The burials of the early Medieval period (IV-VI centuries A.D.) and the background soil of the Ust-Utyak-1 ancient settlement located in the forest-steppe zone of the Middle Pritobol region were studied. It is established that their differences do not exceed the rank of soil type. For the last 1 300 - 1 500 For many years, the development trend of forest-steppe chernozems was directed towards aridity, as a result of which leached chernozems evolved into typical ones. A comparative analysis of the morphological structure and chemical properties of the studied soils suggests that in the IV-VI centuries AD, natural conditions were characterized by greater moisture and heat supply compared to the present time. Judging by historical and archaeological data, this period coincides with the flourishing of the Bakal culture, which fell into decline with its end.

Key words: buried soil, dynamics and evolution of natural conditions, ethno-cultural interactions, Baikal culture, Middle Pritobolye.

Introduction

The study of the state of the environment of past epochs was one of the priority tasks of natural sciences throughout their historical development. Researchers have discovered various natural formations that can preserve paleoinformation. These items include buried soils under archaeological sites (fortifications, burial mounds, cultural layers). It is known that they are able to preserve traces of changes in natural conditions in the form of properties and features of the soil profile [Aleksandrovsky, 1996; Akhtyrtsev B. P., Akhtyrtsev A. B., 1994; Borisov, Demkina, Demkin, 2006; Velichko, Morozova, 1985; Gennadiev, 1990; Demkin and Ivanov, 1985; Ivanov, 1984; Ryskov and Demkin, 1997; Khokhlova, Oleynik, and Kovalevskaya, 2000]. Being buried under an archaeological mound-

* This work was supported by grants from the President of the Russian Federation (MK-54.2008.5 and NS-5582.2012.5), as part of the Program of fundamental research of the Presidium of the Russian Academy of Sciences (R-16.9).

As a result, the soil is largely excluded from the further soil formation process, remaining for a long time in the state at the time of its "conservation". At the same time, soils are capable of preserving objects of non-food origin that can be used as a basis for reconstructing the ancient natural environment (plant spores and pollen [Pollen analysis, 1950], phytoliths [Goleva, 1997], mineral neoplasms [Maher, Alekseev, Alekseeva, 2003], faunal remains [Markova, 2000]). Chronologically, most of the preserved buried soils of the archaeological sites of Northern Eurasia cover the period of 5 thousand years, when the ancient population developed the burial mound rite and the first urban planning traditions [Brashinsky, 1979; Rayevsky, 1985]. In recent years, interest in the study of these soils has led to the creation of a new interdisciplinary scientific direction - archaeological soil science, the methodological foundations of which are described in a number of scientific publications [Aleksandrovsky, 1983; Dergacheva, 1997; Demkin, 1997; Ivanov, 1992; Holliday, 1989; Vreeken, 1975]. It has an extensive methodological apparatus that includes methods not only in soil science, but also in physics, chemistry, biology, mineralogy and other sciences. An integrated approach to the study of paleosols of archaeological sites has provided new data on the structure, functioning, genesis, dynamics, and evolution of soils and soil cover in various regions of the world, covering the second half of the Holocene. They allow us to reconstruct the natural conditions of past epochs, as well as to study the interactions between nature and ancient societies. Geographically, there is a heterogeneity in the degree of study of regions that are promising for archaeological soil science. Along with well-studied areas (the center of the Russian Plain [Aleksandrovsky, 1983; Akhtyrtsev B. P., Akhtyrtsev A. B., 1994], the Lower Volga region [Borisov, Demkina, Demkin, 2006; Demkin, Ivanov, 1985; Ivanov, 1984, 1992; Demkin et al., 2004, 2006], the Southern Urals [Ryskov and Demkin, 1997; Khokhlova, Oleynik, and Kovalevskaya, 2000]) are poorly studied. One of these regions is the Srednyye Pritobolye, where paleosoil studies have been conducted relatively recently and cover individual monuments and archaeological microdistricts [Valdayskikh, 2007; Mahonina and Valdayskikh, 2008; Yakimov et al., 2007]. The available information about the state of soils and the natural environment in different historical epochs is not the same. One of the elabooveshennyh periods is the early Middle Ages, known for its complex cultural and historical events (Botalov, 2009). This paper presents the results of a comparative study of early medieval (IV-VI centuries AD) buried and modern soils of the Middle Partobol region and their paleogeographic interpretation on the example of the Ust-Utyak-1 settlement.

District, objects and research methods

The study area is located in the southwestern part of the West Siberian accumulative Plain and is located within the forest-steppe natural zone (Fig. 1). The climate of the region is continental, the average annual air temperature is 1.3 °C, and precipitation is 330 mm. Coefficient of humidification, according to N. N. Ivanov, 0,6 [Agroclimatic resources..., 1977].

The objects of research were buried soil of the IV-VI centuries AD under the fortification rampart of the Ust-Utyak-1 settlement and exposed soil. Both are confined to the high terrace of the Tobol River, which has an absolute height of 160 m and a slope of 50° [Yegorov and Krivonos, 1995]. Ust-Utyak-1 ancient settlement is located on the territory of the Ketovsky district of the Kurgan region, 22 km south of Kurgan (coordinates: 55°16 'N and 65°19' E). The monument is located compactly and has a relative height above the water level of the Utyak River (right tributary of the Tobol). 2, 3). Its total area is 1,840 ^m2. According to archaeological data, the ancient settlement has a two-layered structure: the lower layer dates back to the X-VIII centuries BC (the transition period from the Bronze Age to the Iron Age), and the upper layer dates back to the IV - VI centuries AD (the Early Middle Ages) [Kaidalov and Sechko, 2008]. The fortification system, the construction of which dates back to the early medieval period of the settlement's existence (IV-VI centuries AD), is represented by a rampart up to 1.5 m high with four small projections on the outside. The ends of the rampart abruptly merge into the steep slopes of the terrace. Internal space

Figure 1. The study area.

2. General view of the Ust-Utyak-1 settlement.

3. Diagram of the Ust-Utyak settlement-1. P1 - section of buried soil; P2 - section of modern soil.

the monument is 1,200 ^m2 long. The moat, the entrance to the ancient settlement, and housing depressions are not visually recorded (Kaidalov, Shilov, and Maslyuzhenko, 2003).

The main research method was soil-archaeological (Demkin, 1997; Dergacheva, 1997). The main chemical parameters (organic matter content, easily soluble salts, anionic-cationic composition, pH value) were determined in samples taken from genetic horizons. The analyses were performed in an accredited environmental research laboratory of the Chemical Faculty of Tyumen State University.

The age of the fortification rampart was determined by radiocarbon dating (¹⁴ C each) of charcoal from the defensive structure (Epimakhov, 2008), as well as organic material from the upper part of the humus horizon of the buried soil. The analyses were performed in the Laboratory of Cenozoic Geology, Paleoclimatology and Mineralogical Climate Indicators of the Institute of Geology and Mineralogy of the Siberian Branch of the Russian Academy of Sciences (SOAN index) and the radiocarbon laboratory of the Institute of Geography of the Russian Academy of Sciences (EGAN index) (Table 1). Five dates for coal were obtained, two of which stand out sharply: obviously aged (SOAN-7054) and rejuvenated (SOAN-7057). The rest are relatively evenly distributed in the interval from the second to the fifth centuries inclusive. Date based on organic material from the upper part of the buried humus horizon

Table 1.

Radiocarbon dates of material from the fortification rampart of the Ust-Utyak-1 settlement

It belongs to the VII-VIII centuries. Thus, the results obtained allow us to reliably date the ancient settlement to the IV-VI centuries AD.

Morphological structure and chemical properties of buried and modern soils

Buried soil. During the field seasons of 2007 and 2008, comprehensive studies of the fortification rampart of the Ust-Utyak-1 settlement were conducted. A transverse trench was used to open its embankment with the soil buried under it (Fig. 4), which we defined as leached chernozem (Klassifikatsiya..., 1977). A soil section laid in the central part of the western edge of the trench (see Fig. 3), identified five stratigraphic levels (Table 2): 1) modern soil (0-50 cm; hereafter depth from the modern surface); 2) the first cultural layer with the remains of a defensive structure (54-80 cm); 3) the second cultural layer (90-128 cm); 4) the third cultural layer (155-200 cm); 5) buried soil (200-265 cm).

The greatest interest is the preserved buried soil. In its structure, two horizons are distinguished: humus [A1] and illuvial-sodium [Bna]. The first one (200 - 227 cm) is a light gray very dense sandy loam with a lumpy structure with inclusions of mineral quartz grains and vertical cracks. The second one (227-265 cm) has a heterogeneous structure and is subdivided into three subhorizons: [B1na] (227-244 cm) - dark brown structureless sand with inclusions of mineral grains of different dimensions, complicated by vertical cracks and wormholes, very dense; [B2na] (244-255 cm) - light gray sandy loam of plate structure, very dense, vertical cracks are noted; [B3na] (255 - 265 cm) - light yellow loose structureless sand. The soil-forming rock [C] (265-270 cm) is composed of whitish structureless sand. Below lies an iron-rich sandy-gravelly mass [D] (270-280 cm), heterogeneous in color (alternating yellowish-red and bluish-gray fragments), heavy loamy granulometric composition, blocky structure, with carbonates in the form of deposits and "cranes" reacting with 10% hydrochloric acid (HCl). In the [Bna] and [C] horizons, there are rare new formations of carbonates - deposits that react weakly with 10% hydrochloric acid.

In the buried soil, the organic matter content decreases with a depth from 1.4 to less than 0.5 % (tab. 3), while a slight increase is noted in the mountain [B2na]. We reconstructed the initial humus content in the organogenic horizon according to the method proposed by S. V. Gubin [1984]. Its diagenetic losses are considered to be

4. Stratigraphy of the fortification rampart and buried soil.

A _der - sod horizon; A1 - humus; P - puncture; US1, 2-carbonaceous layers; KS1, 2, 3-cultural layers; B - waste;

B1na, B2na, and B3na are subhorizons of the illuvial-sodium horizon; C is a soil-forming rock; D is an ironed sandy-gravelly mass. The square brackets represent the buried soil horizons.

Table 2.

Morphological structure of buried and modern soils of the Ust-Utyak-1 archaeological site

* Custom obozn. see Fig. 4, 5.

in the mountains. A1 of medieval soils is at least 50 %. Taking into account the light grain size distribution of the buried soil, we assumed a loss of organic matter at the level of 70 %. The reconstructed humus content was approx. 2,4 %. The main anions (Cl ^-, SO4 ₂ ^-, HCO3 ² -^{) and cations (Ca2+}, ^Mg2+) are evenly distributed over the profile, and their concentrations are low. At the same time, there is an increased sodium content. The [Bna] horizon is characterized by a high concentration of Na2^{+ cations, varying from 1.5 to 4.1 mmol/100 g of} soil. The reaction of water extraction is constant along the profile, the pH value is 6.9-7.3.

Modern soil. A section of the background soil was laid 10 m to the north-east of the fortification rampart (see Figure 3). It is established that modern soils in the vicinity of the monument belong to typical chernozem (Fig. 5). The sod horizon (A _der) with a thickness of 7 cm is composed of dark gray sandy loam of fine-grained structure (see Table 2). It has an increased concentration of roots of woody, herbaceous vegetation and poorly decomposed organic material. A _der smoothly passes into the humus horizon (A1), which lies at a depth of 7 to 35 cm. It is a dark gray sandy loam of a tiled structure with inclusions of-

Table 3.

Chemical properties of buried and modern soils of the Ust-Utyak-1 archaeological site

It is complicated by vertical cracks along which the roots of grassy vegetation spread. The organogenic part of the profile is underlain by an illuvial-glandular horizon-Bfe (35-60 cm). It is a reddish-brown sandy loam with a prismatic structure. At a depth of 44-56 cm, a conglomerate of ferruginous sandstone was discovered, which has a plate structure with a concentric orientation around a dense core. The horizon is complicated by burrows of earthmoving animals. From a depth of 60 cm, a violent reaction of the material with 10% hydrochloric acid is observed. From this level, an illuvial-carbonate horizon (Bca) is distinguished, which has a thickness of

5. Structure of modern soil. A-turf _horizon; A1 - humus horizon; Bfe - illuvial-ferruginous; Bca - illuvial-carbonate horizon; C - soil-forming rock; D - iron-rich sandy-gravelly mass.

20 cm. It is a yellow-brown sandy loam of a lumpy-prismatic structure with new formations of carbonates in the form of powdery spots, primazki, grains,"cranes". The illuvial part of the soil profile borders on the soil-forming rock (horizon C, 80-95 cm), which is composed of whitish structureless sand. Below lies an iron-bound sandy-gravelly mass (horizon D), consisting of heavily loamy material of heterogeneous color (alternating yellowish-red and bluish-gray fragments), a blocky structure, with new formations of carbonates in the form of primazki, drips, "cranes".

The content of organic matter in the soil decreases with depth from 12.1% to less than 0.5%, while in the ironized sandy-gravelly mass it slightly increases (Table 3). In general, the soil profile is brine-free, easily soluble salts are less than 0.1%, with the exception of mountains. And _der, where they are 0.2 %. Special attention should be paid to the distribution of basic anions and cations. The content of bicarbonate ions varies with depth; the maximum (1.5 mmol/100 g of soil) is observed in the mountains. Bca, in other cases it varies from 0.10 to 0.35. The amount of chlorine ions decreases uniformly with depth from 0.2 to 0.1 mmol/100 g of soil. The content of sulfate ions decreases slightly in the mountains. A1 and remains unchanged (0.5 mmol/100 g of soil) to Mt. D, where there is a sharp increase to 6.7 mmol/100 g of soil. Calcium and magnesium cations are evenly distributed over the profile, with the exception of mountain D, where their concentration increases to 10 and 1.1 mmol/100 g of soil, respectively. The content of sodium cations slightly increases in the Bfe and Bca horizons, then in the soil-forming rock it decreases to the level in the upper part of the profile (A de and A1) (_< 1 mmol/100 g of soil) and sharply increases in the mountains. D (1.7 mmol/100 g of soil). The pH value increases with depth from 6.5 to 8.9.

See Table 4.

Radiocarbon dates of material from carbonate neoplasms of relict horizons

A comparative analysis of the morphological structure and chemical properties of buried and modern soils revealed a number of similar features and differences. The studied soils differ at the subtype level. Buried chernozem is less structured and at the same time more compacted in comparison with modern soil, and the color of horizons is characterized by a lightening of the overall tone. The granulometric composition of the studied soils is sandy-sandy loam, and the soil profiles are underlain by a heavy loamy-clayey ozhelezny sandy-gravelly mass (mountain D). In the buried soil, there are rare new formations of carbonates in the illuvial-sodium horizon (Bna), while in the background soil at a depth of 60-80 cm, a carbonate accumulation horizon (Bca) is distinguished. New formations of carbonates are represented by primazki, drips, "cranes", powdery spots. The morphology of the studied soils indicates their polygenetic nature. Thus, the underlying rock in both cases is characterized by a high degree of ironification and well-expressed redox properties. An atypical relict horizon (Bfe) has been preserved in the modern soil, which has complicated the overall structure of the profile. In addition, the Bfe and [D] horizons contain carbonate neoplasms (kutans and "cranes") located on the surface of iron-bearing formations of secondary origin. Their absolute age was determined by radiocarbon dating at Uppsala University, Sweden (Table 4).

The results obtained allow us to speak about the hydromorphic (swamp) stage of soil cover development, which preceded modern soil formation. This stage ended no later than the early Holocene, after which a stable arid trend of natural conditions in the study area was established. The content of organic matter in the profiles of the studied soils decreases with depth, but the quantitative indicators differ. Thus, in the humus horizon of buried soil, it was at least 2.4 % (reconstructed value), while in the modern one it was 2.9 %. Lower in the paleosoil profile, humus is less than 1 %, and in modern chernozem it is more than 1 %, and only in horizons C and D its concentration decreases to 0.5-0.6 %. The studied soils are saline, the content of easily soluble salts is less than 0.1 %. The distribution of anions and cations over the profile is not the same. In the buried soil, the main anions (HCO3 ^-, Cl, SO4 ^-) are evenly distributed; their concentration decreases slightly only in the lower part. In modern soil, only chlorine anions have a uniform distribution. The concentration of bicarbonate ions increases with depth, reaching max-

simuma in the mountains. Ica (1.5 mmol/100 g of soil), after which it decreases again. The content of sulfate ions decreases with depth, while in the mountains. D there is a sharp increase to 6.7 mmol / 100 g of soil. Calcium and magnesium cations are equally distributed over the profiles of the studied soils, while the concentration of sodium cations increases with depth. In the modern chernozem in the mountains. D a significant increase in the content of the main cations (Ca2^+, Mg2+^{, and Na2+}), as well as anions of the sulfate group, was observed. Buried chernozem has a lower pH value compared to modern soil.

Reconstruction of natural conditions

For the territory of the forest-steppe Trans-Urals, most researchers define the early Middle Ages from the fourth to the first half of the tenth century AD (Konnikov, 2007). To date, there are few data on the state of the environment in this region, and in particular in the Middle part of the Volga region, during this period. According to the results of palynological studies of the Tobol-Ishim interfluve (Ryabogina, 2008), moderately cool and humid natural conditions prevailed at the beginning of the early Middle Ages (IV century AD). The middle of the epoch (IV-VII centuries AD) is characterized by the highest humidity under a similar thermal regime. At the end of the early Medieval period (VII-X centuries AD), there is a decrease in moisture content, as well as a short-term warming.

The analysis of the literature materials allowed us to establish that at the time under review, the adjacent territories of Western Siberia also experienced environmental changes in the direction of optimization. The Baraba lowland (forest-steppe zone) shows an increase in the average annual precipitation rate by 20-50 mm/year and a slight cold snap (Volkova, Bakhareva, and Levina, 1989). In the steppes of Northern Kazakhstan, atmospheric humidity was higher by 50-100 mm/year during moderate cooling, and its values are characterized by a larger amplitude, which may be associated with an increase in the continental climate [Ivanov, 2006], and the distribution of pine forests here also dates back to this time [Kremenetsky, Tarasov, and Cherkinsky, 1994]. It is revealed that wet natural conditions gradually give way to arid ones in the direction of deeper Eurasia. Thus, in the dry steppes of Central Mongolia, climate aridization was observed during the historical period under consideration (Wipper et al., 1989).

Analysis of the studied soils showed that in the IV-VI centuries AD, wetter natural conditions typical of the northern forest-steppe prevailed in the area of the Ust-Utyak-1 settlement. Most likely, the maximum moisture content occurred during this period, as evidenced by the state of the buried soil (high degree of leaching, salinity). Our conclusion is in good agreement with the palynological data obtained from archaeological sites of the Tobolsk-Ishim interfluve (Ryabogina, 2008). Paleosoil studies and literature analysis have shown that the humid period was short and probably lasted for about 100-150 years. Nevertheless, it is reflected in the evolution of the soil cover at the subtype level. The high rate and intensity of soil processes can be explained by regional natural features (prevailing light grain size distribution of soils, microclimate). In the area of the Ust-Utyak-1 archaeological site in recent years 1 300 - 1 500 leached chernozems evolved into typical ones, which indicates a general arid trend in the natural conditions of the forest-steppe zone of the Middle Volga region at this time.

The humid, moderately cool period of the IV-VI centuries A.D. correlates well with ethno-cultural processes in the region. At this time, the Bakal culture flourished, fortified settlements with good fortifications appeared, and contacts with neighboring peoples grew [Botalov et al., 2008]. The deterioration of natural conditions in the second half of the sixth century AD coincides with the beginning of the decline of the Bakal culture. Consequently, the change in the natural environment was one of the significant factors (along with political, socio-economic ones) that influenced the life of the early medieval population of the forest-steppes of the Middle Volga region and predetermined the further course of its development.

Conclusion

Comprehensive soil and archaeological studies of the Ust-Utyak-1 settlement and its environs, as well as an analysis of the literature on the paleogeography of the Middle Part of the Volga region, made it possible to study the state of soils and natural conditions in the IV-VI centuries AD and compare them with modern ones. It is established that for the last 1 300 - 1 500 zonal soils have changed at the subtype level over the past few years. There was an evolution of leached chernozems into typical ones, which was a reflection of the changed natural environment. The morphological structure and chemical properties of the paleosol indicate its development in wetter natural conditions than at present. Our conclusions are in good agreement with the data of spore-pollen analysis (Ryabogina, 2008)

about the humid period in the first half of the Early Medieval epoch (IV-VII centuries AD). We assume that it lasted no more than 100-150 years and led to noticeable changes in the environment.

Thus, in the IV-VI centuries AD, a favorable natural environment was established on the territory of the Middle Pritobol region (in the area of the Ust-Utyak-1 settlement), which manifested itself in an increase in the average annual precipitation rate and landscape optimization. The soil cover was dominated by leached chernozems. Apparently, after the sixth century AD, the development of the environment was characterized by a tendency to aridization, which later led to the evolution of zonal soils at the subtype level. At present, the soil cover is dominated by typical chernozems, which developed in more arid natural conditions.

Finally, we note that environmental optimization affected the development of early medieval societies. Thus, the flourishing of the Bakal culture coincides with a favorable hydrothermal period in the forest-steppes of the Middle Partobol region in the early Middle Ages.

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The article was submitted to the Editorial Board on 28.07.11, in the final version-on 23.11.11.

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