In the course of complex studies of deposits uncovered by the section in the estuary part of the Lobanovaya Gap near the burial ground of the VI-II centuries BC, the horizons of the burial ground of the VI-II centuries BC, as well as the cultural layers of settlements of the Late Bronze (?), Antiquity and the Middle Ages were determined. The research revealed general patterns of paleolandscape evolution in the coastal part of the Abrau Peninsula. The composition of plant communities, sea level changes, and seismic and sedimentation processes are correlated.

Key words: paleolandscape, domestic and funerary archaeological sites, stratigraphy, complex research, palynology, soil science, kerkets, torets.

Introduction

In the last decade, complex studies of a number of archaeological sites have been carried out on the Abrau Peninsula in the Krasnodar Territory in the valleys of the Tsemes, Maskaga, and Myshako Rivers, as well as in the coastal zone of the southern slope of the Navagir Ridge, cut through by a number of deep erosion-tectonic gorges (Lobanova Schel tract) [Abrau antiqua..., 2009]. Lobanov's Gap Valley* is a rather deep gorge on the southern slope of the Navagir ridge, which stretches from Anapa to Abrau-Durso. A stream hidden by sediments flows through the valley 1 km from the mouth, which flows into the Black Sea 1.3 km east of Cape Mal. Utrish. On the left slope of the valley, in the estuary part, there is a multi-layered archaeological site Lobanova Gap** (Fig. 1). Data on dates are not available for all archaeological deposits, so it is not possible to get an idea of all the stages of existence of the Lobanova Gap.

In 1998, O. E. Vyazkova carried out a reconstruction of the geomorphological situation in this area in the ancient era [1999]. In her opinion, uchas-

* Named after the Lobanov-Rostovsky estate located here before 1917.

** It was studied from 1984 to 2010 and contains deposits with an area of 230 ^m2 (Dmitriev and Malyshev, 1999; Kolpakova, Shishlov, and Fedorenko, 2011).

Fig. 1. Location of the Lobanova Schel monument on the Abrau Peninsula.

the current on which the multi-layered monument is located has a complex structure, due to the long-term formation of the valley and its development by humans. The formation of the landscape in the region under consideration was influenced by the following factors: sea level fluctuations, which significantly changed the coastline and land area; watercourses that cut through the valleys of mountain gorges and turned into powerful streams in rainy times; rather significant seismic activity, which accelerated landslide processes; intensive surf activity, on the one hand, and the presence of heavy waves. a kind of "buffer" consisting of a pile of large landslide bodies that protected the foot of the ridge from the wave action of the sea-on the other hand (Fig. 2). In 2007, at the necropolis excavation site, sediments that formed the southern slope of the Lobanov Gap beam were studied. 3). Paleolandscape studies conducted here earlier mainly covered the remote areas of the Abrau Peninsula (Spiridonova, Aleshinskaya, and Kochanova, 2009). Completed in 2007. The reconstruction of the natural environment features related to the sea coast, so it took into account, in particular, fluctuations in sea level during the studied time periods, changes in precipitation patterns, and the temporary development of paleo-soil processes.

Description of the stratigraphy of the section deep from the day surface

0-20 cm-modern turf, dark gray, loose with an abundance of roots and the inclusion of a significant amount of coarse rubble from the surface. The lower border is diffuse, noticeable by a decrease in the intensity of gray coloration.

20-40 cm-brownish-gray transition organo-mineral horizon. Compared to the previous horizon, it is denser, contains fewer inclusions of crushed stone, and is finer. The lower bound is diffuse and conditional. The main criterion for selecting the next horizon is an increase in the intensity of whitish-brown color.

Figure 2. Geomorphological map-diagram of the area where ancient monuments are located in the vicinity of the Lobanova Gap (scale 1: 50000) (according to [Vyazkova, 1999, Figure 1]), a-modern; b - the period before the catastrophe (approximately X century); c-the beginning of our era. 1 - deluvial formations of Quaternary slopes; 2-deluvial deposits of slope bases; 3-alluvial and proluvial deposits of river valleys and ravines; 4-circuses and planes of seismic fractures of peaks and slopes (mainly stratified or close to them); 5 - torn and displaced bedrock massifs; 6-isobaths; 7-archaeological sites monuments; 8-modern shoreline on paleoreconstruction diagrams.

3. Profile of the side of the excavation site at the Lobanov Gap monument.

40-70 cm-homogeneous mineral horizon of light brown color with a grayish tinge, dense. with a large amount of fine rubble, which gives the horizon increased strength. The lower boundary is smooth, sharp, and well fixed by the size of crushed stone and its concentration.

70-110 cm - a dense layer of coarse rubble. The upper and lower borders are smooth, sharp, and clearly visible.

110-160 cm-a dense layer of uniform light gray color with an abundance of small rubble. The size of crushed stone varies, and there are interlayers with larger inclusions in the thickness, but a homogeneous fine mass prevails. The lower boundary of the layer is smooth, sharp, and clearly visible by the change in the dimension of crushed stone.

170-210 cm - a layer of coarse gravelly sediment, very dense. The color of fine earth in the filling between crushed stones is gray (ashy). According to the color of fine earth, the layer is divided into two parts - the upper (170 - 180 cm) and the lower (180 - 210 cm). In the upper part, the aggregate color is light and corresponds to the color of fine earth of the overlying stratum, in the lower part, fine earth has a more gray color. The lower border is smooth, clearly visible by the size of the rubble and color.

210-240 cm-a uniform light gray dense layer with a large amount of fine gravelly material. The lower border is flat and is determined by the size of the crushed stone.

240-270 cm-a uniform light dense layer with an abundance of very fine crushed stone. The lower border is smooth, sharp, and noticeable by the size of the rubble.

270-280 cm-gravelly dense layer of brown color. Medium-sized crushed stone. The lower border is smooth and noticeable in color.

280-290 cm - a layer of dense crushed stone of medium size. It differs from the previous layer in gray (ashy) color. The lower border is smooth, well fixed in color and gravel content.

290-330 cm - dark gray humus horizon with a small admixture of crushed stone. Crushed stone inclusions are mostly small. There are also inclusions of fine charcoal. The lower boundary is diffuse, defined by the increased graveliness.

330-350 cm-a dense layer of medium-sized crushed stone. The layer is dark gray in color.

Thus, there are four dense layers of crushed stone separated by fine-grained material in the excavation wall: at the very base of the section and at depths of 270-290, 170 - 210 and 70 - 100 cm. On modern soil, large crushed stone also lies, forming another (fifth) interlayer. The layers indicate a dynamic change in the landscape from ancient times to the present, with a sharp change in the stages of relative stability and the formation of a fine-grained cover by periods of rapid (catastrophic) accumulation of coarse rubble.

For the study, two columns of samples were selected from the top along the section of the vertical wall and from the bottom, including the culture layer. The interval of 70-110 cm has not been tested, because it is a solid stone.

Chemical analysis

According to the obtained data, water solutions along the entire profile have alkaline and strongly alkaline reactions (Table 1). Such pH values are not typical for typical soils of the region, since the washing regime prevails in a humid climate, which causes a decrease in the alkalinity of the source rock. The revealed high alkalinity is due to the regular introduction of fine-earth minerals from the initial carbonate rocks and constant alkalinization of solutions. It is characteristic that the least alkaline, practically neutral pH values are observed in areas with a high content of organic carbon and gross phosphorus, i.e. on the former source surfaces or cultural layers of the settlement. The decrease in alkalinity in these areas is associated with a relatively long stage of surface stabilization, when the CO level has stopped or significantly decreased.-

Table 1. Data of chemical analysis of samples from the Lobanovoy Slit section

* No samples were taken for this analysis in horizons where crushed stone was absolutely dominant.

The process of introducing fine earth was curtailed, and natural processes dominated, during which carbonates of the rock were dissolved and washed out. In this case, the lowest pH values clearly correspond to the period of stability, the absence of intensive slope processes.

The content of organic carbon varies from 5.14 % on the modern surface to 0.43 % in the thickness of carbonate deposits. The distribution of organic carbon in the modern stratum is characterized by a gradual decrease with depth. This is a normal trend of organic matter distribution; it may indicate the relative duration of humus formation processes in the studied area.

Data on the total phosphorus content showed that the upper part of the profile (0 - 40 cm) has a natural origin, without intense anthropogenic pressure. All values for phosphorus are typical for natural objects. In the uppermost horizon (0 - 10 cm), there is slightly less phosphorus than in the next layer (10 - 20 cm). This is not typical for soils and is due to the presence of large rubble on the surface, which means that the original surface was covered with modern gravelly sediment. Once the surface was a layer that now lies at a depth of 10 cm. In any case, the value of 0.20-0.19 % can be considered a reference value for the surface soil horizons of the region. All other soil values should be lower, since phosphorus absolutely accumulates on the soil surface. Therefore, all values above the given value are not natural or soil-based, but are related to anthropogenic activity.

activities*. Horizons with elevated values of organic carbon are considered in the corresponding complexes.

The distribution of mineral carbon (rock carbonates) is even, without pronounced peaks. The minimum values correspond to the upper horizons (20 cm), which is natural for a territory with a flushing water regime. The absence of such low values for the thickness of the identified cultural layer is not surprising, since anthropogenic activity is always accompanied by the accumulation of mineral carbon, and carbonates washed out from above are deposited in the entire underlying layer, enriching it.

Palynological analysis

According to the composition of pollen and spores, the vegetation cover of the territory that existed during the formation of the studied sedimentary strata was restored. According to the section described above, 15 samples were selected on the monument, which were subjected to palynological studies. Almost all samples (except 4 and 5 from depths of 3.15 and 3.05 m, respectively) contained sufficient amounts of pollen and spores for statistical processing. The safety of pollen is very different. The samples contain a lot of mineralized, sometimes ragged and crumpled pollen. In addition to pollen, other organic residues were also found in the samples, and small fragments of wood, sometimes embers, are often found. Based on the results of the analysis, seven spore-pollen complexes were identified in the section, which are often separated from each other by breaks, which is clearly visible in the spore-pollen diagram (Fig. 4, Table 2).

Comprehensive studies of the obtained samples allowed us to characterize the change of cultural and natural landscapes in the region.

Settlement of the (late?)era bronze (depth 320 - 350 cm). The presence of a cultural layer is indicated by the result of chemical analysis: the block (330-340 cm) is enriched in phosphorus, but in this horizon it is significantly (2 - 2.5 times) less than in the necropolis horizon.

Spore-pollen complex I (grasses, mixed grasses / pine with minor participation of oak, linden, hornbeam) is traced according to sample 1 (depth 3.45 m).

The total composition is dominated by pollen of herbaceous plants-66 %, pollen of tree species - 19%, spores-15%.

Tree species are mainly represented by Pinus silvestris pollen (78 %), among which Pinus Haploxylon pollen is singly represented, and birch, alder, and willow pollen is in small amounts. Broadleaf pollen is low (7 %); it belongs to linden Tilia, oak Quercus and hornbeam Carpinus.

Herbaceous plants contain the most pollen from Roaceae grasses (42 %), and large pollen grains of cultivated species are also noted. There is quite a lot of pollen from the Chenopodiaceae haze family (15 %), including Artemisia wormwood (approx.8%). Pollen of Suregaseae sedges is found in small amounts. Mixed grasses make up 33 % of the total pollen and are mainly represented by pollen from the chicory families Cichoriaceae (14 %) and Asteraceae (12%). Pollen of the cruciferous Brassicaceae, buckwheat Polygonaceae, and Malvaceae families, including weed species, is found in small or isolated amounts among various grasses.

Spore plants are represented by green Bryales mosses and single ferns of the family Polypodiaceae and chistousta Osmunda.

The zonal type of vegetation cover of the studied territory at that time was mixed grass and grass steppes. It is possible that representatives of the haze and wormwood families grew selectively on the rocks. In places with the most favorable conditions, there were small areas of forest formed by pines, with an admixture of such broad-leaved species as oak, linden, hornbeam.

The age of the host sediments probably corresponds to the Late Bronze Age, when the territory was drained after the retreat of the waters of the Novochernomorskaya transgression. According to P. V. Fedorov, the Novochernomorskaya terrace was drained already in the VIII-VII centuries. B.C. [1963; Vyazkova, 1999].

The composition of the palynological spectrum is best compared with the lower sections of Section 2 (TPC - I (16)) at the Tsemdolinsky settlement, which has a date of 3960 ± 100 BP (Spiridonova, Aleshinskaya, and Kochanova, 2009) (Table 3).

Spore-pollen complex II (mixed grasses, grasses / minor involvement of pine, birch, oak, linden) was described from samples 2 and 3 from depths of 3.35 and 3.25 m, respectively. It is separated from the previous and subsequent complexes by a temporary break, which indicates the discontinuity of sedimentation processes in the Bronze Age.

The content of tree pollen in the total composition is slightly reduced (11-13%), compared to the previous complex, grasses become even more (74-77 %), spores account for 10-15 %.

The group of tree species still contains the most pollen from Pinus silvestris, although its content is reduced to 50-60 %. The pollen content of Betula birch (20 - 30 %) and Shiro is greatly increased.-

* It should be noted that any movement of fine earth containing phosphorus causes a decrease in the quantitative values of phosphorus due to the loss of some phosphorus compounds during the transfer of the material.

4. Spore-pollen diagram of deposits of the Lobanova Schel monument.

Table 2. Results of spore-pollen analysis of samples from the Lobanova Gap section

Table 3. Correlation of sections at archaeological sites of the Abrau peninsula according to palynological analysis

Note: Roman numerals indicate spore-pollen complexes.

Deciduous species (10-23%). Broadleaf species are represented by Tilia linden (5-14%) and Quercus oak (5 - 9%).

Among herbaceous plants, the pollen content of Roaceae cereals decreases to 22-25 %, and the role of pollen of the chicory families Cichoriaceae (24-27 %) and Asteraceae (13-19%) increases. Haze Chenopodiaceae (19%) and Artemisia wormwood (9-10%) are becoming more common. Ephedra pollen appears in small amounts (2-4%). The pollen of the buckwheat family Polygonaceae was singly recorded. Malvaceae and Cyperaceae sedges.

In the spore group, as in the previous complex, green Bryales mosses predominate, but their share becomes smaller and amounts to 65-75 %. The role of Polypodiaceae ferns is increasing (25-31%). Spores of chistoost Osmunda have been isolated.

In comparison with the previous stage, the nature of vegetation cover has changed little. It is possible that at this time, under the domination of the steppes, more diverse tree species penetrated the boundaries of the Novochernomorskaya Terrace, but their role in the landscape of the territory was small. In the composition of the spore-pollen spectrum, the specific weight of plants of rocky soils, especially the haze and wormwood families, increases. Probably, in the most shaded areas, the role of ferns increased, among which chistoust is represented.

The time of formation of this complex is close to the stage described above. Late Bronze Age bo-

5. General plan of the studied structures (a) and reconstruction of the external appearance of the structures (b) of the aboriginal (Kerketo-Toret) burial ground.

The spore-pollen complex IV (16) of section 2 at the Tsemdolinsky settlement, dated 3130 ± 100 BP (Spiridonova, Aleshinskaya, and Kochanova, 2009), corresponds most strongly (see Table 2).

Horizon of the aboriginal necropolis (depth 280 - 320 cm). The level of 290 - 320 cm corresponds to an increased value of organic carbon. This indicates the presence of a surface horizon here, in which soil formation processes took place, organic matter accumulated. The cultural layer in the range 280-320 cm is determined by an abnormally high phosphorus content - up to 1.43 %. This indicator indicates the presence of a well-developed cultural layer here in the past. Moreover, the level of development of the site during the formation of this complex was higher than during the formation of the next, later cultural layer (260-270 cm).

The date of this horizon is determined by the structures of the burial ground of the indigenous (Kerketo-Toret) population (Fig. 5), as well as by fragments of imported antique ceramics, among which the products of the late VI-early III centuries BC are more widely represented than vessels of the W-N centuries BC (Fig. 6). These materials They are evidence of intensive contacts of the local population of the time under consideration with the ancient world (compare with the Vladimirovsky, Tsemdolinsky burial grounds or Sheskharis located on the shore of the Tsemess Bay and in the Tsemess Valley) and may indicate the presence of Emporium nearby, which was destroyed along with a significant land area as a result of intense coastal abrasion.

Spore-pollen complex III (single pollen grains of cereals, mixed grasses, and pine) was described from samples 4 and 5 from depths of 3.15 and 3.05 m, respectively. It is separated from the previous and subsequent assemblages by a break: the sediments characterized by these samples did not contain the necessary amount of pollen and spores for statistical processing.

Horizon of an Early Roman settlement (depth 250-290 cm). Its presence is indicated by the cultural layer (260-270 cm), which contains more phosphorus than is typical for soils, but not much. This cultural layer was most likely partially redeposited. This conclusion is also supported by the abundance of large rubble at the specified depth.

Burials of the period after the II century BC were not found on the necropolis, so we associate fragments of amphorae from this time with the cultural layer of a Roman settlement located near the necropolis, higher up the slope (?).

Spore-pollen complex IV (mixed grasses, grasses / pine with oak, linden) was described from samples 6, 7, 8, and 9 from depths of 2.95, 2.85, 2.75, and 2.65 m, respectively.

6. Amphora ceramics from the cultural layers of the Lobanova Schel monument. a-end of VI-V century BC; b-IV-beginning of III century BC; c-III-II centuries BC; d-I century AD; d-IX-XI centuries AD.

The total composition is dominated by pollen of herbaceous plants (65-80%), pollen of tree species is from 8 to 24%, spores - 11-18 %.

Among tree species, Pinus silvestris pollen is the highest (39-60%). There is a high pollen content of broadleaf species (24-33 %), represented by Tilia linden (6-17 %) and Quercus oak (16-23 %). The pollen content of Betula birch reaches from 11 to 31 %. Isolated pollen from Picea spruce and Caprifoliaceae honeysuckle is present.

Among herbaceous plants, almost half is pollen of mixed grasses (32-57%), which is becoming more diverse compared to previous complexes. Pollen of the chicory families Cichoriaceae (13-31 %) and Asteraceae (up to 17%) continues to play a dominant role in the composition of mixed grasses. Pollen from the legume Fabaceae (2-13 %), umbrella Apiaceae (up to 7 %), buckwheat Polygonaceae, Rosaceae, cruciferous Brassicaceae, and Malvaceae families was also recorded. The content of Roaceae cereals is from 12 to 25 %. There is a lot of pollen from the haze family Chenopodiaceae (17-31 %), Artemisia wormwood (up to 15 %), especially in sample 6. Ephedra pollen has been found in small quantities, and Suregaseae sedges have been isolated.

Spore plants are mainly represented by green Bryales mosses (80-100%) and partially by Polypodiaceae family ferns (4-20%).

During the formation of this complex, there was a gradual moistening of the climate, which was manifested in an increase in the role of spore plants in the overall composition and in an increase in the share of broad-leaved species in the composition of even small forest areas located in the steppe. There was a slight increase in the participation of herbaceous and shrubby plants from the haze family, which still grew near rocks or in cracks between them. It is possible that some species from the family marevae, as well as ephedra, settled on the sands along the beach and above, within the ancient Black Sea terrace formed during the Phanagoria regression. According to O. E. Vyazkova, who refers to P. V. Fedorov (1963), the beginning of drainage of the terrace occurred in the VIII-VII centuries BC and lasted until the beginning of the I millennium AD.According to the palynological data of the studied complex, the beginning of the rise of the ground water level probably belongs to the ancient Roman time. Starting from the time that Sample 7 corresponds to, this contributed to the development of more moisture-loving natural vegetation. It is possible that the ground water level was rising due to the beginning of a small rise in the Black Sea level against the background of the Phanagoria regression. According to the results of chemical analyses, the ancient Roman period accounts for the formation of soil buried above the structures of the aboriginal (Kerketo-Toret) burial ground. At the same time, the same-age strata belong to a number of other studied sites: the settlements of Myshako, Dubki (section 1), Raevskoe gorodishche (section 2), and Raevsky Kurgan (Spiridonova, Aleshinskaya, and Kochanova, 2009) (see Table 2).

Horizon of a Roman settlement (depth 250 - 200 cm). The soil interval 180-210 is characterized by increased values of organic carbon, which corresponds to the data of surface soil samples. According to the phosphorus content, a thickness of 180 - 230 cm is distinguished; it shows a gradual increase in the amount of phosphorus to a depth of 200 - 210 cm, followed by a decrease in values to a depth of 230 cm. Since the upper part of the stratum contains a large amount of crushed stone, it can be assumed that it is a cultural layer displaced during the disaster, and the lower part is a cultural layer formed in situ, and changes in the quantitative parameters for phosphorus reflect an increase in the intensity of economic activity in this area. The underlying horizon of 240-250 cm contains 0.20% phosphorus: apparently, the surface of the soil on which the settlement was created was recorded.

Spore-pollen complex V (mixed grasses, grasses / with pine, oak, birch, and alder) was described from samples 10 and 11 from depths of 2.55 and 2.05 m, respectively. The complex began to form, possibly after a very short break.

In the total composition, there is a significant increase in the share of tree species (30-40 %), the share of herbaceous plants is reduced to 35 - 55 %, and spores account for from 15 to 25 %.

Tree species are represented primarily by pollen from Pinus pine (48-75%), with isolated pollen from Picea spruce and alder Alnus (4 - 5%). The pollen content of Betula birch becomes less (4-14%), especially closer to the upper part of the complex, the pollen content of broad-leaved species decreases (up to 15 %), which are represented by Quercus oak (5-18%) and Tilia linden (10-14%).

In the group of herbaceous plants, the amount of pollen from Roaceae grasses increases (33 %), and the value of the Chenopodiaceae family decreases (12-24%). A lot of Artemisia pollen (16 %). The role of mixed grasses decreases (up to 27-36%), which is represented by pollen of the families of chicory Cichoriaceae (10-15%), aster Asteraceae (9-10%), buckwheat Polygonaceae, cruciferous Brassicaceae, umbrella Apiaceae, legumes Fabaceae, Malvaceae Malvaceae. Pollen of Plantago psyllium (4 %), a weed that is often associated with human activity, was detected.

Spores are becoming more diverse. Against the background of the predominance of spores of green Bryales mosses (58-65%), the content of Polypodiaceae family ferns increases (34-35%), and spores of Lycopodium clavatum (4 %) and Sphagnum mosses (4%) appear.

The zonal vegetation type at this stage was mixed grass and grass steppes with a high participation of broadleaf and pine forest islands.

Sometimes the forest groups included a very small number of birch trees. The composition of spore plants is diverse, which may be an additional evidence of increased moisture in woodlands. Apparently, the humidification of the climate during this period increased in comparison with the previous stage.

Taking into account the results of the analysis of data obtained from the studied section, as well as the geological structure at the site of the ancient burial site, it can be assumed that after the formation of the studied sequence (complex V) along the Black Sea coast, cataclysms occurred, possibly associated with the Nymphean transgression. The abrasion affected part of the coastal ledge composed of deluvial deposits and the underwater part of the slope, which led to deformation of the natural equilibrium profile [Vyazkova, 1999, pp. 54-55]. In all likelihood, it was at this time that the coastal group of monuments was destroyed, including the burial ground in the Lobanova Gap.

Spore-pollen complex VI (mixed grasses with the participation of grasses / insignificant participation of pine, oak, linden, hornbeam) was described from sample 12 from a depth of 1.95 m. It is separated from the previous and subsequent complexes by a temporary break.

In the total composition, the pollen content of tree species is low - only 11 %, most of all pollen of herbaceous plants - 72 %, the share of spores is 17 %.

The group of tree species is dominated by Pinus pollen (81 %). Pollen of broad-leaved species (19%) was found, which are quite diverse and are represented by pollen of oak Quercus, linden Tilia, beech Fagus and hornbeam Carpinus.

Of the grasses, the most pollen is from the Roaceae grasses (46 %), among which there are cultural forms. Mixed grasses account for 25 %, of which 16% are pollen of the chicory families Cichoriaceae and 6 % are Asteraceae. Pollen of the cruciferous families Brassicaceae, legumes Fabaceae, and basil Thalictrum was singly recorded in the composition of various grasses. Pollen of the haze family Chenopodiaceae is 16 %, Artemisia-12 %. Ephedra pollen has been isolated. The pollen of plantain Plantago was determined from weeds.

Spore plants are represented by an approximately equal number of spores of green Bryales mosses (48 %) and Polypodiaceae ferns (46%). Spores of Sphagnum mosses were found in small quantities (5 %).

After a significant break, which is recorded in the section, the nature of the vegetation cover of the territory has changed significantly. There was a complete degradation of forest vegetation. In the palynological spectrum of complex VI, the role of tree pollen is very small; it is possible that its presence is associated with wind drift of individual pollen grains, especially such as

rocks like hornbeam and beech. Open steppe landscapes dominated. Grasses predominated in the composition of herbaceous vegetation. In less favorable conditions, for example, on gravelly slopes, representatives of the haze and wormwood families grew. In general, the environmental conditions were arid in nature. Taking into account the presence in the spore-pollen spectrum of grains of cultivated cereals, as well as weeds, it can be assumed that the decrease in the proportion of forests with the growth of open landscapes was determined not by natural and climatic, but by anthropogenic factors. In other words, the Roman period of development of the territory was accompanied by massive deforestation for pastures and fields.

According to data on changes in the levels of the Black and Azov Seas (Danovsky and Dikarev, 2007, p. 100-102), the Korsun regression is distinguished in the first millennium AD, during which the sea level decreased by 1.5 - 2.0 m. This regressive stage was also noted by S. I. Varushchenko [1975] and P. V. Fedorov [1982], but it was assumed that the sea level dropped by about 1 m.

Medieval period (depth 180 - 130 cm). According to chemical analysis, the phosphorus content in the section at a depth of 140-150 cm is 0.34 %, which indicates its artificial genesis - this is a cultural layer. In the range of 140-150 cm, the organic content is not more than 1 %, although the pH is highly alkaline. This suggests that the soil corresponding to this interval was at the surface for some time, had a vegetation cover, but was soon covered by a highly alkaline gravelly sediment.

6, d) and grain accumulations suggest that the cultural layer of the Middle Ages, dated from the eighth to the beginning of the eleventh century, was located directly above the necropolis.

Sporoeo-pylcea complex VII (mixed grasses, grasses / minor involvement of pine, oak, and linden) was described from samples 13, 14, and 15 from depths of 180, 170, and 130 cm, respectively.

The total composition is absolutely dominated by herbaceous plants (up to 92 %), there is little tree pollen, its content ranges from 6 to 16%, and very few spores - 2 to 3 %.

In the group of tree species, despite their small role, a high content of broad - leaved pollen (25-50%) was generally noted, represented by pollen from oak Quercus (10-23%), linden Tilia (8-15%), beech Fagus (8-10%) and occasionally hornbeam Carpinus. The pollen content of Pinus pine is less than in the previous complex, and amounts to 15-27 %. The proportion of pollen from Picea spruce (10 %) and alder Alnus (8 - 31%) increases. The pollen content of Betula birch ranges from 5 to 22 %. The pollen of willow Salix and juniper Juniperus was singly recorded.

Among herbaceous plants, the pollen of grasses and mixed grasses is represented in comparable amounts: Roaceae grasses from 34 to 45 %, mixed grasses from 31 to 48 %. Among cereals, there are cultural forms. The composition of mixed grasses mainly includes pollen of the chicory families Cichoriaceae (22-35%), Asteraceae (3-11%). Pollen of the families of buckwheat Polygonaceae, Rosaceae Rosaceae, cruciferous Brassicaceae, umbrella Apiaceae, and basil Thalictrum is found singly and in small quantities. Ephedra pollen was found in a small amount in all samples characterizing complex VII. Pollen of representatives of the Chenopodiaceae haze family is 10-15 %, Artemisia wormwood-6-9 %.

Spore species are mainly represented by Polypodiaceae ferns (50-60%), Bryales green mosses (25-29%), and Sphagnum Sphagnum mosses (15-25%).

At this stage of vegetation development, the climate within the Lobanova Schel tract has again become slightly wetter and warmer. However, the landscape was still dominated by meadow steppes. In the most favorable humid conditions, the forest vegetation formed very small islands. According to palynological analysis, in addition to pine, such broad-leaved species as oak, linden, and beech are constantly present in the spectra.

Conclusion

A unique feature of the studied section is the stable position of the entire thickness of sediments of different ages, which is largely due to its geological structure - the position at the base of the "buffer" of Paleogene rocks, which prevented the erosion of the Holocene strata during strong storms. The study of sediments uncovered by the section in the estuary part of the Loban Gap near the burial ground of the VI-II centuries BC revealed the general trend of paleolandscape changes that occurred in the coastal part of the Abrau Peninsula. At the same time, it was possible to establish correlations between the composition of plant communities, changes in sea level, and seismic and sedimentation processes.

The history of sediments on the southern slope of the Lobanov Gap gully can be characterized as an alternation of periods of stability and dynamic transformations. The first ones are associated with the processes of soil formation and development of the site by people, when the formation of cultural layers took place.

When stability was replaced by the stage of dynamic movement of huge masses of crushed stone, cultural layers and soils overlapped with it, creating new surfaces. The entire studied stratum is a series of such bundles of "stable" and "dynamic" layers.

High values of the total phosphorus content in the entire studied thickness, except for the modern layers, indicate active development of the territory by humans. Due to comprehensive research, in addition to the burial ground horizon of the VI-II centuries BC, the cultural layers of the settlement of the Late Bronze Age (?), Antiquity and the Middle Ages were identified here.

The degree of anthropogenic impact in the region under consideration in the past was higher than at present, which suggests a correlation between the intensity of slope flows and the degree of anthropogenic pressure on the landscape. Since the cultural layers of the settlements are overlaid with large rubble, it is obvious that life activity on the site has always been interrupted by a catastrophe. Dynamic natural processes had a different genesis: the movement of huge masses of crushed stone occurred as a result not only of seismic activity and erosion-tectonic processes, but also of a catastrophic amount of precipitation, which caused the formation of mud-stone flows. This mechanism of formation fits well with the geological structure of the section, the chemistry of soil composition, and palynological analysis data.

Based on the materials of the Lobanova Schel monument, it was possible for the first time to study changes in the region's landscapes not only during stable periods of regressions of the Black Sea, during the formation of soil horizons and cultural layers, but also in the first half of the Nymphean transgression phase (Complex V) associated with the Roman time (I-III centuries AD). The considered palynological spectra record the greatest afforestation of the coastal part of the Black Sea. Communities of broad-leaved pine forests predominated, and grass-mixed meadow groups were common in open spaces. Such a significant afforestation of territories in other parts of the peninsula has not yet been revealed based on the materials of the settlements of Myshako and Dubki, as well as the Raevsky settlement (Spiridonova, Aleshinskaya, Kochanova, 2009). However, these materials are used to trace the events of different stages of the Phanagoria regression. Thus, during this period, in all parts of the Abrau Peninsula, afforestation was minimal, and within the Tsemdolin settlement and beyond it, there was no forest, and dry steppes dominated. In the materials of the Raevsky hillfort (section 1), it was possible to identify the horizon of sown areas, in which large accumulations of pollen from cultivated cereals and a high content of pollen from various weeds were recorded [Ibid.]. This period of agriculture falls at the beginning of the Phanagorean regression - the Early Roman period.

The presence of arable horizons in the settlement of Dubki and the Raevsky hillfort and pollen of cultivated cereals in the soils of ancient times correlates well with a decrease in the forest cover of the territory. The heterogeneity of the spore-pollen spectrum in open spaces in different zones of the peninsula at the same time allows us to draw an important paleoecological conclusion about the intensive anthropogenic transformation of landscapes in the period of antiquity.

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The article was submitted to the Editorial Board on 19.06.14.

* On the Lobanov Schel monument, this stage is presented in fragments.

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