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The focus of this study is on the geochronological and paleo-climatic characterization of late Pleistocene glaciations in Turgen and the Khangai Mountains located in central and western Mongolia. These two mountain ranges form a 700 km long NW-SE transect through Mongolia and allow assumptions of the temporal and causal dynamics of the regional late Quaternary glaciations and their correlation to other mountain glacier records from Central and High Asia. In order to evaluate extent and timing of the Pleistocene glaciations in Mongolia, geomorphological mapping and cosmogenic radionuclide (CRN) surface exposure dating (10Be) were carried out in four valley systems located in the Khangai and Turgen Mountains. Additionally, a coupled 2-D surface energy balance and ice flow model was used to determine steady-state conditions for glaciers under various climatic scenarios. With this model it is possible to test combinations of temperature and precipitation settings, which would produce glacier configurations that fit the field-mapped ice extent. In total, 47 glacial boulders and roche moutonnées were sampled, prepared and AMS measured to determine the absolute timing of moraine formation and ice retreat based on 10Be surface exposure dating. Of these, 27 samples were obtained from the Khangai Mountains (three separate moraine sequences) and 20 samples were taken from the Turgen Mountains (two moraine sequences). The dating results (presented as minimum ages) give evidence for a late Pleistocene maximum ice expansion during late MIS 5 (81−78 ka) and major ice advances during MIS 2 (26−20 ka) in both mountain ranges. Only in the Khangai Mountains (central Mongolia) very significant glacier advances also occurred during mid-MIS 3 (49−35 ka), which exceeded the ice limits set during the MIS 2 glaciation. A final ice position, constructed shortly before the onset of full ice retreat was formed between 19-16 ka, and is likely to represent a recessional ice stillstand, or alternatively a final ice readvance during the early part of the last-glacial-interglacial-transition (LGIT) in both mountain ranges. Energy/mass balance and ice flow modeling results suggest that climatic conditions during the MIS 5 and MIS 3 maximum advances in the Khangai Mountains were depressed between a ∆T of -6.0 to -5.2 °C with a precipitation factor of 1.25-1.75 (P = 125-175 %, compared to modern conditions), and a ∆T of -5.3 to -4.4 °C (P = 75-125 %), respectively. For the MIS 2 ice advances modeling results from the Turgen and Khangai Mountains suggest a temperature depression ∆T of -5.7 to -4.6 °C (at 22 ka; P = 25-50 %) in the East-Turgen, and a ∆T of -7.5 to -6.6 °C (at 20 ka; P = 25-50 %) in the Chulut area (Khangai Mountains). These results document a 1.8 - 2 °C difference of the modeled temperatures required to expand the studied paleo-glaciers in the Turgen and Khangai mountains to their field-mapped MIS 2 ice limits, highlighting a spatially differentiated pattern of paleo-temperature lowering across the studied 700 km NW-SE transect. Taken together, the presented record indicates that the largest ice advance in both investigated mountain ranges occurred during the MIS 5 / MIS 4 transition, despite earlier suggestions by previous studies that the local glacial maximum would be associated with the coldest periods of the last glacial cycle (i.e. MIS 4 or MIS 2). Glacier systems in the Khangai Mountains also increased substantially during MIS 3 (local LGM) in response to cool but comparable wet conditions, probably with a greater-than-today input from winter precipitation and an additional input of recycled moisture from expanded paleo-lakes in the Valley of the Great Lakes. The lack of a severe cooling during the MIS 3 ice advances, and probably also during the late MIS 5 ice expansion, suggests that variations in atmospheric circulation patterns, with its significance for controlling the regional precipitation/moisture supply, was a key driver for these late Pleistocene ice advances in Mongolia. This notwithstanding, there is also clear evidence for the development of an extensive glaciation during MIS 2, coinciding with a period of severe cooling and hyperarid conditions. This highlights that glacier systems in Mongolia responded sensitively, both, to variations in moisture supply and its seasonal distribution, and to the marked insolation minima during the last glacial cycle.
For many years, rangeland ecologists have debated about whether the state of semi-arid and arid rangelands is the expression of an ecological equilibrium or non-equilibrium dynamics reached in response to grazing livestock. Since the problem has been considered at different spatial scales, it is recognised that the competing concepts of equilibrium and non-equilibrium dynamics need to be integrated. Furthermore, the role of environmental variables as vegetation driving factors has long been ignored in the discussion on grazing effects on ecosystems. Present thesis, examines the dependence of plant communities on environmental in particular site-ecological conditions in three ecosystems of Western Mongolia established along a precipitation gradient to detect the vegetation-driving ecological factors involved. Furthermore, grazing impact is exemplary assessed in a desert steppe at additional spatial scales of plant communities and population. At the landscape level, a classification of plant communities in dependence on environmental conditions is carried out. Additionally, the investigations focused on the impact of grazing on soil and on the occurrence of grazing-mediated plant communities. Data were sampled along an altitudinal gradient between 1150 m to 3050 m a.s.l. from arid lowland with desert steppe via semi-arid mountain steppe to humid alpine belt. Within each altitudinal belt, data sampling was carried out along grazing gradients, established from grazing hot spots to areas distant from them. By means of an environmentally based vegetation classification, factors with highest explanation values for largest variation in vegetation were identified and considered as most responsible for vegetation patterns. To validate and affirm the classification, three different statistical methods are applied: environmentally adjusted table work of vegetation relevés supported by cluster analysis of species distribution, detrended correspondence analysis of vegetation data separately from environmental data, and the principle component analysis of only environmental data. Vegetation-driving factors change along the altitudinal gradient from abiotic forces in the desert steppe, as e.g. altitude and soil texture, to abiotic and biotic forces in the alpine belt represented by soil texture, soil nutrients and grazing. Vegetation and soil of all ecosystems respond to grazing but with different patterns and to a different extent. While desert steppe does not indicate grazing communities, mountain steppe demonstrates grazing communities at fertilised sites and alpine belt at nutrients depleted sites. Thus, the grazing sensitiveness of the ecosystems is assumed to be linked with plant productivity and the role of vegetation as site-determining factor (Chapter 2). To examine grazing impact at lower spatial scales on desert steppe as the ecosystem with lowest grazing sensitiveness at the landscape scale, at community scale the total number of species, the total vegetation cover, the percentage of annual species, the cover of annual species, and properties of soil nutrient along gradients of grazing intensity within three different communities were assessed. Vegetation parameters respond to grazing in different ways, and the responses of the same parameters vary between plant communities. Correlations with grazing intensity indicate only partly statistical significance. Significant correlations of grazing intensity with concentrations of soil nutrient point to eutrophication in two communities. A comparison of vegetation and soil properties refers to a greater indirect influence of grazing via increased soil nutrients than the direct effect on vegetation (Chapter 4). At the population level, data about stand density, aboveground biomass, individual plant weight, and the proportion of flowering plants of the dominant dwarf semi-shrub Artemisia xerophytica were collected along a grazing gradient. Soil data were used to distinguish between grazing and edaphic influences. All parameters of Artemisia xerophytica reflect the assumed gradient of grazing intensity up to 800 m distance from the grazing hot spot. As grazing pressure decreases, plant density and total biomass per plot increase. The average shrub weight, an indicator of plant vitality, is related to both: distance from the grazing hot spot and stand density, which may be explained by additional intraspecific competition at higher densities. At a longer distance, these effects are masked by variations in soil parameters determining water availability, leading to quite similar degradation forms. These results are in contrast to other studies carried out at the scale of plant communities which did not detect significant changes along a grazing gradient. One explanation is the different map scale: the study took place only within a single plant community comparing populations of one species (Chapter 3). The comparative study demonstrates that even arid desert steppes of western Mongolia display equilibrial and non-equilibrial properties, depending on the observational scale: while no grazing mediated plant communities could be identified at the landscape scale as predicted by the non-equlilibrium model, at the community level vegetation parameters imply an intermediate position between equilibrium and non-equilibrium system. At the population level, the results clearly reflect the grazing gradient as predicted by the equilibrium model (Chapter 4). As a consequence, the assessment of vegetation dynamics and grazing impact in rangelands requires a multiple-scale approach that duly considers different vegetation properties responding differently to grazing, climatic and edaphic variability at different spatial scales. It is further suggested, that future research should draw comparisons between landscapes that co-evolved with herbivory, and those that did without (Chapter 4).