1.10.2. Underground water resources

Hydrogeological conditions of formation and underground waters spreading of coastal zone are quite diverse. Here one can observe areas from watery to anhydrous ones, from areas with deep level subsidence to flooding territories. Accounting geology-lithological peculiarities, conditions of alimentation and transit, spreading and draining, the following hydrogeological regions with interaction of water levels are distinguished (Fig. 26): Samur-Devechi, Pri-Caspian-Apsheron, Gobustan, Lower Kura, Talysh and Lenkaran. Common run off to Caspian Sea by these regions makes 3,17 km³/a year.

As it was specified in the section 1.2.2.1 by relief peculiarities determining basically by geological structure, the given region are divided into three areas: strip of middle mountains and foothills, Gusar foothill sloping plain and Shollar coastal plain. These 3 parts of territory are different as well as in hydrogeological relation. In middle mountain area and foothills due to sharp relief intersection and clayey rocks composition ground waters of sporadic spreading are mainly developed and located in eluvial-talus or talus-proluvial clayey deposits subsiding near foothills of slopes. In the territory of foothill of slope plain basic horizon of ground waters dissected by deeply cut hydrographic network on several flows are formed. The latter descending to coastal plain enter into area of debris cones development, where a single flow of ground waters is finally formed in the direction of sea.

Following the zone of natural conditions three hydrogeological regions can be distinguished: 1) domination of surficial run off; 2) alimentation and transit of ground waters; 3) ground waters unloading

Ground waters are spread in deposits from Pliocene age to the recent ones. Surface of ground waters flow on the whole follows the day surface, depth of their occurrence from foothills to sea decrease. The most depth of ground waters occurrence is observed in upper parts of debris cones of rivers, here it exceeds 50-75 m, and in the upper part of cone of Samur River it is more than 100. In region of Samur-Apsheron channel ground waters level rising to 3 m (that is linked with water infiltration from channel), eastward Baku-Khudat highway-5-8 m and less. Between sea coast and highway ground waters are mainly at depth 2-3 m, but there one can find massifs, where they are located at depth less than 1 m. In the coastal strip separate areas are flooded and swamped. In sites, where the level of ground waters reaches the surface, springs of different discharge and mineralization are located. In the first and second hydrogeological subregions they are fresh hydro-carbonate calcium with discharge from 2-3 l/sec. Coastal strip (third subregion) is abundant by springs outcrops, which from the north-west to the south-east stretch basically by three lines. For territory located between Samur River and Devechi Mountain there are data on 374 springs with total discharge 6257 l/sec.

Most of springs are of descending nature, but one can mark ascending springs in that place, where loam's interbeds or clays subsiding in the top of water-bearing rocks create local pressure. Springs discharge varies from 10-s share to 280-320 l/sec.

In valleys of rivers recent alluvial deposits are water-bearing only in zone of foothill and in low current of rivers, where depth of ground waters occurrence less the thickness of recent alluvium. Near the sea ground waters are in eolian and recent marine deposits expressed by sands and shells. Quantity of springs, their total and average discharge decreases from the north to the south.

In plain part of territory wells and captation galleries exploiting ground waters strip ground waters out. In the north part of region in Samur-Gusarchai interfluve ground waters are fresh, hydro-carbonate-calcium with thick residual 0,5 g/l. Southward their mineralization increase to 1 g/l and in the coastal strip, where dominate marine turbid deposits to 2,5 g/l (hydrocarbonate-sulphate-natrium waters).

Salted waters are spread mainly in the lowers of Chagadjukchai-Velvelichai interfluve where muddy and clayey rocks of marine origin are developed. To the south of Shabranchai river mineralization of ground waters quickly increase to 25-30 g/l; here one can observe typical salt bottoms. Increase of ground waters mineralization degree in the south-eastern continuation is stipulated by increase of climate aridity and increase of clayey and muddy marine sediments share in the section of upper-Quaternary deposits.

Pressured waters. In the strip of conjunction of Gusar foothill and Shollar coastal plains shingles of Apsheron age are subsided under deposits of debris cones of coastal plain containing clayey interbeds of continental and marine origin. Clayey interbeds of debris cones and underlying deposits separate common flow of ground waters into several "stages".

In accordance with stratigraphic dissection of geological section of the given strip here (in quaternary and Pliocene deposits) six water-bearing complexes and water-prove layers having local spreading are distinguished. Water in these complexes fresh, hydro-carbonate-calcium and hydro-carbonate-natrium with mineralization 0,3-1,0 g/l in some cases to 2,5-3,5 g/l (sulfate calcium-natrium waters). Discharges of wells vary within wide ranges: from shares to 104 l/sec.

Water-bearing complex of Mesozoic deposits is stripped out at a large depth, waters are strongly mineralized and have high temperature. So, in wells in the coastal plain in the Cretaceous deposits water with mineralization approx. 20 g/l containing iodine (10 mg/l) and ammonia (63 mg/l) was stripped out. Water with mineralization 23,6 g/l with iodine content 6,4 mg/l, bromine 9,3-mg/l and ammonia 72 mg/l was obtained from Jurassic deposits.

Common underground run off from the specified aquifer complexes of Samur-Devechi region is 0,87 km³/a year and total ion run off reaches 1470 thousand ton/a year.

Within region Cretaceous, Paleogene and Neogene complexes of deposits outcropping on the surface in the mountain zone are subsided in the direction of sea and overlapped by Quaternary formations of coastal plains and Absheron peninsula. Principally different conditions for formation and spreading of underground waters especially ground ones are created.

Ground waters of region are formed mainly owing to infiltration of atmospheric precipitation as well as a result of technogenic influence.

In mountain an foothill zone of Beshbarmag-Kemchi subregion ground waters are differentiated by sporadic spreading and are mainly found in alluvial-talus formations on the slopes of elevations and zones of jointing of bedrock outcropping near the foothill of slopes. In accordance with conditions of spreading quantitative and qualitative characteristics of ground waters is different.

Thickness of aquifer series usually do not exceed 1-2 m reaching in some places 5-10 m and more. Springs are differed by low discharges-from 0,1 to 3,5 l/sec., water mineralization usually varies within 0,3-10 g/l, sometimes reaching 30-40 and even 126 g/l. Chemical water composition changes from hydrocarbonate-sulfate natrium and sulfate-hydrocarbonate natrium to chloride-sulphate natrium.

In Seaside (Devechi-Sumgayit) subregion water-bearing Cretaceous deposits of mountain zone are subsided in the south-eastern direction under water-persistent formations of Paleogene-Neogene presented by clays and marls. Completing the section clays and sandstones of Middle Pliocene are water-bearing: low-thick lenses an horizons of ground waters of hydro carbonate-chloride and sulfate-chloride composition with residual less 1 g/l are confined to them. Their depth of occurrence varies from 20 to 1 m and along Samur-Apsheron channel 5-10 m decreasing toward the sea to 3-1 m.

Recent beach deposits developed along the coast by strip with width to 1 m are presented by fine-grained sands and shells. Lenses of fresh and salted hydro-carbonate-chloride natrium-calcium waters with mineralization 0,3-9,6 g/l are located at depth 0,3-6,0 m.

Horizon of salted chloride-sulfate natrium-magnesium waters is located under them. In the coastal strip one can observe areas of flooding and swamping.

Apsheron subregion by its hydrogeoplogical conditions is subdivided into two areas: Western-Apsheron and Eastern-Apsheron the border between of which pass from Nardaran village on the northern coast of peninsula to Govsan cape on the south coast.

Western-Apsheron section is mainly composed of dislocated Paleogene-Neogene clays with interbeds of sands and limestones which are non- concordantly overlapped by gently-subsided clays, sands and limestones of Quaternary age.

Ground waters in Paleogene-Neogene deposits are differed by sporadic spreading and confined mainly to zones of jointing and small synclinal structures. Descending springs have discharges to 1,0, rarely-to 3,5 l/sec. Depth of water occurrence from o to 60 m, value of mineralization-from 0,5 to 145,7 g/l. Chemical water composition is hydro-carbonate-chloride, sulfate-chloride natrium-calcium-magnesium and natrium.

In Quaternary deposits ground waters are contained in aquifer horizons of Pleistocene as well as recent, eluvial-talus-proluvial and beach deposits at depth from 0,2 to 26 m and more, discharge of descending springs-0,4-1,0 l/sec, specific discharge of wells-0,01-2 l/sec. m, value of mineralization-from 0,7 to 90 g/l. Chemical water composition is parti-colored mainly hydro-carbonate-sulfate, hydrocarbonate-chloride, sulfate-chloride and chloride-sulphate-hydrocarbonate natrium-calcium, natrium-magnesium.

Ground waters in the eastern part of Apsheron peninsula are spread almost everywhere besides its central and south-western parts. Basic resources of ground waters of described territory are linked with quaternary (Khazar and upper Apsheron) deposits, composing the most part of territory and presented by limestones-shell, sandstones, fine-grained sands and clays. Ratio of filtration of water-enclosing rocks vary within 2,6 to 31m/daily, wells discharge sometimes reach 7 l/sec (Bina-Govsan depression), specific discharges make 0,04-1,8 l/sec-m.

Coastal regions in the eastern part of peninsula are presented by Khvalyn, new-Caspian and recent marine deposits, sands and loose limestones-shell with interbeds of clays. Depth of ground waters occurrence varies within wide ranges-from 2-5 m in central part of Eastern Apsheron to 20 m in its northern and north-western parts.

Mineralization of ground waters varies within 0,05 to 100 g/l and depends upon saltiness of underlying rocks. Fresh and poor-salted (0,5-1,2 g/l) ground waters: hydrocarbonate - chloride - magnesium and natrium - magnesium, hydrocarbonate - sulfate natrium - calcium, chloride - hydrocarbonate magnesium - natrium and chloride - sulphate natrium - magnesium.

It should be pointed out, that territory of Absheron peninsula cross Samur-Apsheron irrigation channel, water loss from which exert a noticeable influence upon regime of ground waters bringing to flooding of considerable areas.

The considered data show, that in south part of peninsula regime of ground waters is formed mainly under influence of climate change and fluctuations of Caspian sea level. On the rest, most part of territory crucial influence upon regime exerts artificial factors: irrigation, infiltration from channels.

Pressured waters in Pri-Caspian-Apsheron region are confined mainly to Quaternary (Baku stage), Neogene and Paleogene deposits.

Aquifer complex of Baku stage (Low Pleistocene) is developed on Apsheron peninsula mainly in Baku, Bina-Govsan and Zirya troughs and consists of three aquifer horizons.

Water mineralization 1,1-5 g/l in some cases increase-to 10-30 g/l. By depth mineralization increase. Water composition is hydro-carbonate-sulphate, sulfate-chloride and chloride-sulfate natrium-calcium, natrium-magnesium, rarely calcium-natrium.

Thickness of aquifer horizons and depth of their occurrence increase from the north o the south. Specific wells discharges vary within 0,4 to 5,2 l/sec. m.

Aquifer complex of Apsheron deposits (Eopleistocene) is stripped out wells in Gyuzdek, Baku and Zirya troughs and consists of three pressured horizons. Water mineralization is mainly 1,0-3,1 g/l composition changes from hydrocarbonate-chloride calcium-magnesium to chloride-sulfate natrium-calcium. In low horizon one can find water with mineralization to 23-40 g/l and even 87,8 g/l, water type is chloride-sulfate, natrium-magnesium and chloride natrium. Wells discharge varies within 0,2-7,5 l/sec, specific discharge varies from 0,3 to 2,0-2,2 l/sec. m. Ratio of filtration of water-enclosing rock vary from 0,2 to 13,8 m/daily.

Aquifer complex of Low Pliocene (Productive series) is presented by 18 water-bearing horizons, locating in complicated interactions with oil-bearing layers. Water pressured on the dominating part of territory is not self-flowing. Wells discharge, vary within significant ranges from 100 to 500 cub. m/daily. Ratio of filtration of water-containing rock varies from 0,4 to 1,0 m/daily.

Hydrochemical section of productive series is sharply divided into two parts: upper, containing strongly mineralized waters with thick residual 80-200 g/l, low for which typical waters with mineralization from 10-15 to 70 g/l. Waters are chloride natrium, non-sulfate.

In Surakhany and Shikhov areas hydrogen sulfide mineral waters are linked with deposits of productive series with content of hydrogen sulfide from 60 to 460 mg/l. Water is muddy with smell of hydrogen sulfide with residual 17-30 g/l, chloride natrium-magnesium, chloride-hydrocarbonate, natrium or natrium-magnesium-calcium.

1.10.2.3. GOBUSTAN REGION

Gobustan region is characterized mainly by development of clayey rock of Paleogene-Neogene age which at significant areas mainly in central and south parts of region are overlapped by quaternary formations and breccia of recent mud volcanoes. Physico-geographic conditions and geological section of region predetermine sporadic spreading and increased mineralization of ground waters.

Ground waters are found mainly in valleys of rivers and in zone of jointing of bedrock outcropping on the surface near the slopes of foothill. In valleys of small-number rivers alluvial-proluvial shingles, loams, sandy loam and sands with interbeds of gravel-shingle deposits with thickness 1-15 m are developed. Ratio of rock filtration varies from 5 to 14 m/per days. Depth of ground waters occurrence varies within 0-5 m, springs discharge as a rule doesn't exceed 1,5 l/sec. Value of water mineralization varies from 0,1 to 37-40 g/l with tendency of values increase down the stream of rivers. Chemical composition is mainly hydrocarbonate-sulphate natrium to chloride-sulphate natrium. Here one can observe dependence of water composition upon bedrock composition. Local spreading has a water-pressured horizon of recent mud volcanic deposits presented by breccia subsiding around mud volcanoes.

Water formation occurs mainly owing to infiltration of atmospheric precipitation. Unloading is realized mainly by lateral run off and evaporation.

Pressured waters are confined mainly to quaternary and Neogene-Paleogene deposits.

Aquifer complex of Eoplestocene (Apsheron stage) is confined to synclinal subsiding limestones or sands interbeds in the thickness of clays and is located at depth from several dozens to 100 m. Ratio of filtration 5,3 m/per day. Wells discharge up to 1 l/sec. Water is chloride-sulfide natrium, mineralization from 2,7 g/l to 22,1 g/l.

Aquifer horizon of the Upper Pliocene (Akchagyl stage) in the Western Gobustan is differed by sporadic spreading. Waters are salted of chloride-natrium composition with dry residual to 7 g/l. Wells discharge reaches to 1,1 l/sec.

Aquifer complex of Low Pliocene (Productive series) has a wide development. Wells's discharge varies within 10-200 cub.m/per day and more. Chloride natrium waters predominate with mineralization 130-300, sometimes to 396 g/l.

Aquifer complex of Upper and Middle Pliocene is marked on structures, representing brachy-anticlines, complicated by dislocations and overthrusts. Water is hard, chloride-natrium with mineralization from 10 to 34-46 g/l.

Aquifer complex of Maycopian deposits subsiding in the deep closed structures of the south-western parts of described territory, frequently contain stratal waters, linked with oil. At different areas different quantity of aquifer horizons is marked sometimes to 4. Wells discharges changed by overflow within 0,05-to 0,6-1l/sec., increasing on the Nardaran-Suleiman areas to 4,6l/sec. Water in many cases is alkali, chloride-natrium with thick sediment from 66-to 148 g/l.

Outcrops of hydrogen sulfide mineral sources (Jabani, Khilmilli, etc) are confined to Maykopian deposits. Their discharge is not great enough water mineralization from 1,9 to 8,3 g/l, content of hydrogen sulfide reaches 12,9 mg/l. Water of Jabanin sources is hydrocarbonate chloride-natrium, Khilmin -sulfate, aluminum-magnesium-calcium. Water temperature is 15,3-18,2⁰.

Structural and morphological peculiarities of region, construction and composition composing geological section of rock characterize region as reservoir of underground waters. Common flow of ground waters, directed to the Caspian Sea, makes 0,02 km³/year, and ion run off 200 thousand t/year.

Ground waters are stripped by wells everywhere. The first from the surface horizon is subsided at depth 1-3 m and is separated from low located horizon of pressured waters, series of clays with thickness from 2-2,5 to 80-100 m. Exception makes areas brachy-anticlinal elevations. Kursangya, Babazanan, Durovdag, Goytepe, etc., where depth of ground waters occurrence increase to 5 and even 10 m. Thickness of water-saturated series varies from 10 to 70 m. Thickness is composed of lithologically different rock of Quaternary age of various genesis. Generally relief of surface of ground waters repeats relief of surface and has direction of recent surficial run off. Beginning of ground waters flow is in the foothills of Greater Caucasus and Talysh where marks of surface is maximal.

Ratio of filtration correspond to regularities of change of lithological structure, their values change within 1 to 60 m/per day, with predominance 3-5 m/per day.

The main source of ground waters alimentation is atmospheric precipitation, condensation of water pores, or filtration from irrigation-melioration systems.

Ground waters are characterized by exclusive variety of degree of mineralization and composition. Available data characterize the main part of ground waters flow.

Waters are considered to be the dominating ones, of chloride-sulfate, natrium type with mineralization 2-10 g/l. Chloride natrium magnesium waters are stable just in the territory of Mugan-Salyan steppe, where their mineralization varies within 10 g/l in near-channel zone to 100 g/l in central part of steppe.

Hydrocarbonate-calcium waters less spreading and have mineralization to 0,7 g/l. By presence of other components in them like sulfate and natrium-water mineralization of this type increase to 1,0 g/l, and by presence of magnesium in some cases to 2,0 g/l.

Pressured waters within regions are confined to Quaternary and Paleocene deposits.

They are salted everywhere, practically not suitable for use. 4-aquifer horizon are studied, mineralization of which varies from 5 to 129 g/l.

Fragmented and fragmented veined waters are mainly developed here. Available data specify to the absence of thick of under riverbed flows in the alluvial deposits of fluvial valleys and to the poor-aquifer talus loam-clayey cover. In some areas one can observe water draining of bedrock of rivers valleys.

Aquifer complex of Middle and Upper Miocene is confined to the interbeds of fragmented sandstones and marls, subsiding among gray and brown-gray clays. Complex is poor aquifer. Discharges of descending springs do not exceed 0,1-0,2 l/sec. Water is fresh or salted with dry residual from 0,5-1,6 g/l, hydro-carbonate, calcium-natrium-magnesium or hydrocarbonate-sulfate and hydrocarbonate-chloride, calcium-magnesium.

Aquifer complex of Oligocene-lowers of Middle Miocene (Maykopian suite) is confined to the interbeds of sandstones and tuff-sandstones, subsiding in thick series of clays. Here there are descending springs with discharge within 1-3 l/sec, water mineralization 0,2-1,5 g/l, composition is hydrocarbonate-sulfate, calcium-magnesium.

Aquifer complex of the Eocene is confined to the fragmented series of tufogene-sedimentary rock, composing the highest parts of Talysh Mountains. On the slopes of mountains one can observe a large amount of descending springs with discharge from 100 shares to 2-2,5 l/sec and more. Mineralization is 0,1-0,5, sometimes 0,7-09 g/l, waters are hydrocarbonate-calcium and calcium-natrium, sometimes hydrocarbonate-sulfate-calcium.

Mineral and thermal sources are widely developed in rocks of Miocene, linked with dislocated tectonic disturbances and are concentrated on the border of Talysh Mountains and Lyankaran lowland, in three areas.

Arkevan, Donguz-Oten, Gotursu (Yanarsu), Misharsu (Muradsu, Misharchai), located along the right coast of Vilyashchai river approx off Masally city are located to the Masally group of sources. Water temperature-48-65⁰, discharge-to 7 l/sec, total discharge approx. 25 l/sec. Water with mineralization 12-17 g/l, chloride-natrium-calcium. One can observe spontaneous gas emanation in which 80-85% make hydrocarbones of methane order, and the rest part -nitrogene. Waters contain iodine (to 30 mg/l), S_iO₂ and other microcomponents.

Low Lenkaran. (Anjyn), (upper Lyankaran (Ibadysu), Gaftoni and Gavzavua are related to Lenkaran group of sources. In this region there are wells with depth to 1013 m. Water temperature on the outcrops of springs 37-43⁰, in wells 34-47⁰, it increase with depth. Total discharge of all natural and artificial (wells) outcrops reaches 25 l/sec, water is salted, chloride-natrium-calcium. In water of springs dry residual makes 3,6-4,5 g/l. Hydrogene sulfide (2,9-6,0 mg/l), bromine, iodine and S_iO₂ in quantity from 26,2 to 40,5 mg/l and other microcomponents. In springs and wells sometimes one can observe gas emanation, consisting mainly of nitrogene. In wells, starting from the depth 500 m, in gas composition dominate hydrocarbons of methane order, quantity of which reaches 77,5%.

Astara group of thermal mineral sources is located in valley of Istisuchai River at a distance of 4 km northward from Alasha village. Total discharge of all outcrops is 2,5-2,7 l/sec; water temperature varies within 45 to 48,5⁰, mineralization from 19,1 to 22,4 g/l. Water is chloride, natrium-calcium and iodine (3 mg/l), and bromine (8 mg/l) were established in it. Gas is intensively emanating from water, for 99-100% consisting of nitrogene. Some less significant emanations of mineral waters of the same aquifer complex has less discharges and more low temperature.

Aquifer complex of Paleocene is presented by aleurolite-tuffites and tuff-sandstones. Water content of these deposits is determined by degree and character of their jointing. All springs are almost descending ones, their discharge 0,5-0,7, rarely 1-1,2 l/sec. Common mineralization 0,1-0,4 g/l. Composition is usually hydrocarbonate, rarely hydrocarbonate-sulfate, calcium-natrium.

Common features of territory formation and "border conditions", in which it is located-tributary of underground waters from foothill side and draining of aquifer horizons by Caspian sea, -determine hydrogeological condition. Underground waters here saturate the whole series of sediments of Quaternary age, having various genesis. In accordance with presence of loam-clayey interbeds in this series underground waters are both of ground and pressured nature. In accordance with geomorphological structure three subregions are determined here, characterizing by different hydrogeological conditions: 1) foothill, alluvial-proluvial plain; 2) alluvial-proluvial lowland; 3) Primorskaya lowland.

Ground waters.

Subregion of foothill plain from the east is limited by projection with zero horizon line. Ground waters subside at depth from 5 to 20 m and more. They are formed as a result of contact overflow of fragmented waters of native deposits into ground waters of lowland and loss of surficial waters in rivers channel. In springs water is fresh with thick sediment to 0,5 g/l, hyfrocarbonate-calcium. Surface of ground waters is subsided at depth 1-3 m. Mineralization varies within 0,5-2,0 g/l, in some cases 25 g/l. Water composition is mainly hydrocarbonate-calcium, hydrocarbonate natrium and chloride-calcium.

Artificial reservoirs substantially influence upon hydrogeological conditions of region, as well as irrigation, causing the rise of ground waters level. Amplitude of seasonal fluctuations of ground waters makes 1-2 m, reaching zero marks in autumn-spring period.

Alluvial-proluvial plain covers mainly debris cones of Lenkaranchai and Vilyashchai.

Within debris cone of Lenkaranchai ground waters are spread everywhere. The main sources of their alimentation is ground waters of river and atmospheric precipitation. Surface of ground waters is subsided at depth 0,5-3,0 m, waters are fresh, thick water sediment usually doesn't exceed 1,0 g/l. Along the periphery and seaside debris cone mineralization usually reaches 3-25 g/l, water type-sulfate-natrium-calcium and chloride-natrium.

Subregion of seaside lowland is composed of loams, sandy loams and sands mainly of marine origin. Ground waters subside at depth 1-2,5 m, and during the high standing of level (spring-autumn) in sites outcrops on the day surface forming vast swamped areas. Ground waters are mainly wasted during evaporation, due to of which salts are accumulated in water and soil. Water mineralization reaches 35 g/l, its composition is chloride natrium. Hypsometrical dominating position occupies seaside bank. Water mineralization here doesn't exceed 2 g/l increasing in marginal parts of bank to 3-5 g/l; waters are hydrocarbonate calcium.

Everywhere ground waters level regime depends upon regime of sediments and closely connected with it regime of rivers waste reflecting that peculiarities of their distribution with which the northern part is differed from the south one.

Irrigation substantially influence upon regime of ground waters. However in most cases this influence is reflected upon seasonal regime and doesn't change reservers of ground waters. Wells discharge varies within 0,23 to 16 l/sec, specific discharges 0,03-2,9 l/sec.m, and ration of filtration-from shares to 40 m/per day.

Pressured waters are stripped in deposits of Khvalyn and Khazar stages of Quaternary system.

Aquifer horizon of Khvalyn stage (Upper Pleistocene) is stripped out at depth from 11 to 87 m. Thickness of aquifer rock reaches 30 m and more. Piesometric level is established at 0,7-4,2 m above the surface. Specific wells discharges are not great enough: 0,3-0,8 l/sec.m. Wells discharges by overflow make to 1,5 l/sec. Mineralization 0,4-0,8 g/l, waters are hydrocarbonate chloride and chloride-hydrocarbonate, natrium-calcium or natrium-calcium-magnesium. Down in the direction of seawater mineralization increase and practically aquifer horizon is used only in the western part of region of its spreading.

Aquifer horizon of Khazar stage (Middle Pleistocene) is subsided at depth from 17 to 200 m. Piesometric level is established at 2,7-6 m above the earth surface. Specific wells discharges 0,1-0,7 l/sec. m. Wells discharges by overflow reach 5 l/sec.

In the north-western part waters regions are fresh with thick residual 0,4-1 g/l, hydrocarbonate-sulfate chloride natrium calcium. In the south direction water mineralization increase to 6 g/l, composition changes into sulfate-natrium-magnesium-calcium.

Possibilities of underground waters use for water-supply and needs of various branches of economics are determined by values of their exploitation resources which were determined by results of exploration on areas of existing water transpiration systems (accounting their extension), on exploring of prospecting areas as well as in the process of regional estimation.

Within plain and low-lying regions natural conditions of ground waters formation are broken by human activity having ancient history. It caused to change very significant, role of most natural, formation of some artificial sources of ground waters alimentation, which in some cases became dominating ones. That's why resources are really determined in practice composing of natural (underwent certain changes) and artificial resources, which are called "composing" resources, i.e. total renewed ground waters alimentation, supplying their total unloading in condition broken by intensive technogenic influence.

In Table 1-10 modules of formed resources of underground waters flow of alluvial-proluvial plains, determined actually by incoming elements of balance of ground waters were characterized, and modules of formed underground run off of fresh and poor-salted waters in the same regions, determined by results of hydrodynamic calculations.

Table 1-10. Modules of formed resources flows of underground waters

Forecasted exploitation resources of low-mineralized underground waters was evaluated for plain zone covering flows of underground waters of alluvial-proluvial plains and territory of eastern part of Apsheron peninsula (Table 1-11).

Table 1-11. Forecasted exploitation resources of underground waters

Note: Performances for poor-salted (1-3 g/l) underground waters by their presence are shown in denominator of fraction

As it is seen from Table 1-11 common prognosticating exploitation resources of underground waters flow of alluvial-proluvial plains reach 3598 thousand m³/per day, from which 96,5% falls to fresh underground waters. Distribution of prognosticating exploitation resources by complexes is also not similar. The most part of resources is linked with upper complex of continental deposits (77,6%).

On the whole modules of prognosticating exploitation resources of underground waters of the whole continental series reach 13 l/s km² on Gusar-Devechi and 1,3 l/s km²- Pri-Talysh plain. Modules of prognosticating exploitation resources of the third aquifer complex (marine deposits) on Gusar-Devechi plain make 5-6 l/s km². On Apsheron peninsula prognosticating exploitation resources of underground waters are insignificant and their modules vary within 0,3 to 3 l/s km².

Exploitation resources of underground waters of river valleys within plains are given in Table 1-12.

Exploitation reserves of underground waters for the period 01.01.1986 year are given in Table 1-13.

1. Abdulla-zadeh A.A. Water-supply and water protection of the Caspian shore of Azerbaijan SSR. – Baku; "Elm", 1989.

2. Askerbeyli E.K. Fresh underground waters of the Quaternary deposits of Kura-Araks lowland and prospects of their use. – Proceedings of Baku Branch of VNII VODGEO, edit.XI, 1975.

3. Askerbeyli E.K., Popov A.P., Bulatov R.V., Kyazimov S.M. Underground waters of Azerbaijan north-eastern part and prospects of their use for water-supply. – Moscow; "Stroiizdat", 1974.

4. USSR hydrogeology, v.XII, Azerbaijan SSR. – Moscow; "Nedra", 1969.

5. Israfilov G.Yu. Ground waters of Kura-Araks lowland. – Baku; "Maarif", 1972.

6. Israfilov G.Yu., Listengarten V.A. Ground waters and development of the Apsheron lands. – Baku; "Azerneshr", 1978.

7. Listengarten V.A., Shahsuvarov A.S. Hydrogeological and engineering-geological conditions, resources, present and prospective use of underground waters of Azerbaijan Republic. – Baku, 1992.

8. Reports of the State Committee of Geology and Mineral Resources for 1990-2000.

INTRODUCTION

SECTION 1

SECTION 2

SECTION 3

SECTION 4

SECTION 5

APPENDIX 15

APPENDIX 16

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