynological analyses in combination with AMS 14c dating. Analogous to adjacent lowland areas, the Younger Dryas climatic deterioration did not result in a complete deforestation of the area and open pine woodlands with locally birch stands and shrubs persisted. A subdivision of the Younger Dryas period, into a humid first phase, followed by a dry second phase was also reflected in our records. For the Holocene, the pollen diagrams show two regionally different vegetation developments, related to substrate and variations in annual precipitation: in the south the ‘classical’ succession of pine then hazel is followed by other deciduous trees, whereas in the northern part, pine kept its dominance far into the Subboreal.

The development of the main northeast Nigerian river complex, the Komadugu System, is reconstructed, and the possible relation to Holocene environmental changes is investigated. At this stage of research, some field work, concentrating on the lithostratigraphy of the alluvial deposits, has been carried out along the middle and lower courses of the Komadugu Yobe and the Komadugu Gana and is supported by laboratory analyses of sediments and soils. The data obtained so far confirm earlier suggestions that the alluvium can be distinguished into Late Holocene floodplain deposits and a wider, fossilized terrace complex that may reflect a rather palustrine to lacustrine palaeoenvironment possibly related to the Early and Mid-Holocene Lake Megachad.

The development of East African savannas is crucial for the origin and evolution of early hominins. These ecosystems, however, vary widely in their fraction of woody cover and today range from closed woodland to open grassland savanna. Here, we present the first Plio-Pleistocene long-term carbon isotope (δ13C) record from pedogenic carbonate and Suidae teeth in the southern East African Rift (EAR). These δ13C data from the Chiwondo and Chitimwe Beds (Karonga Basin, Northern Malawi) represent a southern hemisphere record in the EAR, a key region for reconstructing vegetation patterns in today's Zambezian Savanna, and permit correlation with data on the evolution and migration of early hominins in today's Somali-Masai Endemic Zone. The sediments along the northwestern shore of Lake Malawi contain fossils attributed to Homo rudolfensis and Paranthropus boisei. The associated hominin localities (Uraha, Malema) are situated between the well-known hominin bearing sites of the Somali-Masai Endemic Zone in the Eastern Rift and the Highveld Grassland in southern Africa, and fill an important geographical gap for hominin research. Persistent δ13C values around −9‰ from pedogenic carbonate and suid enamel covering the last ∼4.3 Ma indicate a C3-dominated closed environment with regional patches of C4-grasslands in the Karonga Basin. The overall fraction of woody cover of 60–70% reflects significantly higher canopy density in the Malawi Rift than the Eastern Rift through time. The discrepancy between the two savanna types originated in the Late Pliocene, when the Somali-Masai ecosystem started to show increasing evidence for open, C4-dominated landscapes. Based on the Malawi δ13C data, the evolution of savanna ecosystems in Eastern Africa followed different patterns along the north-south extent of the EAR. The appearance of C4-grasses is considered a driver of evolutionary faunal shifts, but despite the difference of ecosystem evolution in the north, similar hominins and suids occurred in both landscapes, pointing to distinct habitat flexibility and also nutritional versatility.

Three time slices were focused on reconstruction of the Lateglacial and Holocene landscape evolution in the northern Upper Rhine–Rift Valley. The fluvial history of the northern Upper Rhine River during the last 15,000 years is characterised by repeated rapid changes of fluvial morphodynamics and sedimentation conditions. In consequence, the floodplain of the Rhine River may be subdivided into three different meander generations, which differ mainly on morphological, lithological and pedogenetical criteria. Using complementary dating techniques (pollen, IRSL, AMS 14C), a detailed chronology was obtained for the floodplain sediments (e.g. overbank deposits, peat bogs, aeolian dune sands) of the Rhine River and its tributary, the Neckar River (Bergstrasen-Necker). While the latter became completely abandoned during the Younger Dryas period, the Rhine River probably started meandering at the onset of the Allerod period and most likely continued its meandering pattern since the Lateglacial. The change from the Oldest Meander Generation to the Older Meander Generation occurred during the late phase of the Atlantic period. However, the timing of the onset of the Younger Meander Generation is not known in detail, at present. Probably, it started to develop in the late Subboreal period or at the transition from the Subboreal to the Subatlantic period.

Case numbers of endemic Ca-deficiency rickets (CDR) have been reported to be alarmingly rising among children of subsistence farms in developing countries within the last 30 years. Fluoride toxicities in the environment are known to not be related to the disease. To investigate if, instead, CDR is caused by a nutrient deficiency in the environment, subsistence farms in an endemic CDR area near Kaduna, northern Nigeria, were investigated for bedrock, slope forms, soil types, and soil characteristics. The natural environment was investigated according to the World Reference Base, soil texture was analysed by pipette and sieving, and plant-available macronutrients were determined using barium-chloride or Ca-acetate-lactate extraction. The analyses showed that granite and slope deposits were the dominant parent materials. The typical slope forms and soil types were Lixisols and Acrisols on pediments, Fluvisols in river valleys, and Plinthosols and Acrisols on plains. Compared with West African background values, all of the soils had normal soil textures but were low in macronutrients. Comparisons to critical limits, however, showed that only the P concentrations were critically low, which are typical for savanna soils. A link between nutrient deficiency in soils and CDR in the Kaduna area was therefore considered unlikely. Vereinigung der Freunde und F¨orderer of the University of Frankfurt DAAD BMBF

To obtain a broad view of the ages of dunes in Borno State, Nigeria, 23 samples were dated using quartz grains. Results from seven selected samples are discussed in this paper. For all these samples problems arose in the evaluation of the annual doses as the contents of U, Th and K are low. In total, three independent methods for the determination of these radioactive isotopes were tested. The results sometimes differ by more than a factor of two. This leads to the general conclusion that the thermoluminescence ages of samples with small U, Th and K contents are not very reliable. The data from alpha counting are preferable for the evaluation of ages.