Basic information about the soils of the Ryazan region. Soil and climatic conditions in the Ryazan region

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Control work on soil science

TOPIC: Soils of the Ryazan region

specialty nature management

1. Soils in the Land Code of the Russian Federation

2. The composition of the soil cover of the Ryazan region

3. Soils under different land use

4. Problems of rational use and protection of soils

Conclusion

Bibliography

1. Soils in the Land Code of the Russian Federation

1. The Federal Law "On Environmental Protection" of 2002 recognizes the objects of nature protection from pollution, depletion, degradation, damage, destruction and other negative impact economic and other activities of not only land, subsoil, but also soil (Article 4 of the Law).

Although Art. 6 of the Land Code of the Russian Federation does not name soil among the objects of land relations, it does not follow from this that the surface fertile layer of land plots is not subject to legal protection. First, Art. 6 recognizes the lands " natural object and natural resource”, which cannot be without soils - belonging to the natural component of land plots. Secondly, in other articles of the Code, the soil and the protection of its fertility are repeatedly mentioned when it is prescribed to remove and preserve the upper fertile layer during the construction of any objects, during the reclamation of lands whose fertility has been disturbed, the reclamation and chemicalization of agricultural land, etc. Does it practical value allocation of soils as a special object of legal protection? Undoubtedly.

The owner of the land plot receives the land for use, of course, together with the soil, but he cannot dispose of it separately from the land plot. Thus, a land owner, for example, a foreign investor, having bought highly fertile agricultural land (chernozems), cannot withdraw, “scalp” the territory and sell the soil like an ordinary commodity. He can sell a plot of land with soil, but not separately soil. If, for various construction needs, the surface layer of soil is removed, then the owner of the land, having the right to sell the land plot, cannot do this separately from the soil. Consequently, the soil is the national property of Russia, not subject to free sale, despite the fact that there is a physical possibility to separate it from the natural environment.

2. Earth and topsoil, being integral integral part all ecological system of our planet, are inextricably linked with its other parts: waters, forests, animals and flora, minerals and other values ​​of the bowels of the earth. Without land and soil, it is almost impossible to use other natural resources. At the same time, mismanagement in relation to the land will immediately or in the near future harm the entire environment. natural environment, lead not only to the destruction of the surface layer of the earth - soil, their erosion, salinization, waterlogging, chemical and radioactive contamination, but also be accompanied by environmental deterioration of the entire natural complex. Therefore, land protection is considered as ensuring (preserving) the basis of life and activity of the population and creating conditions for sustainable development society (Article 9 of the Constitution of the Russian Federation, Article 12 of the Labor Code of the Russian Federation). Consequently, all categories of land, both agricultural and non-agricultural use, are subject to protection. But priority in this regard deserves agricultural lands and lands of specially protected areas (reserves, national parks, wildlife sanctuaries, etc.). The mode of use and protection of specially protected lands is determined by the Law of the Russian Federation "On Specially Protected Natural Territories".

3. As stated in Art. 79 3K of the Russian Federation, agricultural lands - arable lands, hayfields, pastures, fallow lands, lands occupied by perennial plantations (gardens, vineyards and others) - as part of agricultural lands have priority in use and are subject to special protection.

For the construction of industrial facilities and other non-agricultural needs, lands unsuitable for agricultural production, or agricultural lands from agricultural lands of poorer quality at the cadastral value are provided. For the construction of power transmission lines, communications, main pipelines and other similar structures, it is allowed to provide agricultural land from agricultural land of a higher quality. But then these structures are located mainly along the roads and the boundaries of crop rotation fields.

Withdrawal, including by redemption, in order to provide for non-agricultural use of agricultural land, the cadastral value of which exceeds its average regional level, is allowed only in exceptional cases related to the fulfillment of international obligations of the Russian Federation, ensuring the defense and security of the state, the development of mineral deposits minerals (with the exception of common minerals), the content of objects cultural heritage R.F., construction and maintenance of cultural, social, educational facilities, roads, main pipelines, power lines, communications and other similar structures in the absence of other options for the possible placement of these facilities.

Particularly valuable productive agricultural lands, including agricultural lands of experimental production units of research organizations and educational and experimental units educational institutions higher vocational education, agricultural land, the cadastral value of which significantly exceeds the average district level, may be, in accordance with the legislation of the subjects of the Russian Federation. included in the list of lands, the use of which for other purposes is not allowed.

The use of land shares resulting from the privatization of agricultural land is regulated by the Federal Law on the Turnover of Agricultural Land.

4. The goals of land and soil protection are formulated in Art. 12 RF LC:

1) prevention of degradation, pollution, littering, disturbance of land, other negative (harmful) impacts of economic activity;

2) ensuring the improvement and restoration of degraded lands.

In order to strengthen the protection of agricultural land, the Federal Law “On State Regulation of Ensuring the Fertility of Agricultural Lands” was issued.

As a rule, work on the protection of lands and soils should be carried out by its right holders: owners, landowners, land users, tenants at their own expense. In cases of damage to land and soils by other entities, it is compensated at the expense of the tortfeasors. In necessary cases, the state comes to the aid of land users by allocating funds from the budget, because it is not always possible to implement law enforcement measures only at the expense of the subjects of the right to land, especially when large expenditures of funds and labor are required.

2. Composition of the soilcover of the Ryazan region

Soils of mixed coniferous deciduous forests

Soddy-podzolic soils of the zone of mixed coniferous-deciduous forests are widespread in northern regions Ryazan region. Here, conditions are created for the soddy process to occur, leading to the formation of a humus-accumulative horizon and a weakening of the podzolic process. This circumstance is explained by the fact that in mixed forests there are broad-leaved and small-leaved tree species, in the terrestrial layer there are many herbs. As part of the biological cycle, nitrogen is in the lead, ash elements - Ca, Mg, K, P, S, Fe, Si - are less active. Therefore, with good drainage under the conditions of the leaching water regime, soddy-podzolic soils are formed. The natural fertility of these soils is low due to the acid reaction of the environment, the low degree of saturation with bases, low humus content, a small range of active moisture, and low availability of biogenic elements. The predominant part of soddy-podzolic soils is in the forest fund, their involvement in agriculture is carried out during chemical reclamation (liming, application of organic and mineral fertilizers, green manure). Deprived of vegetation, sandy varieties of these soils are subject to deflation. Soddy-podzolic soils often become waterlogged in burnt areas and clearings.

In the subzone of the southern taiga, with difficult natural drainage, usually in depressions, soddy-podzolic soils undergo gley formation, which leads to their transformation into bog-podzolic soils under conditions of stagnant-leaching water regime. Increased moisture is accompanied by the accumulation of coarse humus and the intensification of eluvial processes. The increase in diagnostic signs of podzolization and gleying is well expressed in catenas on the alluvial outwash plains of Meshchera and in other woodlands. The composition of the catena from top to bottom along the slope, as moisture increases, includes the following soils:

weakly podzolic > podzolic > strongly podzolic deep gley > podzolic gley > podzolic gley > sod gley > peaty gley.

Woodlands were characterized by widespread in the second half of the 20th century. carrying out drainage and chemical reclamation, which made it possible to significantly increase the fertility of bog-podzolic soils and increase the area of ​​agricultural land.

Bog soils on the territory of the region are formed mainly in the subtaiga zone on leveled areas composed of water-resistant rocks. This situation has developed mainly in the Meshcherskaya and Moksha lowlands, where vast sandy massifs on ancient alluvial plains are underlain by water-resistant Jurassic clays.

Bogs and bog soils are formed under conditions of stagnant water regime with excessive surface, ground or mixed moisture.

According to the nature of water supply and availability of mineral biogenic substances, bogs are divided into upland (oligotrophic), transitional (mesotrophic) and lowland (eutrophic).

The formation of raised bogs occurs on watersheds and is associated with surface bogging, when atmospheric ultra-fresh water accumulates in various depressions. In addition, raised bogs can form with the growth of rafting on lakes with relatively steep banks. As the peat layer grows, marsh high peat soil gradually forms. Oligotrophic peat is formed mainly by sphagnum mosses. Under conditions of swamping by atmospheric waters, the marsh high-moor peat soil acquires a low ash content (0.5–3.5%) and a very acidic reaction of the environment (pH = 2.8–3.6). Under the tow of living sphagnum mosses, there is a peat horizon with low water permeability, over which water stagnates. All these unfavorable properties determine the low fertility of the marsh high peat soil.

Sometimes the formation of raised bogs is associated with the swamping of the land with fresh (soft) groundwater, which is explained by the rise of their level in the soil horizons. In this case precipitation, seeping through non-carbonate rocks, stagnate on moraine, cover, lacustrine deposits with low water permeability. The high standing of groundwater causes excessive soil moisture, leads to the formation of peat-gley and peat soil of the raised bog.

Transitional swamps are formed by mixed swamping and have an atmospheric-soil type of nutrition. Perhaps the emergence of transitional swamps when overgrowing reservoirs. Mesotrophic peats of transitional bogs are close in their properties and nature of use to oligotrophic peats, although the conditions for mineral nutrition of plants are more favorable due to some influence of groundwater.

Lowland swamps occur when soil moisture and overgrowth of lakes. These swamps are eutrophic, characterized by a significant content of minerals brought by groundwater. Therefore, the composition of peat-forming plants in lowland bogs is more diverse: sedge, reed, cattail, alder, birch, spruce, and pine. Peat soils of lowland bogs are characterized by high ash content (more than 6%), slightly acidic and neutral reaction of the environment (pH = 5 - 7), and good drainage capacity.

The lowland swamps of Meshchera are characterized by the accumulation of swamp ore

(accumulations of limonite). Swamping with hard groundwater contributes to the deposition of marl, as is observed, for example, in the floodplain of the Oka and its tributaries. In the presence of mineral impurities (limonite, marl), the ash content of lowland peat can increase up to 20-30%.

The formation of swamps and bog soils is primarily associated with the formation and accumulation of peat, which constitutes the organogenic horizon. The deposition of peat is the result of delayed decomposition plant residues in the anaerobic environment typical of subaqueous landscapes. In the middle and southern taiga of the European territory of Russia, the growth of the peat horizon of soils occurs very slowly - at a rate of 1 cm per year. Over a millennium, a peat layer of about 1 m is formed on the surface of the mineral bottom of the swamp.

Under the peat horizon in bog soils there is a mineral gley horizon. Therefore, the profile of bog soils has a simple T-O structure.

Depending on the thickness of the peat layer, bog soils are distinguished on small peat (less than 100 cm), on medium peat (100 - 200 cm) and on powerful peat (more than 200 cm).

Bog soils can evolve under changing conditions of water supply and under the influence of the succession of peat-forming plants. For example, when the groundwater is separated from the capillary rim, the soils of lowland bogs can be transformed into transitional and upland bog soils.

In the second half of the XX century. in the Ryazan region, large-scale drainage reclamation of wetlands was carried out in order to develop grassland and agriculture. With a reclamation drainage fund of 320 thousand hectares, 100 thousand hectares were drained, including about 40 thousand hectares by closed drainage. The main massifs of drained lands are located in the northern part of the Ryazan region, i.e., in the Meshcherskaya and Mokshinskaya lowlands, as well as in the floodplain of the Oka.

Drainage of infertile soils of upland and transitional bogs is considered inexpedient. Therefore, after drainage, the sphagnum peat deposit is used for fuel, compost, and bedding for livestock. The natural, non-drained state of these swamps allows them to be preserved as water protection areas, valuable hunting grounds, berry fields, plantations of medicinal herbs.

Basically, the objects of reclamation were eutrophic soils of lowland bogs, capable of providing agricultural plants with elements of mineral nutrition.

The involvement of drained lowland bog soils in agriculture causes a number of negative environmental consequences, which is associated with their hydrothermal and pyrogenic degradation.

A decrease in the moisture content of these soils after drainage reclamation leads to shrinkage of the peat deposit, an increase in the temperature of organic horizons, an increase in soil aeration, a change in the reducing environment to an oxidizing one, and an increase in biological activity. Under the new hydrothermal conditions, peat (especially grassy and mossy) quickly decomposes with the formation of carbon dioxide, water, and nitrates. An increase in the concentration of carbon dioxide in the surface layer causes a local "greenhouse effect", which further increases the temperature of the peat. Tillage, crop rotation type also have a significant impact on the hydrothermal and biochemical degradation of drained peat soils. As a result, the natural process of conservation of carbon and nitrogen in the organic matter of bog soils is replaced by the irreversible loss of this chemical element due to peat mineralization, crop removal by crops, wind erosion, and leaching with groundwater. The peat horizon of soils decreases most rapidly in tilled crop rotations (at a rate of up to 3 cm per year), that is, when cultivating vegetables and potatoes, a meter-long peat deposit formed over a millennium will disappear within 35-40 years. In its place will be the underlying mineral rock. In the woodlands one should expect the appearance of low-fertile sandy gleyzems.

Another type of degradation of drained peat soils up to their complete disappearance is caused by pyrogenic factors. Usually, during the low-water period, devastating fires occur on drained swamps, often leading to complete burnout of peat to the mineral bottom of the swamps. In Polissya landscapes, peat soils are underlain by a thick layer of fluvioglacial and ancient alluvial barren gleyed quartz sands. After the peat deposit burns out, these sands come to the surface. In addition, the hypsometric level of the territory is noticeably reduced, which contributes to intensive secondary swamping of the previously drained swamp massif. It should also be noted that fires cause many negative social consequences associated with atmospheric smoke.

To protect drained peat soils from accelerated biochemical mineralization and fires, sanding is used as an agro-reclamation measure, i.e., the introduction of sand into the arable horizon or onto its surface. In order to maintain a positive balance of organic matter on reclaimed peat lowland soils, grass-field crop rotations are introduced, hayfields and pastures are created.

With a slight accumulation of organic matter in the form of peat (less than 30%) in lowland and transitional bogs, bog mineral soils related to gleyzems are isolated: humus-gley, soddy-gley, and silt-gley. The profile of these soils includes organic (Am) and gley (G) horizons.

The soddy-gley soils of the subtaiga zone are classified as waterlogged (semi-boggy) because they are characterized by a long-term water-stagnant type of water regime. In this regard, soddy soils usually occupy poorly drained areas: depressions on interfluves, slopes, etc. The largest massifs of soddy-gley soils are located mainly in the northern regions of the Ryazan region.

The formation of soddy-gley soils is associated with the occurrence of two soil-forming processes, namely, soddy and gley, which are accompanied by biogenic and hydrogenic accumulation of chemical elements. The development of the soddy process is due to herbaceous meadow vegetation, resulting in the formation of a powerful soil horizon with a high content of humus (10 -15%), a large absorption capacity (30 - 40 meq / 100 g of soil), a significant saturation with bases, a neutral or slightly acidic reaction and water-stable structure. Gleying is caused by prolonged stagnation of water in the soil, which is reflected in the appearance of the corresponding morphochromatic features in the form of alternating dove (bluish, greenish, gray) and ocher rusty spots in the soil horizons and in the parent rock. Depending on the type of waterlogging (surface, ground, mixed), signs of gleying appear in different parts soil profile (horizons Аg, Вg, G). Due to waterlogging, soddy-gley soils may contain peaty litter, under which there is a humus horizon (At horizon).

Soddy-gley soils have a large reserve of biogenic elements, but have an unfavorable water-air regime. After draining, these soils are introduced into agroecosystems.

Soils of the broad-leaved forest zone

In the central part of the Ryazan region, in the zone of broad-leaved forests, gray forest soils of predominantly heavy granulometric composition were formed. Due to the large dissection of the relief and good drainage of the territory, there are few gleyed soils among them, but for the same reason there are many subcategories that differ in the degree of erosion.

As a rule, in the watershed parts of the interfluves, the most eluvial light gray forest soils are located here, which in the direction of the valleys are replaced by gray and then dark gray forest soils with their inherent accumulation of substances.

Significant podzolization and low humus content bring light gray forest soils closer to soddy-podzolic soils. On the contrary, the predominance of clay-illuvial and humus-accumulative processes in dark gray forest soils allows us to consider them in terms of classification as a transitional variant to chernozems. Therefore, from light gray forest soils to gray and dark gray forest soils, the thickness of the humus horizon increases, the amount of humus increases, and the content of humic acids increases; the acidic reaction of the medium changes to slightly acidic; the degree of saturation of the soil base and the content of exchangeable calcium increase;

soil structure and water-physical properties are improved.

In general, gray forest soils are favorable for agricultural use, but they require the use of organic and mineral fertilizers, as well as anti-erosion measures.

forest soils steppe zone

Podzolized and leached chernozems formed under the meadow steppes and steppe meadows occupying southern part Ryazan region.

During the formation of chernozems, the processes of accumulation of substances predominate, which in the forest-steppe zone is facilitated by the periodically leaching water regime. Podzolized chernozems gravitate towards watershed areas of interfluves and to those areas where the processes of eluviation of substances proceed more intensively. The leached chernozems are located lower, i.e., they are predominantly in transit and accumulative conditions. Within the Ryazan part of the Central Russian Upland, podzolized chernozems are more common, since more favorable conditions are created here for the development of eluvial processes. On the Oka-Donskoy flatland, on the contrary, these processes are weakened, so there are more leached chernozems, and there are also typical chernozems.

The course of the humus-accumulative process was facilitated by the initial dense and high herbage of the meadow steppes, which was dominated by herbs and cereals. Meadow-steppe vegetation is characterized by a sharp excess of underground phytomass over ground and a larger relative value of annual litter, with which 700 kg/ha of nitrogen and ash elements enter the soil. The composition of the biological cycle is dominated by calcium and nitrogen with a significant participation of silica. During the summer moisture deficit in the soil, the decomposition of organic residues was slow, which contributed to the humification of organic residues, some of which, not having time to decompose, accumulated in the form of steppe felt on the soil surface. The content of humus in horizon A of virgin chernozems reached 6–8% (400–500 t/ha), which ensured high natural soil fertility. Humus is characterized by a low ability to migrate, resistant to microbial decomposition, which contributes to its accumulation in the soil. The thickness of the humus horizon is 60 - 80 cm.

Chernozems have a slightly acid reaction of the environment of the upper part of the profile, a high cation exchange capacity and a high content of calcium, calcareous neoplasms, and a good supply of biophilic elements.

Chernozems are especially distinguished by their agrophysical properties. Due to the high content of humus, calcium, and silt, they have a good water-resistant structure of the humus horizon, which makes these soils loose, water- and breath-permeable, and moisture-intensive.

However, due to plowing, the original meadow-steppe vegetation was almost not preserved, which led to the disruption of the biological cycle of substances and the dehumification of chernozems.

With the agricultural use of chernozem soils (mainly for arable land), their fertility is lost due to erosion, loss of humus and deterioration of the soil structure. To maintain fertility, it is necessary to apply organic, nitrogen and phosphorus fertilizers, use anti-erosion measures, accumulate and retain moisture in the soil, and irrigate.

Meadow-chernozem (non-floodplain) soils, also referred to as waterlogged soils, are common in the forest-steppe zone among chernozems, but differ from the latter by the imposition of weak hydromorphism on the main (chernozem) type of soil formation. Therefore, meadow chernozem soils are considered as semihydromorphic analogues of chernozems. In the northern forest-steppe, meadow-chernozem soils can also be found among gray forest soils.

The term "meadow" in this case means temporary overmoistening of soils with fresh groundwater, which, as a rule, is located relatively shallow - 3 - 6 m from the day surface. A shallow occurrence of the groundwater level is observed on flat undrained watersheds, in depressions and hollows, on deluvial plumes.

During snowmelt or after heavy rains the capillary fringe of groundwater reaches the soil horizons, which leads to a short-term watering of the soil. In summer, the groundwater level drops and top part the soil dries up. Therefore, meadow chernozem soils have a pulsating type of water regime, which consists of short-term water-stagnation-leaching and desuctive-effusion types.

Features of the water regime of meadow chernozem soils favorably distinguish them from chernozems. As is known, chernozems are characterized by a noticeable water deficit in the soil during the growing season. On the contrary, meadow chernozem soils better provide grassy meadow vegetation with water and mineral nutrients due to the shallow position of the capillary fringe of groundwater. As a result, the sod process intensifies, the humus content of the soil increases.

The profile of meadow chernozem soils is morphologically similar to the soil profile of chernozems. However, under the influence of weak hydromorphism, the thickness of the humus horizon increases, it acquires a more intense (usually black) color; in the lower part of the soil profile (horizons Bg and G), morphochromatic signs of gleying are noted.

The soil cover of the forest-steppe consists of spots of non-contrasting soils - meadow-chernozem soils, chernozems of varying degrees of leaching, etc. Therefore, there are no significant differences in the use of chernozems and meadow-chernozem soils, although the latter, due to greater moisture content, are more often occupied by hayfields and pastures without drainage.

Intrazonal soils

Alluvial (floodplain) soils belong to intrazonal soils, since they are located in river floodplains, where the influence of river waters largely levels out the effect of zonal factors of soil formation. In the Ryazan region, alluvial soils are ubiquitous, but especially large massifs of these soils are confined to the Oka floodplain.

According to the type of water regime, alluvial soils are classified as soils of periodic flooding. Therefore, their formation occurs under the influence of two processes: alluvial (deposition of fertile silt) and flood (flooding during floods). An important role in the formation of alluvial soils is played by groundwater, as well as surface runoff water from the slopes of the river valley. Thus, alluvial soils are formed under conditions of predominant accumulation of substances.

The influence of the floodplain and alluvial processes is not the same in different parts of the floodplain, which leads to the formation of three subgroups of alluvial soil types.

Alluvial soddy soils occupy the near-channel part of the floodplain, as well as manes in the central floodplain. They are characterized by pronounced stratification, which allows them to be called "floodplain stratified soils". In these soils, a predominantly sandy-pebble granulometric composition is observed, an insignificant participation of groundwater in soil formation is observed, since the near-channel areas are well drained by the river and groundwater is deep during the low-water period. The vegetation is represented by depleted xerophilic, often psammophyte meadows and shrubs (willows). The soddy process proceeds poorly, so the humus horizon is underdeveloped. Insignificant content of humus (1-3%) and light granulometric composition determine the low capacity of cation exchange (10-15 meq/100 g), low buffering capacity and acid reaction of the medium. In general, alluvial soddy soils are underdeveloped, which is reflected in the shortened structure of the profile, consisting of a humus horizon A 15–20 cm thick, underlain by a layered parent rock (horizon C). These soils are often renewed, since the erosion-accumulation activity of the river in the near-channel part is especially intense. Typically, the formation of young soil occurs on pre-existing soil buried under fresh alluvium. The fertility of alluvial soddy soils is low.

Alluvial meadow soils are formed in the central part of the floodplain mainly on loamy alluvium. Groundwater is located relatively shallow (1 - 2 m) and has a significant effect on soil formation even in the low-water period, providing grassy meadow vegetation with additional moisture and minerals. In addition to meadow vegetation, oak forests can grow in the central floodplain.

In water meadows, highly productive forb-grass vegetation has a powerful root system. Therefore, the sod process and humus formation proceed intensively here. A powerful root system, covering a soil layer of several tens of centimeters, has a loosening effect on the mineral substrate and, thereby, contributes to the formation of an agronomically valuable soil structure. There are numerous "beads" on the roots. The soil is dominated by granular mesoaggregates with good water resistance and porosity. Therefore, alluvial meadow soils are also called "floodplain granular". Structure formation in these soils is so intense that the initial layering of alluvium in them is difficult to detect visually; it is often established only by laboratory-analytical methods.

Abundant soil mesofauna and diverse microflora also take part in the process of structure formation. The aggregation of the soil mass is associated with the presence of structure-forming substances that glue individual soil particles into aggregates. Such substances include humus, iron hydroxides, silt, lime, microbial mucus, etc. Such a soil structure provides an optimal water-air and nutrient regime for plants.

Soil hydromorphism manifests itself in the form of color signs of gleying of the middle and lower parts of the soil profile, as well as in the presence of ferromanganese or carbonate nodules. The chemical composition of nodules depends on the degree of mineralization of groundwater and the reaction of the environment in the soil: iron and manganese are deposited from fresh water at the oxygen barrier, meadow lime is formed from hard water in saturated and carbonate soils. In addition, bright blue spots can be observed in gleyed horizons against a dirty gray background. These are accumulations of the mineral kerchenite (FePO 4), which quickly acquire a brown (to red) color in air due to the oxidation and hydration of iron with the formation of the mineral beraunite (FePO 4 * Fe (OH) 3 * 3H 2 O).

Alluvial meadow soils are more developed than alluvial soddy soils, which is explained by the lesser influence of the erosive-accumulative activity of the river. The profile of alluvial meadow soils consists of horizons transitional in terms of humus content: Ad-A-AC-Cg. In the humus-accumulative horizon, the humus content is high (8-12%). A significant degree of soil humus content and loamy mineralogical composition determine the high capacity of cation exchange (20 - 30 meq/100 g). Depending on the chemical composition groundwater and the mineralogical composition of alluvium, soils can have a different reaction of the environment - from acidic to neutral.

Alluvial meadow soils, along with chernozems, are the most fertile. Moreover, alluvial meadow soils have a number of significant advantages over chernozems: 1) under natural vegetation on leveled floodplains, they are almost not subject to water erosion; 2) their high natural fertility is constantly renewed by the alluvial process and other factors of accumulation of substances in heteronomous landscapes; 3) they are optimal for herbaceous plants water regime, since ground moisture is added to atmospheric moisture.

Alluvial bog soils are formed in the near-terrace area, in oxbow and interridge depressions. They are under the influence of alluvial river waters, wedged out slope flow of groundwater, and surface runoff. Therefore, they are characterized by intense hydromorphism caused by the wedging out of groundwater and, accordingly, by the stagnant regime. The speed of river waters entering the terrace area during floods is low, therefore, clayey alluvium predominates (the second name of these soils is silt-humus-gley, silt-peat). Waterlogging contributes to the formation of hydrophytic plant associations: sedge-reed, black alder and others, characteristic of lowland eutrophic bogs. Hydrogen-accumulative provide a high content of biogenic elements, including nitrogen and phosphorus. Depending on the conditions of accumulation of organic matter in the soil, humus (A) or peat (T) horizons are formed, under which there is a gley horizon (G).

In place of highly productive water meadows, agroecosystems with a number of negative properties arose. The soils of such agroecosystems are characterized by less fertility than their natural counterparts. The degradation of soil properties is primarily due to the destruction of the natural soil-protective grass cover. As a result, soil dehumification develops against the background of a negative humus balance, destructuring due to the use of irrigation equipment and improper soil cultivation, a decrease in the number of soil mesofauna and an increase in pathogenic microflora, soil and plant products are contaminated with heavy metals coming from irrigation river waters and fertilizers, etc.

Currently, irrigation and drainage facilities in the floodplains are actually abandoned, which leads to the gradual restoration of natural grassy meadow vegetation.

Alluvial soils near Ryazan and other cities are being destroyed, which is explained by the construction of various kinds of objects on them.

The decrease in the fertility of alluvial soils is partly due to an increase in water intake in the Moscow region and, as a result, the shallowing of the Oka and its tributaries, and a decrease in the amount of alluvium.

Washed-out and washed-out soils of slopes and bottoms of ravines, gullies, small rivers, and adjacent slopes are characteristic of territories with increased horizontal and vertical dissection and, accordingly, a developed erosion network.

These soils do not form an independent soil type, since they are eroded and washed-out variants of the main soil types among which they are common. However, erosion-accumulation processes also create some differences. Thus, washed and reclaimed soils are in conditions of increased migration of substances and are constantly “rejuvenated”. They are underdeveloped soils with a shortened (washed out soil) or increased (washed out soil) soil profile of the primitive structure A - (AS) - C.

In eroded soils, the humus horizon is reduced and may be completely absent. Alluvial soils are characterized by lithological layering of deluvial and deluvial-alluvial origin; therefore, they contain buried soil humus horizons of different thicknesses. In general, the structure of the profile of eroded and reclaimed soils depends on the intensity of erosion-accumulation processes. For example, when slopes are plowed, the thickness of eroded soils occupying autonomous positions in landscapes decreases, while the thickness of eroded soils of heteronomous positions, on the contrary, increases.

As a rule, these soils have a peculiar water and temperature regime in accordance with the position in the mesoform of the relief, which is reflected in soil formation. So, the appearance of soil and plant groups that are not characteristic of this area depends on the exposure of the slope. natural area. For example, in the zone of deciduous forests, the southern slopes of the ravines can be occupied by steppe meadows on chernozems, which is typical of the steppe zone.

Belonging to a certain relief element determines the direction and intensity of geochemical processes and affects the development of the main and additional soil-forming processes. For example, eroded soils are more podzolized and leached, which is a consequence of intensive eluviation of substances. Alluvial soils are more often gleyed, more humus-rich, sometimes peaty, contain concretions, and have a heavier granulometric composition.

The properties of eroded and reclaimed soils can differ significantly from the main zonal soils, which is due to the lithological heterogeneity of parent rocks. For example, the riverine plains of the Oka-Tsna plateau in the Shatsk region are occupied by eroded chernozems on mantle loams underlain by ancient sandy alluvium. On the slopes of valleys and gullies, erosion destroyed both the parent and underlying rocks. Therefore, washed away soils are represented by primitive soddy-calcareous soils on limestone eluvium; the reclaimed soils of the deluvial plumes are primitive soddy sandy soils.

Consequently, within the tree-like erosion network, there is a significant diversity of the soil cover associated with the diversity of local factors of soil formation. This circumstance makes soil mapping very difficult, which is reflected in the grouping of various soils into one group: eroded and washed-out soils of ravines, gullies, small rivers, and adjacent slopes.

Washed and washed-out soils of slopes and bottoms of ravines, gullies, small rivers are especially in need of preserving the natural vegetation cover due to increased erosion hazard. Therefore, it is more expedient to use them for hayfields and pastures.

3 . Soils under different land use

Schematic soil map PYazan region

(genetic characteristic)

1. Peat-podzolic-gley. 2. Light gray forest. 3. Chernozems leached. 4. Dark gray forest. 5. Podzolized chernozems. 6. Gray forest. 7. Alluvial (floodplain). 8. Sod-medium podzolic. 9. Sod-strongly podzolic. 10. Sod-podzolic-gley. 11. Humus-gley. 12. Sod-weakly podzolic. 13. Humus-peat. 14. Peat. 15 Meadow-chernozem. 16. Fat powerful chernozems.

4. The problem is rationalth use and protection of soils

land use soil forest ryazan

The problem of rational use of soils is inextricably linked with another no less urgent problem - their protection. Soil protection, as part of an even broader problem of environmental protection and the rational use of natural resources, became particularly acute in the second half of the 20th century. the following reasons.

First, in connection with scientific and technological progress, it became obvious that the natural resources of the planet are not unlimited. Given the rapidly growing needs of human society and social production, a deep revision of the strategy for using global resources has become necessary. First of all, this applies to soils, more precisely, using the term of V. I. Vernadsky, “pedosphere”, which plays a major role in providing the population of the planet with food.

Secondly, the soil, the pedosphere of the planet is inextricably linked with the process of metabolism and energy with other components of the biosphere. Ill-considered anthropogenic impact on individual natural ingredients inevitably affects the state of the soil cover - a change in the water regime after deforestation or waterlogging of fertile floodplain lands due to a rise in the level of groundwater after the construction of hydroelectric power stations.

A serious problem is caused by anthropogenic soil pollution. The uncontrollably growing amount of emissions of industrial and domestic waste in environment reached dangerous levels in the second half of this century. Chemical compounds that pollute natural waters, air and soil enter plant and animal organisms through trophic chains. This is accompanied by a gradual increase in the concentration of toxicants, which can have the most undesirable consequences. The implementation of urgent measures to protect the biosphere from pollution and more economical and rational use of natural resources is a global task of our time, on the successful solution of which the future of mankind depends. In this regard, the protection of the soil cover, which receives most of the technogenic pollutants, partially fixes them in the soil mass, partially transforms them and includes them in migration flows, is of particular importance.

Soil protection is not an end in itself, but a means for preserving and optimizing their properties, primarily fertility. The soil must be protected from the influence of processes that destroy its valuable properties - structure, content of soil humus, microbial population, and at the same time from the ingress and accumulation of harmful and toxic substances. Therefore, soil protection should be considered as a system of measures aimed at the conservation, qualitative improvement and rational use of the land funds of our country and the planet as a whole.

The territory of the Ryazan region is affected by both exogenous geological processes (EGP) and anthropogenic ones.

Specialized work on the study of EGP on the territory of the Ryazan region began to be carried out in the late 70s - early 80s.

Since 1999 the study of manifestations of exogenous geological processes on the territory of the Ryazan region is carried out by the branch of Ryazangeomonitoring.

As a result of the complex of works carried out, it was established that erosion, landslide, karst processes and swamping of river floodplains are most common.

erosion processes cover 60% of the region.

Erosion processes, which are represented by gully and river lateral erosion, are the most widespread in the study area.

Ravine erosion. The ravine-gully network is widely developed in the Korablinsky, Miloslavsky, Skopipsky districts. Both large deep branched ravines and shallow gullies are observed here. Large ravines, as a rule, are stable and forested. In places, growth of ravines was noted - the formation of gullies and slush along the sides (Miloslavsky district). The upper reaches and near the edge of the ravines located within the settlements are often littered household waste, which prevents the examination and obtaining objective information.

The activation of the growth of the ravine-gully network is associated with spring floods and depends on meteorological conditions.

The gullies develop most actively on the slopes and in the edge part of the floodplain terraces.

River lateral erosion. Erosion processes are most intense on the bends of river channels during their meandering. Washout and landslide were noted along the sides of the rivers Muravka, Polotebnya (Miloslavsky district), Gremyachka, Slobodka, Kleshnya, Brusna (Skopinsky district), Mosha, Kaluzinka, Ranova, Khupta (Ryazhsky district). Molva, Ranov (Korablinsky district), as well as some small nameless rivers and streams.

Waterlogging. Bogging areas were noted in the floodplain parts of the rivers Muravka, Polotebnya (Miloslavsky district), Gremyachka, Slobodka, Kleshnya, Brusna (Skopinsky district), Mosha, Kaluzinka, Ranova (Ryazhsky district), Molva, Ranova (Korablinsky district).

Damping of streams in Miloslavsky, Skopinsky, Ryazhsky districts led to waterlogging of the thalwegs of beams and ravines.

Flooding. In the village of Sofiyevka, Miloslavsky district, there is flooding of the cellars of residential buildings in spring period, which most likely was the result of the construction of a pond on the southwestern outskirts of the village.

Karst phenomena. Most of the territory of the region is free from manifestations of karst. The area of ​​the territory affected by karst processes is 4.6 thousand km 2 . The average incidence is 0.2 karst manifestations per 1 km 2, varying from 0.01 to 2.3.

According to the materials of previous studies, various forms of karst are distinguished: underground (deep), buried and surface.

Underground forms include pores, caverns, cavities, which were encountered by many deep wells for various purposes at great depths and everywhere.

Buried forms of karst are also found during drilling in the central part of the Oka-Tsna swell.

Surface karst forms are represented by funnels, basins, karst logs and dry valleys, ponors, karst springs,

The area most affected by surface karst processes is the central part of the Oka-Tsninsky swell on the right bank of the Oka River (Kasimovsky, Pitelipsky, Shilovsky, Sasovsky districts). Represented by funnels, basins, karst logs.

Surface karst phenomena are distributed over the territory of the region extremely unevenly. Most of it is free from surface karst manifestations. The area of ​​areas intensively affected by karsts is 1600 km2, i.e. 4% area.

Karst-fissure waters serve as the basis for the water supply of many settlements in the region. Karst funnels with ponors serve as natural drains and in some cases can reduce the waterlogging of the territory. But, on the other hand, karst phenomena can cause deformations of various structures, create complications in the construction and operation of national economic facilities, and withdraw agricultural land from use. In order to prevent the adverse effects of karst, as well as to benefit from its presence, it is necessary to study its development and manifestation.

Human economic activity in general leads to an increase in karst processes - a decrease in the level of groundwater and an increase in water exchange associated with the exploitation of aquifers, as well as an increase in the aggressiveness of groundwater caused by pollution with industrial waste and infiltration of dissolved mineral fertilizers. Progression of the process of karst formation worsens the condition of agricultural lands, and through open karst sinkholes (v. Komsomolets, v. Zmeinka, Kasimovsky district), groundwater pollution is possible.

Landslide processes. The processes associated with the manifestation of gravity, the activity of surface and groundwater include landslides and mudflows. Based on the results of the work carried out by the Ryazangeomonitoring branch, as well as taking into account the data of previous researchers, more than 600 landslides are identified in the region. But despite the wide development and variety of forms, the distribution of landslides is extremely uneven. Most are located in the western part of the region (Rybnovsky, Mikhailovsky, Zakharovsky, Pronsky and Skopinsky districts). In the central (Spassky, Ryazansky, Shilovsky districts), northeastern (Kasimovsky District) and eastern (Sasovsky, Shatsky, Kadomsky districts) landslide processes are not so widespread, and within the Meshcherskaya lowland in the north of the region, they are practically absent. The formation of landslides is everywhere due to the deformation of clayey horizons involved in the geological structure of the slopes of valleys, sides of rivers and ravines. According to the age of the main deforming horizon, according to Lebkov N.N., landslides are divided into Quaternary, Cretaceous, Jurassic and Carboniferous.

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The predominant soils of the Ryazan region are chernozems (44%), gray forest soils (37%), sod-podzolic (13.8%), floodplain (5%), peat soils (4%).
In the Ryazan region, chernozems are mainly represented by leached and podzolized ones. The thickness of the humus horizon of leached chernozems varies from 69 to 110 cm. The structure is from granular to porous-lumpy. The granulometric composition is medium and heavy loamy.
The type of gray forest soils is divided into 3 subtypes: light gray, gray and dark gray. The thickness of horizon A is 31-38 cm, depending on the erosion and topography. The structure is lumpy-lumpy-powdery. There is a lot of silty fraction, stickiness is high, so a crust forms on the arable land.
Soddy-podzolic soils have different degrees of podzolization and gleying. They have a shallow humus horizon (20–39 cm), a thin illuvial horizon (17–30 cm), and closely spaced gley horizons. These are unstructured soils.
The northern part of the region, located in Meshchera, is represented along with soddy-podzolic alluvial meadow soils. They are characterized by a weak manifestation of the alluvial process at a shallow level of groundwater.
The supply of soils in the arable layer with mobile P and K is very high. Gray forest soil has its own natural features. It is characterized by a rich content of mobile phosphates in the parent rock, illuvial and humus horizons. Chernozems are enriched with phosphates. The nutrient regime of the arable layers of these sections differs in the content of acid-soluble phosphates and K due to the introduction of different fertilizer rates. Soddy-podzolic soils were systematically fertilized and limed; therefore, the content of mobile P and exchangeable K is very high here, and the reaction of the soil solution is neutral. Alluvial soils have a relatively well-cultivated arable layer, sufficiently supplied with phosphates, with a neutral reaction. The content of K is much less due to its large removal by vegetable crops, irrigation and groundwater.
An important characteristic of the soil cover is its availability of humus. Its content in the soils of the Ryazan region is low and very low. All types of soils contain the fulvate-humate type of humus.
All of the above agrophysical and agrochemical properties affect HM migration processes, since the geochemistry of HM migration forms is determined not by the properties of metal ions, but by the properties of their carriers.

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Other related news:

The climate of the Ryazan region located in the temperate climate zone, temperate continental with warm summer and moderately cold winters.

Regional climatic conditions are determined by the magnitude of solar radiation, the characteristics of the circulation of air masses, the nature of the underlying surface, and in some areas and economic activity person.

The amount of total solar radiation entering the earth's surface within the region increases from north to south from 90 to 95 kcal/cm-tod. The radiation balance changes accordingly from 33 to 35 kcal/cm-tod.

In winter, the radiation balance is negative, since the surface of the earth gives off more heat than it receives. average temperature the coldest month - January - decreases from west to east from -10.5 ° С in the Mikhailov region to -12 ° С on the border with the Republic of Mordovia. January isotherms, as well as on the Russian Plain as a whole, are elongated in the meridional direction.

Features and patterns of soil distribution

This is due to the fact that with a negative radiation balance in winter, heat is carried to the Russian Plain from the Atlantic. It is characteristic that in the southwestern, most elevated part of the region, the average January temperatures are relatively lower, down to -11 °С -11.2 °С. The effect of lowering the temperature is related to the altitude.

On average, the temperature decreases with height by 0.6 °C for every 100 m.

The average temperature of the warm month- July - rises from the northwest to the southeast from +18.5 °С to +19.5 °С. In most parts of the region, it is +19.0 °С - +19.2 °С. Most low values average July temperatures, as in January, are observed in the relatively elevated southwestern part of the region, which is associated with a decrease in temperature with height.

The average annual air temperature is positive.

In the northern regions of the region, it is slightly below +4 °С (in Elatma +3.9 °С), in the southern regions it is more than +4 °С (in Ryazhsk +4.6 °С). The duration of the frost-free period averages from 134 days in the northern part of the region to 150 days in the south. In some areas, depending on local conditions, there may be deviations from the characteristic average values.

So, in Ryazan, located in the northwestern part of the region, the frost-free period is 155 days, and in Ryazhsk, located 100 km south, it is 143 days.

Due to the position of the Russian Plain in temperate zone The territory of the region is characterized by a general transfer of air masses from west to east. At the same time, the center of the Russian Plain receives not only temperate marine air (MSA) from the Atlantic, but also Arctic marine air (MAA) from the Barents Sea and tropical air from mediterranean sea and Central Asia.

The direction of the wind in the surface layer varies widely, which is associated with seasonal changes in the position of areas with high and low pressure and the movement of cyclones and anticyclones.

In winter, when pressure is relatively low over the Barents Sea, and high in the south of the Russian Plain, southerly winds prevail in the Ryazan region (48% of the number of observations excluding calms).

Western and northwestern winds are quite characteristic (24%).

In summer, due to the decrease in air mass over the continent, in the western sector of the Arctic, the pressure is higher than over the Russian Plain.

On the territory of the region at this time, the western, northwestern and northern winds are the most repeatable. The arrival of relatively colder air from the Atlantic and the Arctic leads to a cooling of the surface. The arrival of MAS occurs in the rear parts of the cyclones and is accompanied by an increase atmospheric pressure and cessation of precipitation.

MAW quickly warms up and transforms into continental temperate air (CAM). With a relatively rarer influx of tropical air from the southeast of the Russian Plain, a significant increase in temperature to +30 ° C and above and a decrease in relative air humidity to 30% and below occur.

The bulk of the moisture in air masses coming to the Ryazan region - advective, smaller (about 10%) - the result of evaporation from the surface.

The main supplier of moisture is MUW coming from the Atlantic. About 70% of precipitation falls during the warm period - from April to October, and most of all to the north of the Oka valley. In the south of the region, the amount of precipitation during the warm period decreases to 300 mm or less. The exception is the southwestern part of the region, where the amount of precipitation during the warm period reaches 350 mm or more. Here, as in the case of air temperature, the relief factor affects. The height of the surface here is 50 - 60 m higher than the plain located to the east of the Oka-Donskoy plain and precipitation is 50 - 60 mm more.

In winter, snow cover forms throughout the region.

The average amount of precipitation during the cold period (November to April) ranges from 120 to 160 mm. A stable snow cover forms at the end of November and lasts until the end of March, sometimes until the second decade of April, i.e. from 145 days in the north to 136 days in the south. Its thickness reaches 0.3-0.5 m by the end of winter.

The annual amount of precipitation on the territory of the region ranges from 600 mm in the northern part and in the elevated southwest to 500 mm or less in the south.

In Ryazan, an average of 500 mm of precipitation falls annually. In some years there may be more or less of them. Precipitation is a necessary condition for surface moistening. However, the degree of moisture is determined not only by their quantity, but also by the ratio of the amount of precipitation and evaporation. When precipitation exceeds evapotranspiration, moisture is excessive, and when the ratio is reversed, it is insufficient.

The northern part of our region, located on the left bank of the Oka and on the right bank of the Moksha, is characterized by excessive moisture. To the south of Ryazan (approximately south of 54°30′ N), moisture becomes insufficient. The exception is the southwestern elevated part of the region, where the moisture coefficient is approximately 1.

In the Ryazan region, as elsewhere in the temperate zone, vegetation is most active at daily temperatures above +10 °C. Photosynthesis reaches its maximum at a temperature of +20 °C - +25 °C.

The duration of the active vegetation period in the region increases from north to south from 134 to 145 - 147 days. In the north, the transition of average daily temperatures through +10 ° C in spring occurs by the end of the first decade of May, in autumn - by the end of the second decade of September, in the south, respectively, on May 2-5 and September 25-28.

The sum of average daily temperatures above +10 °С (the sum of “active” temperatures) increases from north to south of the region from 2155 °С (Tuma) to 2355 °С (Ryazhsk). In the southwestern elevated part of the region, the sum of active temperatures is relatively low (Pavelets -2165 °C).

As elsewhere in the temperate zone, the seasons of the year are clearly expressed on the territory of the region.

A significant part of the territory is flat, in the northern direction there is the Meshcherskaya lowland, in the southwest there is the Central Russian Upland, and in the southeast - the Volga.

The satellite map of the Ryazan region shows that there are about 70 rivers, lakes, ponds and swamps in the region.

Important rivers are:

• couple;
• Goose;
• Voronezh;
• Pronya;
• Moksha.

The climate is moderate. On the online map of the Ryazan region with borders, it is noted that part of the territory of the region is occupied by forest-steppe, there are pine, mixed forests, oak groves and steppe areas.

The area of ​​the forest fund exceeds 1052 thousand hectares. More than 40 species of animals and about 120 species of birds live within the boundaries of the subject.

Minerals are mined in the region. There are several large industrial enterprises. Mechanical engineering and power engineering are well developed. More than 320 agricultural enterprises, 2540 peasant farms, over 210 enterprises of the processing and food industries are involved in the agro-industrial complex.

Road communication of the Ryazan region, routes and routes

Highways laid through the Ryazan region:

• Federal M5 "Ural".

  PLANT AND SOIL RESOURCES OF THE RYAZAN REGION

  Moscow - Chelyabinsk;

• P105. Moscow - Kasimov;
• Federal P22 "Caspian". Moscow - Astrakhan.

There are other routes as well. Railway lines pass through the region. One in the direction of the Caucasus, the other - Siberia. There are several single-track roads, more than 50 narrow-gauge railways, three locomotive depots, 40 railway stations, 30 stations.

A branded train runs between the capital of Russia and Ryazan. Length railways exceeds 1500 kilometers. There are two airports on the territory of the region, river transport runs along the Oka, there is a port and marinas.

Districts and settlements of the Ryazan region

On the map of the Ryazan region with districts it is said that the subject consists of 25 municipalities:

• Alexander Nevsky;
• Yermishensky;
• Zakharovsky;
• Kasimovsky;
• Klepikovsky;
• Miloslavsky;
• Mikhailovsky;
• Kadomsky;
• Skopinsky;
• Sarajevo;
• Spassky;
• Ryazhsky;
• And others.

On the lands of the Ryazan region there are 4 urban districts, 29 urban and 249 rural settlements.

More than 530 thousand people live in the capital of the region, which is Ryazan, and over a million Russians live in the region, about 8 thousand Ukrainians, more than 5 thousand Armenians. There are also people of other nationalities.

The climate of the Ryazan region

The climate of the region is temperate continental, with warm summers and moderately cold winters. Average monthly temperature the coldest month is January -11.0°С in the northeast and -10.5°С in the southwest of the region. The average monthly temperature of the warmest month, July, is +18.8°С in the north of the region and +20°С in the south. From north to south, the period of active vegetation increases - from 137 days to 149.

The average duration of the frost-free period is 130-149 days.

Late spring and early autumn frosts are frequent in the region. The Ryazan region is located in a zone of sufficient moisture.

The annual amount of precipitation in the region is up to 500 mm. Rains in the summer are predominantly torrential in nature, sometimes with hail.

Ryazan Oblast

A stable snow cover forms in late November - early December and breaks down in late March - early April. The number of days with snow cover is 135-145 per year. The height of the snow cover by the end of winter reaches 25-38 cm, in some winters - up to 62 cm.

Climatic conditions are favorable for agricultural production. Winter, spring grain, industrial and fodder crops are fully provided with heat and moisture.

The Ryazan region is a land of majestic forests, full-flowing rivers and sun-drenched meadows. The beauty of these expanses has been repeatedly described by various poets and writers.

Ryazan land amazes an outside observer with an abundance of life forms, their diversity and a harmonious ecosystem. Hundreds of species of animals live in these endless expanses, many trees, various herbs and shrubs grow. Rivers and lakes abound with fish, and the dense Ryazan forests have become home to many animals and birds. Let's talk in more detail about the flora and fauna of this amazing region.

The flora of the Ryazan region

The flora of the Ryazan region is interesting and diverse. In summer, abundant vegetation creates a real riot of colors. Slightly less than a third of the region's territory is occupied by different types forests. AT deciduous forests such species of trees as ash, sycamore and holly maples, linden, oak are represented. The undergrowth consists of bird cherry, mountain ash, buckthorn, euonymus and forest honeysuckle. In the grass cover, you can find the usual types of grasses for the central strip: perennial forest herb, bellflower, violet, wild strawberry, yellow zelenchuk, oak mannik, male shield, etc. In coniferous forests, spruce and pine trees predominate, there are various types of shrubs - blueberries, lingonberries, cranberries , lightning blue.

A significant part of the forest cover is made up of birch forests and oak forests. Of the meadow and field plants, the most common are red clover, alfalfa, fescue, timothy grass, meadow geranium, bluebell, brome, etc. In the south-west of the region, vegetation characteristic of the steppe zone is widely represented: feather grass, thyme, couch grass, yarrow, wormwood. In total, at the moment, about 1,300 plant species have been registered in the Ryazan region, of which over 100 are listed in the Red Book of the region.

Fauna of the Ryazan region

The fauna of the Ryazan region is extremely diverse and rich. dense forests and the endless fields became home to many animals and birds. The region is inhabited by bears, wolves, foxes, lynxes, wild boars, hare and hare. Several species of deer have been preserved in the region - noble, spotted and deer. The region is also a habitat for squirrels, hedgehogs, desmans, muskrats, weasels, ermines and many other animals.

But the fauna of the Ryazan region is not only mammals. About eighty species of fish live in the rivers and lakes of the region. The most common are bream, crucian carp, carp, roach, silver bream, ide and rudd, there are pike, pike perch, catfish, tench, blue bream, sabrefish, etc. In addition, the Ryazan region is a habitat for two hundred and ninety species of birds. These include ducks, geese, swans, capercaillie and black grouse, owls, woodcocks, quails, partridges, etc.

Synanthropic birds (living in close proximity to humans) are widespread - rooks, pigeons, crows, sparrows, magpies, jackdaws, swifts. It should be noted that the wildlife of the Ryazan region needs protection and protection. At the moment, 281 species of animals are listed in the Red Book of the region.

The climate of the Ryazan region

Each of the seasons in the Ryazan region is beautiful in its own way. In spring, snow melts and rivers open up. In mid-April, the Oka floods. Summer is the warmest time of the year, in the south of the region the temperature reaches forty-one degrees Celsius. Thunderstorms are typical for summer, hurricanes often pass. Autumn is divided into two periods - warm and cold. Until early October, the weather is usually dry and warm, even hot, followed by short periods of rain. In October and November the weather is cloudy, cold and rainy. Winters in the Ryazan region are usually long and cold, but now they are getting warmer. And this cycle repeats every year.

PLEASE HELP answer the question. "Write down basic information about the soils of the Ryazan Territory."

Answers:

The soils of Ryazan, as well as the entire region, were formed mainly on Quaternary sediments. Swampy soils prevail near Solotcha - their formation was facilitated by excessive moisture and a weak slope of the relief. Organic matter in the form of peat accumulates here. One of the largest peat mining in the region - the Solotchinsk peat mining enterprise with its own narrow-gauge railway - is located there. On the coast of the Oka there is a narrow strip of podzolic and sod-podzolic soils - they have high water permeability, so that the vegetation on them does not suffer from excess moisture. floodplains are floodplain soils, which are the basis of the fund of natural fodder lands. These soils are rich in silt, thanks to which the floodplains are perfect place for fodder pastures and lands