Aquifer complex and horizon. Aquiferous Gzhel-Assel carbonate complex
The underground aquifer complex of the Moscow region is represented by five horizons of Paleozoic Carboniferous deposits that are of interest for water supply: the aquifer of the Oka and Serpukhov suites of the Lower Carboniferous, the Kashirsky and Myachkovsko-Podolsky horizons of the Middle Carboniferous, the Kasimovsky and Gzhel horizons of the Upper Carboniferous.
The aquifers of the Tula, coal-bearing and Upinsk strata of the Lower Carboniferous, located by the Podoksky limestones, as well as the Upper Devonian horizons in the territory of the Moscow Region, are characterized by low water abundance and increased water salinity.
These five aquifers used for water supply are separated from each other by significant layers of clay, which make it difficult to connect the waters of individual horizons. Each horizon has its own conditions for the formation of waters and reacts differently to local conditions.
The aquifer of the Oka and Serpukhov formations of the Lower Carboniferous with a thickness of 60–70 m is represented by limestones and dolomites. In the south of the region in the lower part of the river valley. The Oka aquifer has a very large water abundance. The specific flow rates of wells often exceed 50 m3/hour, while in other areas of the region, the specific flow rates of wells of this horizon rarely reach 25 m3/hour.
The Kashirsky aquifer of the Middle Carboniferous, 40–60 m thick, is represented by limestones and dolomites with interlayers of calcareous clays, characterized by low abundance.
The exception is the territory of the city of Kolomna, where, due to specific hydrogeological conditions, significant specific debits of water intake tubular wells are observed.
The Moscow-Podolsky aquifer of the Upper Carboniferous, about 45 m thick, is represented by dolomites and limestones with numerous layers of calcareous clays. In the zone adjacent to the southern boundary of its distribution, there are areas where it consists mainly of clays, being practically anhydrous. In places where the aquifer is covered with Gzhel deposits, the specific flow rates of tubular wells do not exceed 15 m3 / h, and where there are no Gzhel deposits and the aquifer is located at a shallow depth, specific flow rates reach 60 m3 / h (for example, the city of Shchelkovo).
The Gzhel aquifer of the Upper Carboniferous, about 75 m thick, consists of dolomites and limestones with very rare and thin layers of marl and limestone clay. The horizon has a well-developed fracturing and a large water abundance. Specific debits of tubular wells sometimes exceed 60 m3/hour. Within the Klinsko-Dmitrovskaya ridge, specific flow rates decrease to 10 - 20 m3 / hour.
In the northern, eastern, and most of the central part of the region, the Carboniferous deposits are covered by a layer of Upper Jurassic clays 10 to 60 m thick (the area of the city of Istra). The Upper Jurassic clays serve as a waterproof roof for the Carboniferous waters and create pressure for these waters. In a significant part of the distribution of Upper Jurassic clays, they are covered by sands and clays of the Volgian stage of the Upper Jurassic and Lower Cretaceous up to 30 m thick (110 m within the Klin–Dmitrovskaya ridge).
The Lower and Upper Cretaceous sands of the Volgian stage contain huge reserves of groundwater. However, it is extremely difficult to use these waters for centralized water supply, because the sands are very fine-grained and clayey with poor water loss. The issue of using these waters is very relevant. Especially in the northern regions of the region.
The quality of chalk waters is generally satisfactory. They belong to the hydrocarbonate type with a dense residue of 200–300 mg/l, but often contain large amounts of iron (up to 10 mg/l). In the opoka-like sandstones of the Upper Cretaceous and tripoli there are waters that feed springs and wells in the Zagorsk region. Such waters are low-mineralized, hydrocarbonate type with a dense residue in the range of 150-200 mg/l.
Analyzing the aquifer complex of the Moscow region, it can be concluded that the conditions for the capture of groundwater by coal deposits are extremely diverse. Therefore, tubewell depths, filter designs and equipment vary widely.
According to the conditions of occurrence of aquifers, according to the quality of water, the territory of the region can be divided into seven hydrogeological regions.
1. The southern region has tubular wells fed by the waters of the Serpukhov and Oka formations of the Lower Carboniferous, 40–120 m deep with a specific debit of up to 15 m3/hour. Static water levels in wells are located at a depth of 10 to 70 m. Dense water residues do not exceed 600 mg/l, fluorine content is about 1 mg/l.
2. Water intake wells of the Southwestern region are fed by the waters of the Kashirsky aquifer of the Middle Carboniferous and the Serpukhov and Okskaya suites of the Lower Carboniferous, the Kashirsky aquifer is characterized, as a rule, by a small water abundance. Specific well flow rates are 2 - 3 m3 / hour. In the upper layers of the horizon, the dense residue of water does not exceed 300 mg / l, and the fluorine content is about 0.5 mg / l. In the lower layers, a dense residue is up to 500 mg / l. and fluorine up to 3 mg / l.
The aquifer of the Lower Carboniferous is more watery. Specific debits here reach 5 - 7 m3 / hour. It is characteristic that the mineralization of the waters of the Lower Carboniferous decreases from the southeast to the northwest. In the south-eastern parts of the region, the dense residue reaches 900 mg / l, the fluorine content is 2.5 - 3 mg / l, the sulfate content of the waters increases significantly. In the northwestern parts of the region, dense sediment does not exceed 400 mg/l, and the amount of fluorine in water is up to 1 mg/l.
3. The large central region occupies a significant part of the region's territory. The tubular wells of the area are fed mainly by the waters of the Myachkovsko-Podolsky aquifer, less often - the Kashirsky aquifer of the Middle Carboniferous and the Lower Carboniferous horizons. In this area, wells should be laid on the Myachkovsko-Podolsky horizon, which is characterized by a greater water abundance than the underlying horizons. The specific flow rate of wells of the recommended horizon reaches 15 m3 / hour.
The waters of the Myachkovsko-Podolsky aquifer are characterized by a dense residue of up to 500 mg/hour, a fluorine content usually up to 1 mg/l, and belong to the hydrocarbonate or hydrocarbonate-sulfate type. The areas of the territory confined to the areas of occurrence of Mesozoic phosphorite deposits are characterized by waters with a fluorine content of up to 5 mg / l.
4. In the small central region, tubular wells are fed by the waters of the Kasimovsky horizon of the Upper Carboniferous and the Myachkovsko-Podolsky horizon of the Middle Carboniferous. The Kasimovsky horizon at the southern border of the region has a thickness of 10-20 m, to the north its thickness increases to 45 m. The water abundance of the horizon increases from south to north, where the specific flow rate of wells reaches 20 m3 / hour. The waters of the horizon have a weak mineralization, the dense residue is not higher than 300 mg/l, the amount of fluorine is up to 0.6 mg l.
Myachkovsko - Podolsky horizon is characterized by low water abundance, specific flow rates reach 10 m3 / hour. The waters are characterized by significant sulfate content and mineralization. The dense residue reaches up to 1650 mg/l, the fluorine content is 5.5 mg/l.
1The hydrogeological conditions and problems of the territory of the Perm Territory are characterized: the shortage of fresh groundwater, the depletion of their reserves, and environmental problems. The materials of hydrogeological mapping and research are summarized. Hydrogeological stratification and zoning of the territory have been completed. A modern hydrogeological map has been built. 25 main aquifers and horizons of the zone of active water exchange, which have different practical significance for water supply, have been identified and characterized. Their characteristics are given in terms of water abundance of sediments, chemical composition and quality of groundwater. There is a connection between the water content of sediments and geodynamic active zones and tectonic structures. The main prospects for the search for groundwater to provide the population with fresh water are associated with water-abundant zones due to geodynamic factors. It is noted that the identification and mapping of water-abundant zones will be facilitated by the integration of standard hydrogeological methods with remote methods and geoinformation technologies.
hydrogeology
fresh groundwater
aquifers and horizons
watery zones
hydrogeological map
Perm region.
2. Atlas of the Perm Territory / edited by A.M. Tartakovsky. - Yekaterinburg: Ural worker, 2012. - 124 p.: ill.
3. Budanov N.D. Hydrogeology of the Urals. – M.: Nauka, 1964. – 303 p.
4. Hydrogeology of the USSR. T. XIV. Ural / ed. I.K. Zaitsev. – M.: Nedra, 1972. – 648 p.
5. Konoplev A.V., Kopylov I.S., Pyankov S.V., Naumov V.A., Iblaminov R.G. Development of principles and creation of a unified geoinformation system of the geological environment of Perm (engineering geology and geoecology) // Modern problems of science and education. - 2012. - No. 6. - URL: http://www.science-education.ru/106-7893.
6. Kopylov I.S. Geoecological studies of oil and gas regions: Dissertation for the degree of candidate of geological and mineralogical sciences. - Perm, 2002. - S. 307.
7. Kopylov I.S. Drawing up a hydrogeological map of the Perm region at a scale of 1:500,000 / Inform. map. – M.: VGF, 2002.
8. Kopylov I.S. Compilation (updating) of serial legends of state hydrogeological maps at a scale of 1:200,000 (Perm series) / Inform. map. – M.: VGF, 2003.
9. Kopylov I.S. The concept and methodology of geoecological research and mapping of platform regions // Prospects of Science. - 2011. - No. 23. - P. 126-129.
10. Kopylov I.S. Principles and criteria for an integral assessment of the geoecological state of natural and urbanized territories // Modern problems of science and education. - 2011. - No. 6. - URL: www.science-education.ru/100-5214.
11. Kopylov I.S. Hydrogeochemical anomalous zones of the Western Urals and Cis-Urals // Geology and minerals of the Western Urals. - Perm, 2012. - S. 145-149.
12. Kopylov I.S. Lineament-geodynamic analysis of the Permian Urals and the Urals // Modern problems of science and education. - 2012. - No. 6. - URL: www.science-education.ru/106-7570.
13. Kopylov I.S. Anomalies of heavy metals in soils and snow cover of the city of Perm as manifestations of factors of geodynamics and technogenesis // Fundamental research. - 2013. - No. 1-2. - S. 335-339.
14. Kopylov I.S. Compilation of the geological atlas of the Perm region // Problems of mineralogy, petrography and metallogeny. Scientific readings in memory of P.N. Chirvinsky. - 2013. - No. 16. - P. 356-362.
15. Kopylov I.S. Patterns of formation of soil landscapes in the Urals, their geochemical features and anomalies // Modern problems of science and education. – 2013. – no. 4. - URL: www.science-education.ru /110-9777.
16. Kopylov I.S. Results and prospects of regional hydrogeological work in the Perm region and their geoinformation support // Geoinformation support for the spatial development of the Perm region: Sat. scientific tr. Perm. state nat. research un-t. - Perm. - 2013. - Issue. 6 - S. 34-40.
17. Kopylov I.S. Search and mapping of water-abundant zones during hydrogeological work using lineament-geodynamic analysis // Polythematic network electronic scientific journal of the Kuban State Agrarian University. - 2013. - No. 93. - P. 468-484.
18. Kopylov I.S. Geodynamic active zones of the Urals, their manifestation in geophysical, geochemical, hydrogeological fields // Successes of modern natural sciences. - 2014. - No. 4. - S. 69-74.
19. Kopylov I.S. Geoecological role of geodynamic active zones // International Journal of Applied and Fundamental Research. - 2014. - No. 7. - S. 67-71.
20. Kopylov I.S., Konoplev A.V. Geological structure and subsoil resources in the atlas of the Perm Territory // Bulletin of the Perm University. Geology. - 2013. - No. 3 (20). - P. 5-30.
21. Kopylov I.S., Konoplev A.V., Iblaminov R.G., Osovetsky B.M. Regional factors of formation of engineering-geological conditions of the territory of the Perm region // Polythematic network electronic scientific journal of the Kuban State Agrarian University. - 2012. - No. 84. - P. 102-112.
22. Kopylov I.S., Likutov E.Yu. Structural-geomorphological, hydrogeological and geochemical analysis for the study and evaluation of geodynamic activity // Fundamental research. - 2012. - No. 9-3. - S. 602-606.
23. Methodological bases of hydrogeological zoning of the territory of the USSR / L.A. Ostrovsky, B.E. Antypko, T.A. Konyukhov. – M.: Nedra. - 1990. - 240 p.
24. Mineral resources of the Perm region: encyclopedia / ch. ed. A.I. Kudryashov. - Perm: Book Square, 2006. - 464 p.
25. Mikhailov G.K., Oborin A.A. Underground storeroom of fresh waters of the Sylvensky Ridge. - Perm: Publishing House of Perm University, 2006. - 154 p.: ill.
26. Principles of hydrogeological stratification and zoning of the territory of Russia (methodological letter) / M.S. Golitsyn, M.V. Kochetkov, L.V. Leonenko and others - M .: Ministry of Natural Resources of the Russian Federation, 1998. - 21 p.
27. Sherstnev V.A. watery zones. - Perm: PGU, 2002. - 132 p.
28. Shimanovsky L.A., Shimanovskaya I.A. Fresh underground waters of the Perm region. - Perm: Prince. publishing house, 1973. - 195 p.
29. Likutov E.Yu., Kopylov I.S. Complex of methods for studying and estimation of geodynamic activity // Tyumen State University Herald. - 2013. - No. 4. - S. 101-106.
Introduction
The territory of the Perm Kama region - the Perm Territory is a large region with an area of 160.6 thousand km2, with a population of more than 3 million people, characterized by a wide variety of natural conditions and resources, complex hydrogeological and hydrogeoecological conditions. 126 deposits of fresh groundwater have been explored in the region, with a total operational reserves of 1125 thousand m3/day, of which (according to the GIDEK - 2010) 67 deposits are being exploited with a total water withdrawal of 226 thousand m3/day. The current demand for utility and drinking water is met by groundwater only by 15%. The most important problems of the territory are the lack of water supply sources for many settlements, the shortage of fresh groundwater, the depletion of its reserves, environmental problems associated with widespread water pollution, and the lack of modern regional hydrogeological information.
Materials and methods of researchBased on the materials of hydrogeological mapping and research (L.I. Shimanovsky, G.K. Mikhailov, E.A. Bobrov, A.M. Oskotsky, V.I. Moshkovsky, E.A. Ikonnikov, V.A. Popovtsev, S. V. Zayakin, A. G. Melekhov, I. M. Sinitsin, A. V. Revin, V. P. Kulikov, P. P. Vedernikov, V. M. Baldin, I. S. Kopylov, etc.) systematization, data analysis; hydrogeological stratification and zoning were carried out. In accordance with c, the territory is located at the junction and within four first-order groundwater basins: I - the eastern margin of the East Russian complex formation water basin, II - the Cis-Ural complex formation water basin, III - the Timan-Pechora complex formation water basin, IV - Bolsheuralsky complex basin of crust-block waters, divided into basins (blocks) of lower orders. In the hydrogeological section, the following are distinguished: aquifers or impervious floors > aquifers (AC) > aquifers (AH) or aquifers (AZ). Their names are given in accordance with the principles of hydrogeological stratification and the updated serial legend of state hydrogeological maps at a scale of 1:200,000 for the Perm series of sheets with clarification. Their distribution, taking into account modern geological and hydrogeological foundations, is shown on the hydrogeological map (Fig. 1).
Rice. 1. The main aquifers and horizons of the Perm Territory
Research results and discussionIn accordance with the principles outlined below, a brief description of the main hydrogeological units of practical importance is given below.
The aquifer complex of Cenozoic formations includes a number of aquifers and impermeable horizons of eluvial, deluvial, alluvial, lacustrine, marsh, glacial, fluvioglacial, polygenetic formations, as well as relatively impervious horizons of Neogene and Paleogene formations. All of them can be important for water supply, but their sources are not constant over time, and their waters are often substandard in quality.
The aquifer of Quaternary alluvial formations is distributed along the river valleys, especially - Kama, Chusovaya, Sylva, Obva, Inva, Chermoz, etc. It combines deposits of low accumulative terraces (floodplain, high floodplain, terraces I and II above floodplain) and upper basement and erosion-accumulative terraces (III and IV above-floodplain terraces). The thickness of alluvium is in the range of 5-15 m, reaching 40-50 m in the valley of the river. Kama. The upper part of the section is dominated by clays, loams and sandy loams, while the lower part is dominated by sands, gravel, and pebbles. Filtration coefficients have values within the first ten m/day.
Alluvial deposits contain free-flowing groundwater, the depths of which are determined by the surface of the terraces above the water line and range from 0 to 13 m. The flow rates of springs usually do not exceed 0.2-0.3 l / s (up to 8 l / s), wells - 0.3-2 l / s at depressions of 1-7 m. The composition of the waters is mainly HCO 3 -Ca (Mg-Ca, Na-Ca) with a mineralization of 0.1-3 g / dm 3, an average of 0.2 g / dm 3 . Groundwater is fed from the alluvium of small rivers due to atmospheric precipitation and inflow from bedrock deposits. The waters of the horizon are used for water supply by water intakes: Ust-Kachka, Konets-Bor, Okhansk, Kama. Due to the low hypsometric position, in addition to swamp pollution (Na, Cl, SO 4 , NO 3), there is a high probability of sewage getting into it.
The aquifer of the Dnieper fluvioglacial formations is distributed in the basin of the rivers Veslyana, Timshora, Kama, Kosa, Urolka. Associated with quartz fine-grained sands with rare pebbles. The thickness of the horizon is from 0.5 to 40 m. Water HCO 3 -Ca (Na-Ca) composition with a mineralization of 0.1-0.2 g/dm 3 Possibly swamp contamination.
Relatively water-resistant horizons of Neogene and Paleogene formations are distributed in the southern part of the territory in the overdeepened parts of the river valleys of the river basin. Buoy. Represented by clays, loams, with interlayers and lenses of siltstones, sands and pebbles. The thickness of the deposits of horizons is up to 20-25 m. According to the chemical composition of water, HCO 3 -Ca (Mg-Ca, Ca-Mg) composition with a mineralization of 0.3-0.4 g / dm 3.
The aquifer complex of Mesozoic formations is developed in the northwestern part of the territory in the basins of the Veslyana, Kosa, and Inva rivers. The aquifer of the Middle Jurassic is composed of sands with lenses of gravel and pebbles, sandstones and clays with interlayers of siltstones up to 25 m thick or more. The relatively water-resistant horizon of the Lower Triassic is composed of clayey rocks with interlayers of sandstones and siltstones up to 21 m thick. (Na) with mineralization up to 0.5 g/dm 3 . The water content is low, the flow rate of springs does not exceed 0.5 l/s. Water supply of small enterprises and farms is possible.
The aquifer complex of the Middle-Upper Permian includes the aquifers of the Severodvinsk, Urzhum and Kazan deposits. The aquifer of the Severodvinsk deposits of the Upper Permian is distributed in the western part of the territory, a strip with a width of up to 30 km of variegated sandy-argillaceous deposits, sporadically flooded. The flow rates of the springs are up to 1 l / s, the composition of the waters is HCO 3 -Ca-Na, with a mineralization of up to 0.5 g / dm 3.
The aquifer of the Urzhum deposits of the middle Permian is widespread in the western part of the Perm Kama region, with a width of up to 120 km, a thickness of up to 200-260 m. It is represented by a red-colored sandy-clayey stratum with a predominantly sandstone (> 50%) type of section with subordinate limestones, conglomerates, mudstones . The thickness of water-saturated layers is 1-5 m, rarely reaches 10-15 m or more. The horizon is extremely heterogeneous in terms of filtration properties. The most permeable layers lie above the local erosion incision, where spring runoff is formed, which is often characterized by large springs (5-20 l/s and more). The water abundance of sediments is determined by geodynamic and structural-tectonic conditions, with which significant water-abundant zones are associated. Almost all of them are confined to the intersections of large lineaments identified with tectonic faults and causing geodynamic active zones. -Ca, Ca-Mg-Na), with a mineralization of 0.1-0.5 g / dm 3. Sometimes there are inflows of mineralized waters. The underground waters of the horizon are widely used for water supply of medium-sized settlements.
The aquifer of the Kazan deposits is confined to the Belebey suite of the Kazan stage of the Middle Permian. Distributed east of the Urzhum horizon, in a strip up to 30 km wide. The total thickness is 100-275 m. The deposits are represented by sandstones, conglomerates, siltstones, mudstones, with lenses of limestones, marls; but down to a depth of 100-150 m, the clay type section prevails (clay>50%). Aquifers are siltstone layers with interlayers of sandstones. The thickness of water-saturated layers is usually 1-5 m, rarely 5-10 m. Sporadic distribution of groundwater with separate water-abundant zones is characteristic. The largest water-abundant zones (flow rates of springs from 5-20 l / s to 50 l / s) are established at the junction of the Perm arch and the Visim depression, characterized by increased geodynamic activity and rock fracturing. Groundwater HCO 3 (Ca-Mg and Ca-Na) composition and mineralization 0.2-0.4 g/dm 3 . Below the local erosion incision (up to a depth of 100 m), waters of mixed composition with a salinity of 10-15 g/l were established (in the sections of the rivers Inva, Chermoza, Nerdva). Groundwater can be used by the operation of single wells with a capacity of 50-100 m 3 /day.
The aquifer complex of deposits of the Ufimian stage includes the aquifers of the Sheshma and Slickam deposits of the Ufimian stage of the Lower Permian. The aquifer of the Sheshma deposits (P 1 ss) is confined to the Sheshma horizon of the upper substage of the Ufimian stage. It comes to the surface in a strip of meridional strike up to 60 km wide, from 20-30 to 320-410 m thick, in the valley parts of the Kama, Babka, Tulva rivers, as well as on the watersheds of the Kama and Vishera, Buya and Bystry Tanyp rivers. Composed of interbedded sandstones, siltstones, mudstones, with lenses of limestones, marls; gypsum is typical. Aquifers are fissured interlayers of rocks, 1-3 m thick. Flow rates of springs are from 0.1-0.5 to 5-10 l/s. The composition of the waters above the erosion incision is predominantly HCO 3 -Ca (Mg, Na), with a mineralization of 0.2-0.5 g / dm 3, below the erosion incision SO 4 (HCO 3 -SO 4, CI-SO 4) -Ca prevail (Na, Mg) water with salinity from 1.5 to 14 g/dm 3 . The waters of the horizon are used by the population of Perm for water supply by single wells, wells and spring capturing, rarely - group water intakes. Within water-abundant zones, it is possible to construct water intakes with a debit of 1000-2000 m 3 /day.
The aquifer of the Solikamsk deposits is confined to the Lower Ufimsky (Solikamsk) horizon. It comes to the surface in the form of a strip of meridional strike up to 30 km wide in the Cis-Ural basin and a narrow intermittent strip within the Tulva group of basins, sometimes overlapping with Sheshma deposits, and, plunging westward under the Sheshma horizon to a depth of more than 600 m. The thickness of the horizon reaches 300 m and more. Represented by alternation of limestones, marls, mudstones, sandstones, gypsums. The composition of waters is predominantly HCO 3 -Mg-Ca with mineralization up to 0.5 g / l, in areas with industrial and domestic pollution and inflow of water from underlying sediments up to 1.0 g / dm 3, the composition changes to HCO 3 -CI and HCO 3 -SO 4 . In the lower zone of supra-salt waters at a depth of 300-350 m, CI-Na brines with mineralization up to 155-317 g/dm 3 are developed. It is of great practical importance for water supply, however, due to poor protection, groundwater is prone to pollution.
The aquifer complex of deposits of the Kungurian stage is represented by several aquifers and aquifers. The first Kungurian (Irenian) VG is confined to the western flank of the Permian-Bashkir arch and the wings of the Xenophon-Kolvinsky swell and the Kolvinskaya saddle. It is composed of alternating gypsum-anhydrite and limestone-dolomite packs, which are water-bearing only in the place where they come to the surface; with immersion under younger rocks, the complex becomes an aquiclude (water-resistant Irensky horizon). The upper part of the section is subject to intensive karsting. The composition of the waters is higher than the erosion incision SO 4 -HCO 3 -Ca, with mineralization up to 3 g/dm 3 . At a depth of about 100 m, mineralization increases to 4.1-9.3 g / dm 3, the composition of water is SO 4 -Ca-Na, CI-Na. The groundwater of the aquifer is practically unprotected and can be subject to pollution. The second Kungurian VG is distributed on the surface in the eastern parts of the Timan-Pechora and Cis-Ural complex basins. The lithology is very diverse. Based on the facies heterogeneity and inconsistency of water-bearing rocks, it is characterized by complex hydrogeological conditions, a diverse chemical composition from HCO 3 to HCO 3 -SO 4 and SO 4 -CI- with a mineralization of 0.1-3.0 g / dm 3 and more.
The aquifer complex of the Assel-Artinsk deposits occupies a discontinuous strip along the eastern side of the Cis-Ural trough. It is composed of sandstones, mudstones, with interlayers and lenses of conglomerates, limestones, marls, up to 330 m thick. Characterized by the complete absence of gypsum. According to the composition of the water of the complex, mainly HCO 3 -Ca, with mineralization up to 0.1-0.8 g/dm 3 . The aquifer systems of the Lower Permian in the Kungur and Artinsk deposits are of particular interest for water supply, especially on the Ufimsky plateau, where in linear fractured zones the flow rate of springs reaches 1000 l/s, and the specific flow rate of wells is 135 l/s.
The aquifer complex of the Middle and Upper Carboniferous is developed within the western slope of the Urals in areas of predominantly submeridional strike and the crest of the Ksenofontovsky-Kolvinsky swell. It is composed of limestones, dolomites with interlayers of sandstones, mudstones, marls up to 200 m thick. Fissure-karst waters are developed mainly HCO 3 -Mg-Ca, with a mineralization of 0.1-0.7 g/dm 3 . It is used for centralized water supply in the city of Kizel. Prospects are associated with linear water-abundant zones, where flow rates of springs reach 100-400 l/s.
The following aquifers are developed within the Bolsheuralsk complex basin of crust-block waters: VC of the Lower and Middle Carboniferous, VC of carbonate deposits of the Middle Devonian - Lower Carboniferous, VC of terrigenous deposits of the Devonian, VC of carbonate deposits of the Silurian - Lower Devonian, VC of carbonate deposits of the Middle - Upper Ordovician, VC of terrigenous deposits of the Lower - Middle Ordovician, VC of terrigenous deposits of the Upper Vendian, VC of terrigenous and metamorphic deposits of the Lower Vendian, aquiferous zone of fissuring of metamorphic rocks of the Riphean, aquiferous zone of fracturing of igneous rocks. They contain crust-block waters confined to the fractured zone of the weathering crust and local tectonic fissures. The first two VCs contain fissure-karst waters. Within the development of tectonic fissures, they are more watery (the flow rate of springs is up to 1-3 l/s). The composition of water is predominantly HCO 3 -Mg-Ca, with a mineralization of 0.01 - 0.2, rarely up to 0.9 g / dm 3. Groundwater is poorly studied, according to data it may be of interest for local water supply.
Conclusion
On the territory of the Perm Territory, 25 main aquifers and horizons have been identified. The main prospects for the search for groundwater to provide the population with fresh water are associated with water-abundant zones located unevenly in area, mainly due to the action of geodynamic and structural-tectonic factors. Identification and mapping of water-abundant zones is most effectively carried out by combining standard hydrogeological methods with remote methods and the use of GIS technologies based on the creation of databases, automated methods for deciphering and processing data.
Bibliographic link
Kopylov I.S. MAIN WATER-BEARING COMPLEXES OF THE PERM PRIKAMIE AND THE PROSPECTS OF THEIR USE FOR WATER SUPPLY // Successes of modern natural science. - 2014. - No. 9-2. - P. 105-110;URL: http://natural-sciences.ru/ru/article/view?id=34364 (date of access: 07/19/2019). We bring to your attention the journals published by the publishing house "Academy of Natural History"
Aquifer - layers, rock, in which groundwater occurs. Ground and underground waters are divided into three main categories of aquifers: perched water, interstratal and artesian waters.
The uppermost groundwater horizon, or otherwise the “perch water”, is the most accessible for exploitation, since it is closer to the surface than the rest. However, its availability is also associated with certain disadvantages: perched water tends to change its depth depending on the time of year, average daily temperature and natural precipitation.
Also an important negative factor is the problem of groundwater pollution with chemical fertilizers, insecticides used in adjacent areas, emissions and effluents from industries, vehicles, etc. that enter the soil.
Less accessible are interstratal groundwater located under the so-called "impermeability", which is a layer of clay soil that changes its thickness depending on the landscape. Such waters have a much more stable chemical composition and greater constancy, almost unchanged water abundance throughout the year.
It should be taken into account that interstratal waters can be pressurized, i.e. freely flowing after opening with a pit or drilling to the surface, as well as free-flowing, and remain in the zone of the sandy aquifer, not rising above the clay aquiclude.
Artesian waters, also called spring waters, are self-flowing, having a local outflow.
The construction of a well for watering plants and technical needs does not require digging a well to the depth of occurrence, interstratal groundwater, as in cases where high-quality drinking water is required. To do this, it is enough to equip a well of lesser depth in the lowest part of the site using the "top water".
Digging a well to provide high-quality drinking water and an autonomous water supply system for housing requires the passage of a "water seal" made of clay using drilling or manual labor.
The search for suitable groundwater for use as the main or alternative autonomous source of water supply is carried out using engineering methods of drilling pits and wells, or by such non-traditional dowsing methods of dowsing, using all kinds of contour frames that respond to fluctuations in the human biofield. The noise "background" from high groundwater, however, does not always make it possible to determine with unmistakable accuracy the places where water occurs between the layers.
Water flows through permeable rock layers, from higher absolute levels to lower ones. The voids, mines, cavities and wells encountered on the way of movement, the water fills up to the same level at which it itself is located.
For the same reason, the maximum depth of wells in areas located in a river valley, on a terrace or in a floodplain is limited by the excess of the location of the well above the level of the river, and for wells located directly on the bank, by the height of the bank itself.
The depth of water in the well cannot be greater than the depth of the water edge in the river, for the reason that the aquifer is hydraulically connected to the river, and the water inflow directly depends on the filtration coefficient in the bottom river part.
An aquifer (aquifer) is a layer or several layers of permeable rocks, the cracks, pores and other voids of which are filled with groundwater.
The degree of permeability of rocks, i.e. the ability of rocks to pass water depends on the size and number of interconnected pores and cracks, as well as on the sorting of rock grains. Highly permeable rocks include pebbles, gravel, coarse-grained sands, intensely karst and fractured rocks. Practically impermeable (impervious) rocks are clays, dense loams, non-fractured crystalline, metamorphic and dense sedimentary rocks.
The permeability of rocks can be determined by the filtration rate, which is equal to the amount of water flowing through a unit area of the cross-sectional area of the filter rock. This dependence is expressed by the Darcy formula:
V = k*I,
where V is the filtration rate,
k - filtration coefficient,
I - pressure gradient equal to the ratio of the pressure drop h to the length of the filtration path
The filtration coefficient has the dimension of speed (cm/sec, m/day). Thus, the filtration rate at a pressure gradient equal to unity is identical to the filtration coefficient.
Due to the fact that water in rocks can move under the influence of various factors (hydraulic pressure, gravity, capillary, adsorption, capillary-osmotic forces, temperature gradient, etc.), the quantitative characteristic of water permeability of rocks can also be expressed by water conductivity and piezoconductivity. In hydrogeological studies and calculations, the water conductivity coefficient (the product of the filtration coefficient and the thickness of the aquifer) is an indicator of the filtration capacity of the rock.
Depending on the geological structure, water-bearing rocks in terms of filtration can be isotropic, when the water conductivity is the same in any direction, and anisotropic, characterized by a regular change in water permeability in different directions.
The study of the permeability of rocks is necessary in the search and exploration of groundwater for the purposes of water supply, in the construction of hydraulic structures, the operation of various types of groundwater, in the calculation of permissible drops in the water level and the radius of influence of water wells, in the design and implementation of drainage and irrigation measures.
An aquifer complex is a set of aquifers or zones confined to a thickness of a certain age. It is usually characterized by a regular change in the chemical composition of groundwater along the strike and dip of the complex and the heterogeneity of the filtration properties of rocks.
An aquifer is usually distinguished when it is not possible to delineate well-aged aquifers (poor hydrogeological knowledge, rapid change in facies-lithological composition, complex tectonic structure, etc.), for example, when exploring coal deposits characterized by facies-lithological variability of rocks, for small-scale or overview description of the area. The presence of hydraulic connections within the aquifer complex complicates the drainage of aquifers and increases the duration of drainage work in mines and quarries.
The main source of water supply for country houses in the Moscow region are aquifers of Paleozoic Carboniferous deposits.
Let's list them:
- Gzhel-Asselsky and Kasimovsky aquifers of the Upper Carboniferous,
- Podolsko-Myachkovsky and Kashirsky horizons of the Middle Carboniferous,
- Protvinsky and Aleksinsky-Tarussky horizons of the Lower Carboniferous.
The listed horizons are separated from each other by fairly consistent interlayers of clays, so they have practically no connection with each other. Each horizon has its own characteristics of water abundance, head pressure and chemical composition of groundwater.
According to these characteristics, the Moscow region can be divided into six hydrogeological regions.
Aquiferous Gzhel-Assel carbonate complex
It is the main source of water supply in Taldomsky, Dmitrovsky, Sergiev-Posadsky, Pushkinsky, Shchelkovsky, Noginsky, Pavlovo-Posadsky, the northern part of the Orekhovo-Zuevsky and Shatursky administrative districts.
Depth of occurrence of water-bearing rocks: from 2 to 190 m. The horizon is characterized by a very high, albeit heterogeneous, water abundance. Specific debits of wells vary from 3 to 50 m3/hour.
The waters are fresh, with a standard content of impurities. Sometimes there is an increased content of iron and fluorine.
Water-bearing Kasimov carbonate complex
Klinsky, Solnechnogorsky, Mytishchi, Sergiev-Posadsky, Pushkinsky, Schelkovsky, Orekhovo-Zuevsky, Noginsky, Pavlovo-Posadsky, Ramensky, Shatursky and Egoryevsky districts take water from this aquifer.
The water content of the Kasimovsky horizon, as well as that of the Gzhel-Assel horizon, is very high, but heterogeneous, well flow rates vary from 3 to 50 m3/hour. The highest water abundance is observed in the river valleys.
The chemical composition of the water is fresh, the amount of mineral impurities is 0.1-0.6 g/liter. In some wells, there is an increased content of iron and fluorine.
Aquifer Podilsko-Myachkovskiy carbonate complex
This aquifer is spread over almost the entire territory of the Moscow region, with the exception of the southwestern part. It is the main source of household and drinking water supply in Volokolamsk, Shakhovsky, Istra, Ruzsky, Mozhaysky, Odintsovsky, Naro-Fominsky, Podolsky, Domodedovsky, Voskresensky, Kolomensky, Chekhov administrative districts.
The depth of the roof of the Podolsk-Myachkovsky aquifer starts from 10-20 m in the valleys of the Ruza, Moscow, Pakhra and Oka rivers (in some places it even comes to the surface) and increases in the northeast direction, reaching 450 m. The water pressure in the wells ranges from 20 to 120m. The debit of wells for water drilled on this aquifer can reach 15 m3/hour.
Water mineralization increases to the northeast of the Dmitrov-Noginsk-Shatura line and reaches 10 mg/liter, with an increased content of fluorine (up to 6 mg/liter) and iron (up to 2-3, sometimes 7-10 mg/liter). Therefore, if you live in these areas, you will have to think about purchasing a quality water treatment system.
Aquiferous Kashirsky carbonate complex
The Kashirsky aquifer system is distributed throughout the Moscow region and is eroded in the south. The water-bearing rocks are fractured limestones and dolomites.
The depth of their occurrence varies from 10–20 m in river valleys to 30–40 m in watersheds. The Kashirsky horizon is mainly confined. The magnitude of the pressure increases as the horizon sinks in the northeast direction. The specific debit of wells drilled to this horizon is usually small: 2-3 m3/hour.
Mineralization of water reaches 1.0 mg/liter with a predominance of sulfates. The Kashirsky water-bearing complex is mainly operated in the southern and southwestern parts of the Moscow region.
Aquifer Protvinsky carbonate complex
The water-bearing rocks are fractured, often karst limestones. Gypsum dolomites appear in the northeastern regions, which affects the chemical composition of the water.
Water levels in wells for this aquifer range from 9 m (near Mozhaisk) to 89 m (near Podolsk), and to the northeast of Moscow they increase to 110-150 m. The flow rate of wells is 3-5 m3/hour.
The water in the Protvinsky horizon is hard (up to 15-20 m. mol/liter), with a high content of iron (2-3 mg/liter) and fluorine (up to 5 mg/liter).
Aquifer Aleksinsko-Tarussky carbonate complex
The depth of occurrence of the complex varies from a few meters in the valleys to 110 m on the watersheds and increases in the northeast direction, reaching 350-400 m in the area of Shatura and Dmitrov. Water levels in artesian wells vary from 0 to 60 m, decreasing towards the Volga and Oka valleys.
The territory under consideration belongs to the northern part of the Volga-Sura artesian basin.
The depth of the study of the section is mainly limited by the zone of active water exchange or the zone of fresh water. In this part of the section, taking into account the geological structure, lithofacies composition, the permeability of the rocks that make up them, and finally, the conditions of occurrence of water-bearing rocks and the nature of the relationship associated with them, PVs, a number of hydrogeological divisions are distinguished:
Kazan aquifer with fissure-karst-stratal waters in limestones, dolomites in the northern part of the Volga Upland, the territory of the Low Trans-Volga region and with porous-fissure-stratal waters in terrigenous rocks interbedded with carbonate rocks within the High Trans-Volga region;
Tatar aquifer with porous-fractured-stratal waters in terrigenous rocks interbedded with carbonate;
Neogene-Quaternary water-bearing complex with porous-stratal waters in sandy-argillaceous deposits.
Kazan aquifer
Represented by two large types of accumulations of groundwater:
a) fissured-karst-layered in limestones and dolomites of hydrogeological sections of the northern part of the Volga Upland and the Low Trans-Volga region;
b) porous-fractured-stratal in terrigenous rocks interbedded with carbonate in sections of the High Trans-Volga region.
The depth of the roof of the complex is consistent with the structural and tectonic features of the territory and varies depending on the modern relief. In the zone of occurrence of fresh waters, the depth of the roof varies widely - from a few meters in river valleys to 80-100 m in watershed areas, averaging 20-60 m.
The thickness of water-bearing rocks in the whole region is 20-50%, and in fractured, destroyed and karst carbonate deposits up to 70-100% of the thickness of the aquifer complex. According to the conditions of occurrence, the underground waters of the Kazan complex are classified as pressure-non-pressure, the pressure varies from a few to 100 m, rarely more. On a larger area of distribution of the complex, the pressure values are within gradations of 0-20, 20-40 m.
In terms of water content, the Kazan complex is characterized by significant heterogeneity, which is due to different lithological composition and conditions of occurrence of water-bearing rocks; in general, a decrease in the water content of the complex can be traced from the southwest to the northeast.
The aquifer is fed mainly by the infiltration of atmospheric precipitation in the areas where the described deposits reach the day surface, as well as by the overflow of water from the overlying aquifers. In some areas, the complex is additionally fed due to the inflow from the underlying Ufa deposits. Water is discharged into the local hydrographic network, rarely into the underlying complexes.
According to the component composition, groundwater belongs to hydrocarbonate, sulphate and chloride types, hydrocarbonate and sulphate types prevail. Of the cations in groundwater, calcium was identified, and to a lesser extent magnesium and sodium. Groundwater within the zone of intensive water exchange is mainly bicarbonate calcium, fresh, mineralization up to 0.5 g / dm 3, confined to the central parts of the watersheds. Within the slope parts of the watersheds, and sometimes in the valley areas, groundwater of the hydrocarbonate-sulfate type with a mineralization of 0.5 to 1 g/dm 3 can be traced. Down the section, a regular increase in mineralization is observed due to lesser washing of rocks. Groundwater of sulfate, sulfate-hydrocarbonate, sulfate-chloride types is water of increased mineralization, distributed in the form of local areas against the background of fresh water, confined mainly to river valleys.
The waters of Kazan deposits are widely used for water supply of large cities, regional centers, small settlements, industrial enterprises by centralized water intakes, single wells, and springs.
Tatar aquifer
Represented by porous-fissure-stratal waters in terrigenous rocks interbedded with carbonate. The complex has a wide distribution, almost similar to the Kazan aquifer complex, is absent or has a sporadic distribution only in places of general geological uplift of layers.
Groundwater is confined to the Upper and Lower Tatar deposits, which often have an identical lithological composition of rocks and conditions for the formation of groundwater. The Upper Tatarian deposits are less widespread than the Lower Tatarian deposits, since in the uplifted structural-tectonic zones they are completely or partially eroded, groundwater is drained and has a sporadic distribution. A distinctive feature of the Tatar formations is the inconsistency of the lithological composition, density and fracturing of rocks, both in the distribution area and in the section.
The aquifer complex is composed of a thick layer of red-colored and variegated argillite-like clays, siltstones and sandstones with interlayers and lenses of sands, limestones, dolomites, marls, conglomerates. The carbonate interlayers are confined mainly to the lower part of the section of the Tatar complex and have a local distribution. With a deep occurrence of the water of the complex, they have increased mineralization. The water-bearing rocks are loose sandstones, sands, interlayers of gravel-pebble deposits, fractured siltstones, marls, limestones, and lenses of conglomerates. The presence among the water-bearing rocks of insignificant thickness of water-resistant ones, which are clays of the same age and dense siltstones, creates the condition for the formation of a large number of aquifers with a thickness of several centimeters to 13-24 m. The thickness of the aquifer complex within the fresh water zone varies from several meters to the boundaries of its wedging out up to 80-100 m and more.
The total thickness of water-bearing rocks is 10-50%, rarely more than the thickness of the aquifer and varies mainly from the first to 30-40 m, reaching 60-85 m in local areas. Groundwater of the Tatar complex is formed at different depths; depending on the relief, terrain and thickness of the overlying sediments, the depth of the aquifer complex ranges from 3.5 to 135 m or more.
The waters of the considered complex on the territory of its distribution are predominantly fresh, the mineralization does not exceed 1 g/dm 3 . Less mineralized (up to 0.5 g / dm 3) waters are more common in the central parts of the watersheds. Waters of increased mineralization are distributed locally, in separate areas of various sizes, and are more often confined to the valleys of large rivers. Significantly long sections of such waters can be traced in the valleys of the Volga and Kama.
In terms of chemical composition, groundwater is quite diverse: the hydrocarbonate type is developed mainly within the watersheds, in the washed-out upper part of the complex. The most widespread are bicarbonate-calcium waters, less - bicarbonate-sodium and slightly - bicarbonate magnesium. Sulfate-type underground waters are locally distributed in places where there is a connection between the aquifer and the mineralized waters of the underlying strata.
The power source of the complex is atmospheric precipitation in the places where the rocks of the Tatar age come out to the day surface, with a deep occurrence of water-bearing sediments, there is an overflow from the upper horizons. Groundwater is discharged through erosion incisions in the form of latent runoff into rivers. Open discharge is manifested by numerous springs, reservoir outcrops, hollows along river valleys, slopes of gullies and ravines.
The waters of Tatar deposits in shallow areas are widely exploited for drinking and domestic water supply of numerous settlements, both with the help of single wells and through group water intakes.
Neogene-Quaternary aquifer complex
It is represented by porous-formation waters in sandy-clayey deposits. It has the widest distribution within the study region.
It is difficult to distinguish between the genesis of water-bearing alluvial-Quaternary formations and complex Neogene sections of freshwater, brackish and marine sediments due to the ambiguity and lack of geological and hydrogeological knowledge.
Water-bearing deposits of the complex as a whole are represented by Neogene and Quaternary rocks. The above formations are characteristic of certain landforms, have lithological features, with which their watering is directly related. Separate flooded strata of the Quaternary age, stratigraphic units of the Neopleistocene and Holocene, the water content of which is not of significant practical importance, were removed from the map. These are deposits of the Don horizon and eluvial-deluvial, biogenic and eolian; in general, they are characterized by both mosaic and cloak-like occurrence with a dominant clay composition of predominantly small average thicknesses.
The depth of the waters of the complex is within 0.5-50 m or more from the surface of the earth, the maximum depths are up to 70 m or more. Watered sand layers are not consistent in thickness and strike, often lenticular, hidden at various depths from several to 40-50 m. Within the considered boundaries of the distribution of the complex, there are numerous areas with a reduced thickness of water-bearing rocks less than 10 m.
According to the conditions of occurrence of water, for the most part of its distribution, they are classified as non-pressure.
The aquifer complex is fed by atmospheric precipitation, surface waters, as well as pressure waters of the underlying aquifers.
According to the chemical composition of the waters of the complex, most of their distribution is fresh, their mineralization is from 0.04 to 1 g / kg. The composition is bicarbonate-calcium, sodium, less often - bicarbonate-sulfate calcium and magnesium. An increase in mineralization is also possible due to the enrichment of waters with soluble components when moving from the recharge area to the discharge area and due to the discharge of sulfate waters from the Lower Permian deposits. Rigidity in most cases from 1-7 to 8-10 mmol/dm 3 , in some areas above the norm.
Domestic and industrial pollution often occurs throughout the entire area of distribution of the aquifer. Groundwater (within certain areas) has been studied by a large number of deposits explored for water supply of settlements, industrial enterprises and agricultural facilities, and almost everywhere they are promising for water supply, both for small settlements and for use as a source of centralized water supply for large cities .
The complex geological and hydrogeological conditions of the region predetermine the uniqueness of the hydrodynamic characteristics of groundwater, including the directions of surface and underground runoff. The feeding areas of the first aquifers from the surface are usually the areas of their distribution; for deep-lying, based on geological considerations, usually hypsometrically elevated domed structures of the first order, where conditions exist for surface water infiltration. The area of discharge of deep-seated aquifers is the Caspian Basin, which continuously subsided in the Mesozoic-Cenozoic time.
Structural-tectonic features play a dominant role in determining the conditions for the accumulation of groundwater, and physical-geographical and paleographic features in the formation of their chemistry. Within the region, there is a numerous change of sharp uplifts and subsidences of structures of higher orders with the imposition of structural subdivisions of lower orders, which generally determine the depth of distribution of fresh waters.
The physical and geographical conditions of the study area correspond to three landscape zones, determine the conditions for the recharge of aquifers and, ultimately, their chemical composition. Groundwater recharge generally deteriorates from north to southeast. For territories with insufficient supply of groundwater of the upper structural-hydrogeological level and shallow dissections of the relief, peculiar conditions arise when water-bearing rocks of individual stratigraphic units do not have independent practical significance. Groundwater under such conditions may have sporadic watering, usually several aquifers are exploited together, forming single aquifers with lithological uniformity of water-bearing rocks.
