The article presents the results of a palynological study of the Middle Paleolithic monument Chagyr Cave (Altai). The sediments comprising the Sibiryachikhinsky technocomplex of the Middle Paleolithic of Altai accumulated during the period corresponding to the end of the fourth stage of the marine isotope scale and belong to the final stage of the Ermakov glaciation. The results of palynological analysis indicate the existence of steppe landscapes in dry and cold climates at this time.

Key words: palynological analysis, vegetation reconstruction, Ermakov stadium, MIS4, Paleolithic, Chagyr cave, Siberia.

Introduction

Currently, when reconstructing the ancient human habitat, a comprehensive interdisciplinary natural science approach is a priority. At the same time, paleoreconstruction of the natural conditions of mountain territories is complicated by the peculiarities of the structure of ancient and modern relief, the influence of macro-, meso - and microclimate, possible redeposition of geological sediments, insufficient material for direct dating, etc.Meanwhile, in such areas there is often a concentration of archaeological sites of different ages.

One of the leading methods of studying the deposits of cultural layers is spore-pollen analysis. To date, considerable palynological data have been accumulated on Paleolithic sites in the Altai region (Bolikhovskaya et al., 2011; Bolikhovskaya and Markin, 2002; Bolikhovskaya and Shunkov, 2005; Derevyanko et al., 1999, 2000; Malaeva, 1995, 1998, 1999; Prirodnaya sreda..., 2003).

This article presents the results of a palynological study of the deposits of the Chagyr Cave, where, as in the Okladnikov Cave, "dezhetoid" artefacts comparable to the Mousterian complexes of Transcaucasia, Southwestern Europe, and Western Asia were found (Derevyanko, Markin, and Zykin, 2009). The study of the archaeological material of these two sites made it possible to identify the Sibiryachikhinsky variant, which differs from other variants of the Middle Paleolithic of Altai (Derevyanko, 2010).

District and research object

The Chagyr Cave (51°26'34.6" N, 83°09'18.0" E) is located in the middle mountain belt on the left bank of the Charysh River, draining the spurs of the northern slope of the Tigiretsky Ridge (Krasnoshchekovsky district of Altai Krai). It has a northern exposure, is located at an altitude of 25 m above the river level, the estuary part opens onto the vertical surface of the ledge of the basement terrace with a height of 50-60 m, composed of massive gray Lower Silurian limestones. The cave has two halls with an area of approx. 130 ^m2. One of them gives rise to three almost completely buried horizontal and vertical galleries. The subterral layer of the cave includes seven lithological formations, among which the Holocene ones are distinguished

(layers 1-4) and Pleistocene (layers 5-7) deposits. Paleolithic artifacts are associated with the sixth layer (Derevyanko et al., 2010).

The climate of the area where the Chagyr Cave is located is continental with an average temperature of -14.5 °C in January and +17.9 °C in July. The annual amount of atmospheric precipitation is 430 mm (Atlas..., 1991). Modern vegetation in the vicinity of the monument is represented by real mountain-steppe turf-grass steppes with the participation of grasshoppers Stipa zalesskii, S. cappilata, S. pennata, Spiraea Spiraea trilobata, rose hips Rosa spinosissima. In the scheme of botanical and geographical zoning of Altai, the studied territory belongs to the Middle Karysh taiga-shrub-forest-steppe region of the Kolyvansko-Charysh taiga-shrub-steppe district of the Western Altai Province. The vegetation of the region as a whole is mosaic and includes both steppe groups, associations of steppe meadows, and shrubs (Ogureeva, 1980). The latitudinal Tigiretsky and Korgon ranges located south of the cave are the first to stand in the way of wet westerly winds, which ensures the development of forest and meadow vegetation in their lower parts, including a wide distribution of black taiga and forests with Siberian pine (Kuminova, 1960).

Age of sediments containing Paleolithic artifacts

The material for radiocarbon dating was collagen isolated by a new method [Talamo and Richards, 2011] from bison bones with signs of human use (slicing) found in the sixth layer (Table 1). Samples from layers 6b and 6b/1 were used to obtain dates in the range of 52-45 and > 52 thousand liters.n. This makes it possible to attribute these deposits to the end of the Ermakov (Zyryansky) glaciation or MIS4 (according to Bassinot et al., 1994). The use of a complex of geological methods also suggests that most of the sixth layer's thickness was formed at the specified time and represents the Tulinsky loess (Markin, 2011), the final phase of which corresponds to the fourth stage of the marine isotope scale (Zykina and Zykin, 2008).

Methods and materials

For palynological analysis in 2008 - 2009, 103 samples (50-100 g of dry matter each) were taken from all layers with an interval of 15-20 cm. They were treated according to the separation method of V. P. Grichuk (Pollen analysis, 1950), combined with the method of processing palynological samples (according to [Faegri and Iversen, 1989]). Before separating the sediment in a heavy liquid, hydrofluoric acid was added to it to remove silicates. Pollen grains and spores were counted using a light microscope with x400 magnification. Determinants and atlases were used to determine their taxonomic affiliation (Kupriyanova and Aleshina, 1972,1978; Reille, 1992, 1995, 1998).

Samples prepared for spore-pollen analysis were also used to count non-pollen palynomorphs (NII). The results of palynological studies are reflected in diagrams constructed using the TCa and TiliaGraph programs (Grimm, 1991). Cluster analysis of spore-pollen spectra, taking into account their stratigraphic alignment, was performed using the CONISS program (Grimm, 1987).

Vegetation types were identified based on the obtained palynotaxon spore-pollen spectra by biomization (Prentice et al., 1996). The essence of the method is that each palynotaxon, depending on its life form, ecology and-

Table 1. AMS ^14C-dates obtained from Bison sp. bones found in the sixth layer of the Chagyr cave

In addition to some climatic indicators, it falls into a certain functional type of vegetation (FTR), and if its constituent species have different ecology, then into several. The result of the distribution of taxa by FTR is expressed as a FTR-taxon matrix. Functional vegetation types are combined into biomes, forming a FTR-biome matrix. A set of specific PTRS characterizes a particular biome. As a result, a taxon is created-a biome matrix in which each palinotaxon is assigned to one or more biomes.

Quantitatively, the proximity of a set of taxa of a palynological sample to a certain biome (biome weight) is calculated by the formula [Ibid.]:

where A _ik is the proximity of a set of taxa of palynological sample i to biome k; ∑j is the sum of all taxa of the palynocomplex; δ_tjis the taxon-biome matrix for biome i and taxon j; P _ikis the taxon content as a percentage; θ _j is the threshold for taxon inclusion in calculations, expressed as a percentage. The mathematical operation of extracting the square root is used to stabilize different percentages of taxa and increase the sensitivity of the method to taxa that do not show a large abundance. The inclusion of a taxon in the FTR and biomes has a certain statistical threshold (assumed 0.5 %), which is necessary to exclude taxa with a single content of pollen grains or redeposited forms. The result of reconstruction is expressed quantitatively as the weight of each biome in a certain spectrum. To calculate it, the method relies on the provisions of fuzzy logic. The biome with the highest weight will be decisive, and if there are several with the same weight, the one with the lowest number of FTRS will be decisive.

Before applying the biomization method to the deposits of the Chagyr Cave located in a mountainous area, it was tested on 47 subfossilized spore-pollen spectra obtained in various mountain landscapes of the Russian Altai (Rudaya, 2010). Biomization showed that the coincidence of actual vegetation types and those reconstructed using subfossilized spectra is 61 %. To assess the consistency of the observed and reconstructed biomes, the Kappa statistical criterion was used (Monserad, 1990). The kappa value calculated from Table 2 is 0.42, which indicates a noticeable consistency [Prentice et al., 1992]. This good result allows us to use the biomization method to interpret data from the palynological analysis of Chagyr Cave deposits.

Table 2. Comparison of numerical values of reconstructed biomes and those actually observed at sampling points

Results of analysis and interpretation of palynological data

Spore-pollen records from the 2008 and 2009 sections in the Chagyr cave revealed several palynological complexes whose boundaries do not always coincide with the boundaries of lithological layers. Based on the obtained taxa, functional vegetation types and their corresponding dominant biomes were identified (Table 3).

Palynological characteristics are given both for individual lithological layers and for functional clusters.

Layer 1. Herbaceous palynotaxons predominate, with significant participation of sagebrush (Artemisia), Asteroideae (Asteroideae, Cichorioideae), and grasses (Roaceae). The time of accumulation of the layer is characterized by steppes that correspond to the present-day composition of the palynological spectra (Figs. 1, 2).

Layer 2. Compared to layer 1, the proportion of Cichorioideae and mixed grasses pollen increases. The reason for the increase in the number of pollen grains in the Cichorioideae subfamily of Asteraceae, which includes a large number of synanthropic species and weeds (dandelion, sow thistle), may be the economic activity of people who lived in the cave (see Figures 1, 2).

Layer 3 (section description 2009). Herbaceous palynotaxons with Asteroideae, Cichorioideae, and mixed grasses predominate. The percentage of pollen of Siberian pine(Pinus sibirica) and common pine (P. sylvestris), fern spores increases. In general, steppe communities are being reconstructed, although the influence of the forest component is also increasing (see Figures 1 and 2).

Layer 4. Apparently, filling of anthropogenic origin (in the 2009 section is absent). Cichorioideae pollen dominates. The presence of haze, grasses, and sagebrush is noticeable (see Figure 1).

Layer 5. This layer, unlike the three overlying layers, is characterized by an increased content of tree pollen. The upper part of the spectrum contains a significant proportion of coniferous pollen grains: Pinus sibirica, P. sylvestris, Abies fir, and Picea spruce (see Figs. 2, 3).

Table 3. Dominant biomes reconstructed from palynological data from Chagyr cave deposits

Fig. 1. Results of palynological study of layers 1-4 of the 2008 section (squares K7, L7). Other/Tr. - ratio of woody and herbaceous vegetation.

2. Results of palynological study of layers 1-3, 5 of the 2009 section (squares L8, H8). Dr. / Tr. - ratio of woody and herbaceous vegetation; CLL - cold deciduous forests.

3. Results of palynological study of layers 3, 5-7 of the 2008 section (squares L6, M7).

4. Results of palynological study of layer 6 of the 2009 section (squares L8, M8, and H8).

5. Results of palynological study of layers 6B2 and 7 of the 2009 section (squares L8, M8).

See Figure 2 for additional information.

Layer 6a. In general, the pollen of herbaceous plants (Poaceae, Asteroideae, and Cichorioideae) is predominant and steppe communities are being reconstructed, although conifers are still significantly present in the upper part of the layer (Figs. 3, 4).

Layers 6b and 6b/1. Pollen of herbaceous plants absolutely dominates. The participation of cereals significantly increases in the palyn spectra of the 2008 section, and Cichorioideae and Asteroideae in the spectra of the 2009 section. Steppe coenoses are reconstructed by the biomization method (see Fig. 3,4).

Layer 6b / 2. In a single sample from this layer in the 2009 section, the proportion of tree pollen, mainly represented by pine trees, reaches 80%. Two samples from the 2008 section contain pollen grains of cereals, Betula spp. and Asteroideae (see Fig. 3, 5).

Layer 7. It is characterized by a low concentration of pollen and spores, and many samples are "empty". From four representative spectra (the content of pollen and spores in the samples allowed us to calculate a statistically significant number of grains) taiga biomes are reconstructed for three of them, and cold deciduous forests are reconstructed for one of them (see Figures 3, 5).

In layers 5 and 6 of the 2008 section, clusters whose boundaries do not coincide with the boundaries of lithological layers are identified (see Figure 3).

Cluster I (depth 35-95 cm). It combines the spore-pollen spectra of layer 5 and the upper part of layer 6a. A distinctive feature of the cluster is the relatively high percentage of tree pollen (Pinus sibirica, P. sylvestris, Picea). In the upper part of layer 6a, the largest amount of it is noted in the divisions of the sixth layer. Herbaceous taxa are mainly represented by Compositaceae (including Cichorioideae and Artemisia), grasses, and mares.

Cluster II (depth 95 - 130 cm). It includes the palynospectra of the lower part of layer 6a and the upper part of layer 6b. The cluster is characterized by a sharp decrease in the content of tree pollen, although in some spectra it still reaches 20 %.

Cluster III (depth 130 - 160 cm). It includes the spore-pollen spectra of the lower part of layer 6b and the upper part of layer 6b / 1. Here the pollen of trees almost completely disappears. Another feature is the increased role of cereals.

Steppe is the dominant biome reconstructed for all three clusters.

Samples from the lower part of layer 6b / 1, as well as from layers 6b/2 and 7 of the 2008 section contain pollen grains and spores in minimal concentrations, which makes clustering impractical (see Figure 3).

Non-pollen palynomorphs are mainly represented by chlamydia spores of the endomycorrhizal fungus Glomus, which is found in all geological layers and can serve as an indicator of soil erosion,

including as a result of human activity [van Geel et al., 2003]. The Holocene strata contain remnants of the shell amoeba arenaria var. compressa. a cosmopolitan species that lives in moss pillows or moist forest floor; and the egg shells of the roundworm whipworm Trichuris trichiura, which is a parasite of the large intestine only in humans.

Interpretation of the data obtained from the palynological records of the 2008 and 2009 sections makes it possible to reconstruct the existence of steppes and dry climate during the accumulation of Holocene sediments (layers 1-3), as well as Pleistocene sediments - the lower half of layer 6a, layers 6b and 6b/1.

In Western Siberia, the Ermakov stadial deposits were formed in tundra and forest-tundra landscapes, which only at the end of the epoch were replaced by northern taiga ones. The climate changed from Arctic at the beginning of the glaciation to moderately cold boreal during the period of relative warming, and again to cold at the end of the stadial (Volkova, 1969; Volkova and Kulkova, 1984). According to palynological data, in the taiga part of the Northwestern Altai, at the final stage of the Ermakov time, two phases of the development of the natural environment are observed [Prirodnaya Sreda..., 2003]. The first one, with a relatively humid and cold climate, is characterized by a high content of spruce and scots pine pollen, with a sharp decrease in the concentration of birch pollen and the complete absence of pollen grains of broad-leaved plants in the palynological spectra. During the second phase, the spruce taiga massifs noticeably shrank, reflecting a change in climate to a drier one. The distribution of steppe tundra and forest-tundra vegetation of the MIS4 stage is also recorded in palynological records obtained during deep-water drilling on the lake. Baikal. In the Selenga River basin, there were haze and mixed grass and grass steppes. The sharply continental climate was cold and arid (Bezrukova et al., 2003).

The results of the spore-pollen analysis of the sixth layer of the Chagyr Cave, which contains Paleolithic artifacts, generally agree well with other natural science methods obtained during the study of these deposits. According to palynological data, as well as data on the species composition of the fauna of large mammals (Vasiliev, 2009), the sixth layer was probably formed in a relatively dry climate and dominated by steppe landscapes. This does not contradict the general scheme of development of the natural environment in the final of the Ermakov stadium in the south of Western and Eastern Siberia.

The increasing role of forest formations or forest steppes in the middle reaches of the Charysh River, which implies an increase in climate humidity, is reconstructed during the accumulation of the fifth layer and the upper half of layer 6a. Natural conditions during the formation of the seventh layer are also characterized by the development of forest vegetation.

Conclusion

Based on geological, palynological, and paleontological data, as well as direct dating results, it can be assumed that the sediments comprising the Sibiryachikha culture technocomplex of the Chagyr Cave accumulated during the period corresponding to the end of the fourth stage of the marine isotope scale, and belong to the end of the Ermakov glaciation. At that time, in the conditions of a dry, cold climate, steppe landscapes were widespread in the vicinity of the Chagyr Cave.

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The article was submitted to the Editorial Board on 13.06.12.

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