Physical and geographical conditions

1. Geological description

Geological texture of the Turkmenistan coastal zone is composed of sediments of Palaeozoic, Mesozoic and Cainozoic groups. The Palaeozoic group of sediments outcrops at the Tuakyr eminence, forming a deep lying plicate bed. Drilling at the Krasnovodsk peninsula stripped this bed. Igneous rocks, outcropping near the city of Turkmenbashi, Major Balkhan and Tuakyr mountain ridges refer to this age. All these deposits relate to Upper and Middle Palaeozoic according to their stratification and geological features. Middle Palaeozoic deposits outcrop at north-eastern slope of the Kyzil-Kaya eminence. Formations of the Permian system are exposed in the central part of the Tuakyr anticline. They form the sub-altitudinal eminence of Kyzil-Kaya and consist of conglomerate and sandy-clayey rock masses with the thickness up to 3 000 m.

The Mesozoic group is composed of deposits of Jurassic and Cretaceous systems. The Jurassic system consists of upper and middle series. The middle one crops out at Major Balkhan, the upper – at Major Balkhan and Kubadag. The upper Jurassic mainly consists of marine deposits in the lower part and lagoonal-marine in the upper part of the section. Major Balkhan and Northern types of sections are distinguished in the Jurassic of the Caspian zone. Jurassic sections of Major Balkhan and Kubadag relate to the Major Balkhan type, where Jurassic deposits have the thickness up to 4 200 m and consist of two parts. The lower Middle Jurassic part crops out only at Major Balkhan and consists of thick series of dark argillite, shale and sandstone. The upper Upper Jurassic consists of terrigenous-carbonaceous, carbonaceous and carbonaceous-sulphate rocks. The Northern Jurassic type is representative for northern Karabogazgol, where Jurassic sediments occur over Palaeozoic with the thickness of 900 m and consist of partly or entirely eroded carbonaceous-sulphate deposits.

The Cretaceous system consists of two series – lower and upper. The Lower Cretaceous crops out at Kubadag, Major and Minor Balkhans, Tuakyr (south east of the Karabogazgol gulf), and was stripped off by drilling in Cis-Karagogazgol. The Lower Cretaceous is composed of berias-valanjine, goterive, barrem, apt and alb strata. According the nature of sections, the sediments of the Lower Jurassic in the coastal zone are subdivided into southern and northern. Lower Jurassic sediments of Major Balkhan and Kubadag, which are characterised with no break between Jurassic and Cretaceous, better saturation with organic debris, and exclusively marine type of sediments and the highest thickness (up to 3 000 m) are related to the southern type. Sections of the Lower Cretaceous of the same type consist of two parts: lower carbonaceous, according to age referring to berias-valanjine, goterive, barrem, and composed of limestone and dolomite, and apt-albian, composed of sandstone, silt and clay. The Northern type is ubiquitous in Tuakyr, usually with little thickness to 500-750 m, with breaks between Cretaceous and Jurassic and transgressive overlapping of the Lower Cretaceous on underlying sediments. The upper part (apt, alb) is composed of marine facies.

The Upper Cretaceous outcrops in Tuakyr, Kubadag, Major and Minor Balkhans. In the coastal zone it is divided into tuakyr and western-kopetdag types. The Tuakyr type of the Upper Cretaceous is characterised by prevailing low-carbonaceous-clayey siltstone in lower and marl in upper part of sections, frequent breaks and phosphorite horizons, and little thickness of sediments. The biggest sediment thickness, rare breaks and prevailing terrigenous and carbonaceous rocks are typical of the western-kopetdag type.

The Cainozoic group has the widest extent; it is subdivided into Paleogene, Neogene and Quaternary systems. In the coastal zone, deposits of the Paleogene system are exposed at the Krasnovodsk peninsula, near Major Balkhan and in northern and eastern Cis-Karabogazgol. Drilling has stripped off the Paleogene almost everywhere. Mainly two types of sections are distinguished in the Paleogene. The northern (platform) developed in the Krasnovodsk peninsula, near the Tuakyr eminence. It is characterised by little thickness, carbonaceous-argillaceous content of sediments and occurrence of red-coloured rocks. The Southern type of the Paleogene occurs in south-western part of the Krasnovodsk peninsula and in Minor Balkhan. It is composed mainly of clayey rocks with high thickness. The deposits of the Neogene system are widespread and refer to the marine Crimean-Caucasian type. They crop out at a foothill belt of Major Balkhan, on the Krasnovodsk peninsula, in the region of Tuakyr and at the north of Cis-Karabogazgol. Drilling stripped off the Neogene almost all over the flatland. According to the nature of sections they are divided into northern and southern types. The Northern type has developed in a platform region and marked with almost a flat pitch, little thickness and gypsiferousness of sediments. The Southern, geo-synclinal type with the thickness to 4 000 m is spread in the West-Turkmen lowland and in Minor Balkhan. It is characterised with sediment dislocation and variable facies.

The Quaternary system covers the surface of the West-Turkmen lowland, north-west of the Krasnovodsk peninsula and the basin of the Karabogazgol gulf. The Quaternary deposits are divided into Pleistocene and Holocene. Marine sediments of Pleistocene and Holocene with the thickness from 30 to 1 000m developed in the coastal zone. In compliance with stratigraphic scale, the Quaternary deposits is from top to bottom are dissected into Turkan series and Baku stage, Khazar and Khvalyn stages, and Recent Caspian strata. Continental sediments occur in the flood plain of the Uzboy.

2. Tectonics and Seismicity

Studying rocks developed at the Turkmenistan coastal zone, in terms of the level of their metamorphisation, coincidence with appearance of post-igneous processes, and according to the level of their dislocation, one can single out three tectonic from the south to the north, where influence of alpine tecto-genesis is different:

• Region of intense manifestation of alpine tecto-genesis;

• Region of moderate manifestation of alpine tecto-genesis and

• Region of weak manifestation of alpine tecto-genesis.

Pic1. Tectonic zoning/ 1 – Turan platform; 2 – Plicate uplifts (a), depressions and troughs (b), areas of alpine folding; 3 – epi-platform orogenic region; 4 – deep fault: I-Tuahryh, V-Repetek-Erbent, VII-Shordja-Geokchin, VIII-Southern-Turkmen.

Regions, to the south of Kopetdag thermal zone and reaches of Major Balkhan and Kubadag refer to areas of intense manifestation of alpine tecto-genesis.

Regions, bordering in the south with the foothills of northern slope of Major Balkhan and Kubadag, in the north – a line, lying in latidudinal direction from southern escarpment of Cheluninkyr on the Uzboy and to the south of Kemal and Koshaba anticline westward till the Caspian shoreline.

Region of weal manifestation of alpine tecto-genesis is situated to the north of the second tectonic region.

The indicated tectonic regions are separated with deep tectonic faults mostly covered by recent sediments. Tectonic shoves occurred and occur presently along theses tectonic faults during the whole geological development history of the region in various periods, in different places, and with assorted intensity.

Seismically dangerous zones of different magnitudes (from 6 to 9) are distinguished at the territory of Turkmenistan coast of the Caspian. Turkmenbashi seismic region coincides with northern borderland of the alpine folded region, with a deep fault zone. However, this region in not isoseismal: the highest activity is recorded at the reaches of fault development of the north-western strike. Earthquake epicentral area in the Turkmenbashi region extends with a broad belt in western-north-western direction from the city of Kazanjika through the city of Balkanabad (former Nebitdag) to the city of Turkmenbashi and further into the Caspian Sea. A number of limiting and diagonal disjunctive dislocations are found here, related to the above deep fault, which crosses with another zone of north-western disturbances. Zone of maximal earthquake magnitude (9) comprises Major Balkhan – Kubadag metacline, a narrow trough between Major and Minor Balkhan ridges, most western part of the Kapetdag trough and Kapetdag anticlinorium.

The general level of seismicity of this zone is relatively low. However, in past severe earthquakes happened here. Near the city of Turkmenbashi in 1895 – 9-magnitude, near the city of Gazanjika in 1946 – to 8 magnitude, and less severe earthquakes with 6-7 magnitude in 1913, 1934, 1938.

The focuses of recent earthquake is defined to be at the depth of about 30-40 km, i.e. they are located near the bottom of the earth’s crust. In the same time, a vast expanse covered by tremor of the Krasnovodsk earthquake in 1895, allowed for assessing it as a subcrustal with the hypocentre at the depth of about 100 km.

The nature of tectonic processes, leading to earthquakes within Turkmenbashi etrap, alters in latitudinal direction. The peculiarity of the zone is coincidence of weak earthquakes with the places, where severe earthquakes took place in past. In accordance with materials of rerunning of levelling, the Turkmenbashi seismic zone is characterised as a very mobile one in terms of tectonics.

The areas with gradually diminishing isoseismals (from 8 to 6) spread to the north and south of the Turkmenbashi seismic zone. A seismic zone with an 8-magnitude encircles it from the north, south and southeast.

The Karabogazgol gulf is located in a seismic zone with the magnitude ranging from 6 to 7. In general, areas with 6 magnitude are situated on a platform region, therefore severe earthquakes are hardly possible. Far northern and southern end of the Turkmenistan coast of the Caspian Sea is situated in a 6 magnitude seismic zone.

3. Hydro-geological conditions

The investigated area refers to hydro-geological region of inland run-off area, which is subdivided into two hydro-geological regions – Turan and Southern-Ciscaspian. Northern reaches of the region related to Karabogazgol artesian basin, central and southern – to Western-Turkmen artesian basin.

The external region of alimentation of the Karabogazgol basin consists in the east of the Tuakyr eminence, in the south – Major Balkhan. The internal region of alimentation coincides with Ciskarabogazgol lowland plain and intermontane troughs of Tuakyr dislocation system.

Springs with flow not exceeding 0,5 litre/second discharge from Permian sandstone and shale in Tuakyr, with sulphate-chloride sodium water, mineralization - 2-10 g/l. Pressure water in Permian-Triassic gritstone and sandstone was stripped to the north of Major Balkhan. Water-bearing capacity of rocks is poor, water is chloride sodium with bromine, mineralization - 22 g/l.

Ground water of Jurassic sediments is characterised with low water bearing, flow of water points is not more than 1 litre per second. Water mineralization - 0,5-48 g/l, content - sulphate-carbonate, calcic-sodium and chloride-sulphate sodium, water temperature at the depth of 300-620m is 46,5⁰C.

Cretaceous water bearing complex is stripped at the depth of 100-600m. Fresh water is developed in the area of the Koshobin uplift. With deeper subsidence in western direction, water mineralization is increasing up to 30-40 g/l, and at the Adgeshir structure at northern slope of pre-Balkhan trough mineralization reaches 70-80g/l. Upper Cretaceous carbonaceous deposits to the south-east of the Karabogazgol gulf contain poorly mineralised water, which discharges to the surface in a number of low flow springs. In western direction water mineralization increases to 70 g/l in the south of the gulf and up to 90-100 g/l at southern Karabogazgol spit.

In Quaternary deposits, fresh and salt water is found in preluvial deposits of Major Balkhan and in wind-blown sands of Tuakyr. The most interesting here are the takyrs, which are often associated with the biggest lens of fresh water, occurring at the depth up to 10m.

West-Turkmen artesian basin includes western slopes of Kopetdag, western slopes of Minor Balkhan, southern slopes of Major Balkhan and Kubadag, and West-Turkmen basin. Mountains are mainly composed of deposits of Palaeozoic, Triassic, Jurassic, Cretaceous, to lesser extent Paleogene, Neogene and intrusions of Pre-Cambrian granite. The West-Turkmen basin is composed of Mesozoic, Paleogene, Neogene and Quaternary deposits. Kelkor trough, Cis-Balkhan, Urundshurk-Boldag, Gograndag-Okarem zones of uplift and Shakhman trough are distinguished in its texture, according to Neogene complex.

6 water-bearing complexes are distinguished in more recent sedimentary formation of Mesozoic and Cainozoic, in deposits that constitute mountain surrounding of the basin, and eight in sedimentary formations of West-Turkmen basin, representing internal region of its replenishment.

Spring flow in western Kopetdag is from fractions to 5-7 l/s, wells – to 25-40 and sometimes up to 100 l/s. Water is hydrocarbonate, sulphate and chloride. Hydrocarbonate water is usually fresh to 1 g/l, sulphate – 0,4-7,1 g/l, chloride – 10-17 g/l. Water temperature reaches 46⁰C at the depth of 1 100 m. Iodine, bromine, boron, naphthenic acid, lead, zinc, copper, iron, aluminium, barium, etc. were found in mountain water.

The thickness of red-coloured strata of the West-Turkmen basin is about 3 000m. Water-bearing rocks of lower part consist of intercalations of sand, sandstone and silt, occurring amid clay. Water-bearing capacity is low, mineralization of ground waters is quite diverse. Waters with the highest mineralization (202 g/l) occur in the structural highs of Cheleken. Elsewhere mineralization usually doesn’t surpass 40 g/l and increases to 110 g/l only in places. Silt, sand, and sandstone relate to water-bearing rocks of the upper part of the red-coloured strata, clay - occurring amidst refer to water-resisting rocks. Springs, coinciding with them, are as a rule in a fault zone, with water temperature to 60⁰C, and some of them up to 80-90⁰C. Well flow reaches 8-10 l/s, certain – 100-120 g/l. Water mineralization is mainly high – up to 280-290 g/l, water is chloride sodium and sodium-calcic.

Ground and pressure waters were also found in series of Quaternary deposits. The first have developed in marine, alluvial and proalluvial deposits. They occur at the depth of 1-2 m near salinas and up to 80-250 m in an upper part of foothill prolluvial trains. Chloride and chloride-sulphate sodium water with mineralization 25-50 g/l is prevailing in coastal lowland and foothill trains of Minor Balkhan and Western Kopetdag, mineralization increases to 200 g/l in recent Caspian sediments.

Ground water with mineralization 7-10 g/l is found in the delta of the river Atrek, along irrigation canals. Fresh waters are spread in prelluvial deposits of piedmont part of Kopetdag and Major Balkhan.

Pressure water is developed in Balkhan and Khazar deposits. They recharge low flow springs with mineralization to 80-95 g/l and chloride-sodium content at the Cheleken peninsula.

4. Soil types

Significant landscape and relief diversity of the considered territory allows for distinguishing in the coastal zone of Turkmenistan the following natural regions: Southern Usturt, Zauzboy region, Krasnovodsk peninsula, Cis-Balkhan region, Uchtagan and Chilmamedkum, Cheleken peninsula, coastal plain of South-western Turkmenistan, foothill plains of Western Kopetdag and Balkhan ridges, alluvial-delta plains of the river Atrek.

Grey-brown soils developed in Southern Usturt, takyrs and patches of highly gypsiferous soils are distinguished at their background.

Grey-brown soil formed on the eluvium of Sarmatian limestone, which stipulated increased carbonation of ground. Silt thickness at the shores of the Karabogazgol bay is 40-80 cm, a calcareous fractured platform occurs beneath. The thickness of silt layer is increasing to 100-150 cm by moving away from the Karabogazgol scarp. Takyrs are found quite often, especial in eastern part of the zone. Their overall area is not big. The biggest stretches are situated to the north-east and east of Karagbogazgol.

Highly gypsiferous soils are strewn in the near escarpment belt and in eastern part of the region. These are convex, heavily chipped, and densely covered with lichen patches with 15-30 cm in diameter.

Grey-brown typical soils are widely spread in Zauzboy region, particularly between Kaimat and Chagyl sands. These soils are more chipped than in Usturt, thickness of silt ranges from 1 to 2 m, humus content is low. Grey-brown saline soils are strewn in Koimatkyr and to the west of Begirarslan scarps (southern part of Usturt). Sandy arid soils are associated with small sand massifs – Koimat, Chagyl, Tuar and Geokdere (north-eastern part of the studied area). Takyrs are found everywhere, their general area is not big, and there are big stretches of salinas, associated with depressions.

Grey-brown soils have the widest occurrence at the Krasnovodsk peninsula, then sandy arid soils and solonchaks, and takyrs strewn in patches. A belt of grey-brown loamy soils prolongs in the south of the plateau. Texture of surface layers is almost loamy, below – more fine-grained gypsiferous sediments, containing rocky embeddings.

Grey-brown sandy loam occupies a significant extent in the north of the plateau. Silt thickness doesn’t exceed 60-100 cm, below occurs a calcareous platform or conglomerate. These soils differ from the previous with a lighter composition.

Grey-brown saline sandy loam occupies a longitudinally protracted belt in the central part of the plateau. Contour of such soils also identified at the peninsula Omchaly (south of the Karabogazgol gulf). Contour of these soils is less expressed than of others.

Sandy arid soils have developed on ridgy sands of Oktumkum and western end of Chilmamedkum sands. Soil texture is sandy, upper half-meter layer is not salted, with low humus content.

Takyrs are rarely found and are associated with depressions. Coastal solonchaks are situated at the margins of the peninsula and occupy a vast expanse. Poorly fixed and unconsolidated sands are marked in the north and east of Oktukum and at the Caspian coast. Eroded scarps are situated at northern edge of the Krasnovodsk plateau, with a steep face turned toward the Karabogazgol gulf.

Grey and grey-brown soils, takyrs and patches of sandy arid soils have developed in submontane belt of the Major Balkhan range. Grey soils are associated with elevations higher than 250 m at northern and higher than 70 m at southern slopes of mountains. They are highly stony in southern piedmont and less stony – in northern. Accumulations of fine crystallised gypsum are often found at the depth of 40-60 cm. Grey-brown soils occupy a broad belt and shade into similar soils of the Krasnovodsk plateau in the west. The soils are poorly salted, with low humus.

Considerable extents of takyrs are situated in the margins of a plain situate at foothills of Major Balkhan, small patches of takyrs are strewn all over northern edge of the plain. Small spots of sandy arid soils occur at northern plain situated at foothills of Major Balkhan, insignificant massifs are also found at southern one.

Sandy arid and sandy arid crusty highly saline soils are found on sandy massifs of Uchtagan and Chilmamedkum. The first develops under grass cover. The content of clay doesn’t exceed 14%, humus content is low – 0,1-0,4%.

Sandy arid soils are prevailing at the Cheleken peninsula, there are also a lot of saline and clayey desert soils, takyrs cover a small area.

Sandy arid soils develop under grass cover, poorly gypsiferous, insignificantly saline at the depth of 40 cm and below. Sands are mainly middle- and fine-grained. Humus content is low.

Clayey arid soils are found mainly in lowlands. Their surface is bumpy, sometimes covered with sand, humus content is about 0,6%. Takyrs are strewn with separate spots, forming a complex with clayey arid soils.

Soils of the Cis-Caspian plain consist mainly of salinas, alternating with quick and poorly fixed sands. With it, the major part of the area is covered by salinas in southern reaches, and sands - in the north. Patches of takyrs are also found in the area.

Foothill plains and submontane belt of Western Kopetdag and Balkhan ranges have a lot of available arable lands. Takyrs (more than 250 thousand ha) and clayey arid lands (about 100 thousand ha) are prevailing, as well as grey soils (130 thousand ha) located to the east of Meshed sands. Massifs of grey-brown soils (40 thousand ha) are distinguished at southern foothills of Major Balkhan. Soils are mainly composed of sandy loam and light loamy prolluvial sediments, low humus content, low salt content in the first half a meter. Patches of solonchaks are found in different parts of foothill plains, mainly in depressions. Takyrs occupy the lowest reaches of foothill plains and are composed of predominantly layered clayey-loamy prelluvial overburden.

A large massif of grey soil is situated on the Chat plain, between Meshed sands and foothill of Western Kopetdag. Soils are composed of dusty loamy sediments with small interlayers of clay and sandy loam.

Takyrs are spread almost all over within fluvial-delta plain of the river Atrek. There are also solonchaks and separate patches of clayey arid soils. Traces of ancient agriculture are found everywhere.

Takyrs entirely occupy the Misrian plain, up to modern valley of the Atrek, predominantly with heavy texture and with high content of soluble salts. Clayey arid soils are strewn with small patches south of Meshed sands. They are composed of layered, saline loamy overburdens with interlayers of sandy loam.

Remnant solonchaks are situated in north-west of the Misrian plain and are composed of heavy clayey overburdens.

Meadow soils and solonchaks are widespread within the modern delta of the Atrek, meadow-marshy and meadow-takyr soils also occur.

Meadow soils occupy more than a half of the area of the delta. They are composed of stratified saline loamy-clayey overburdens interbeded with sand and sandy loam. Soils are rich with organic matter, humus is up to 2%. Solonchaks are ubiquitous, especially in western part.

Meadow-marshy soils occupy a longitudinal elongated belt in the north of the delta, and meadow-takyr soils occur with separate patches.

5. Land use

Diversity of natural conditions in the coastal zone of Turkmenistan superimpose a significant imprint on land use. Industrial orientation is considerabley manifested in this zone, which is linked to great reserves of hydrocarbon, chemical and other kind of raw materials. Given lack of fresh water, presently the area is distinguished with poor development of farming. Although, irrigate agriculture was developing from II millennium BC in the south-west of Turkmenistan, at the Misrian and Chat plains. A developed irrigation network allowed for watering up to 100 000 ha in certain period. For this purpose was used the water of Atrek-Sumbar system and temporal surface run-off from western slopes of Kopetdag. The total area of available lands in Western Turkmenistan constitutes 13,9m ha of which more than 90% is plain and highland pastures with the different level of water supply.

Natural conditions, particularly forage and water resources, made provision for predomination of grassland farming in agriculture, the main branches of which are karakul and camel husbandry. These directions are particularly representative of northern and southern parts of the studied territory.

The perspectives of further development of farming in the coastal zone are connected with extending the Karakum canal up to south-western reaches of Turkmenistan and land development in Meshed-Misrian plains.

Significant areas of land are allocated for thoroughfares. Side by side with the existing railway Turkmenbashi-Ashgabad, motor roads and pipelines, construction of new lines such as railways Turkmenbashi-Yerashevo (Kazakhstan) and Kazanjik-Benderturkmen (Iran) is underway. Construction of a railway Turkmenbashi-Dashoguz is in the pipeline. Pipelines are of special importance in the transport communication system. The total length of oil pipelines for transportation of oil via the territory of the Balkan province to the city of Turkmenbashi is 475 km. The total length of gas pipelines Khazar (Cheleken) – Belek – Turkmenbashi, Gumdaf - Belek – Centre ans Korpedje – Kurtush (Iran) is more than 4 000 km. There are water pipes, which provide fresh water to the coastal communities and industries: Yaskhan – Balkanabad (Nebitdag) – Jebel – Turkmenbashi, Kazandjik – Balkanabad – Turkmenbashi and Balkanabad – Khazar (Cheleken).

The coastal zone is widely used for recreation. Comfortable spas and resorts were erected in the vicinity of the settlements Avaza, Tarta, Karshi, Bekdash and Khazar.

Summarising the above, we can distinguish the following forms and types of land use:

• Lands, used by industries;
• Lands used for a year-round ranging;
• Arable lands and recently developed lands;
• Irrigated lands in valleys of the rivers Atrek and Sumbar;
• Lands allocated for thoroughfares;
• Recreational areas;
• Sanctuaries; and
• Unutilised lands (dunes, solonchaks, bed rock outcrops).

6. Coastal patterns

It is well known that sea and ocean level fluctuation cause movements of shorelines and result in alteration of geo-morphological processes and lithodynamics of coastal zones. Since the Caspian has been developing with an alternating regime all through its history, the real forecast of geo-morphological changes in a transgressive stage is impossible without knowledge of the previous state, which developed after the last drop of water levels.

Most intense fall of the Caspian water level appear in 1931-1977, when sea level decreased by more than 3 m. This process has significantly influenced on coastal morphology and dynamics. When the sea shrinks, the depth of continental slope and correspondingly the relief forming force of waves diminishes. The coast trends towards accumulative development, since the shrinking sea transports overburdens toward the coast and creates favourable conditions for formation of accumulative forms of relief. Cliffs and scarps vanished and became covered by aggradation terrace. Vast shallow expanses have dried, large bays disappeared (Gasankuli, Mikhaylovskiy, Uzyn-Ada), Dervish island turned to south Cheleken spit, Cheleken island itself united with the mainland.

Swap of regressive regime to transgressive in 1978 lead to alteration of continental slope of the coast and correspondingly of geological and geo-morphological processes. Denudation and abrasive-accumulative forms of relief started to form instead of deposition coasts. Destruction of the coast doesn’t take place on sloping coast, where there is practically no inclination of continental slope, and there weren’t found any traces of accumulation. The shore here is in the state of equilibrium.

Presently, the following coastal types are identified at the Turkmenistan coast:

a) Coast without development of abrasive-accumulative processes.

Such shores are associated with Atrek, Kyzylkum, Kelkor and Balkhan troughs, where the continental slope of the coast is almost horizontal; sea depth in the coastal zone doesn’t exceed 3-10 cm, water energy is entirely dispersed when passing broad shoals. Wave action is insignificant under such conditions and water inundates areas without a clear coastline, with numerous tongues-bays, with wet marshy ground in between. Surface of such areas is almost on the same level with water surface.

Sea encroachment is especially intensive at such a coastal zone. For example, in 1990-1996, the waterfront has moved by 25 km in the Balkhan trough and 7 km in Atrek. If water level rise would continue, the sea would come up to the settlements Gasankuly, Chikishlar, the oil fields Komsomolskoye and Goturtepe would be partially flooded. Ground water level also rises with sea invasion, which creates favourable conditions for overgrowth of the coastal zone with rush and other vegetation.

b) Deposition coast

Deposition coast coincides with subsidence of anticlinal structures of Gograndag-Okarem, Cis-Balkhan and Darjan uplift zones and with east Cheleken trough (between Cheleken and Goturtepe-Barsagelmes uplifts). Loose eolian rocks, which formed during sea regression, are spread in these areas. Underwater coast has a gentle slope and a little depth. Water energy doesn’t entirely wasted for floor friction and though this water can’t cause any destruction, it moves sandy (eolian and indigenous) particles, removing roughness of the relief and forming aggradation terraces and beaches. These forms also exist in lagoons and bays, protected from the impact of sea waves-breakers, though the continental slope has enough inclination to erode the coast. Formation of coastal spits and bars is not observed yet. Sea encroachment over the land is less intensive than in the previous type of the coast.

c) Abrasive coast

Abrasive coast coincides with limb and periclinal parts of large anticlinal structures – Okarem, Kamyshldja, Cheleken and with outcrops of rocky bedrock, which earlier had decadent or active cliffs. At such stretches, the coast is deep with considerable incline. In these conditions, wave energy consumption occurs at short distance immediate to the shore and waves themselves can cause destruction, though this kind of destruction is different at different stretches of the coast.

At Okarem-Kamyshldja extent, the continental coastal slope, which is composed of Quaternary rocks, was altered by abrasion and the coastline gradually moves eastward, towards indigenous coast that used to be a cliff. The sea still forms a lagoon, separated from the open basin by big above-water and underwater coastal bars, at the foothill of the cliff. The above-water bar is always modified by waves-breakers and pushed inland. It has moved for 30 m from 1990 to 1996.

The height of the decadent cliff is gradually reducing in the north of the settlement Prichal and it sinks under Recent Caspian sands at the latitude of the mud volcano Gokpatlauk, then it emerges again in form of small elevation (1,5-2 m) in far western leg of the Kamyshlja structure. Development of the coast is similar to that of Okarem, but in 4-5 km north of the settlement Prichal, the sea undermines its indigenous coast.

The sea began to undermine the indigenous coast in the vicinity of western Cheleken in 1993 and cliff formation resumed after a long continental break. Breakers undermine indigenous Upper Pliocene dislocated clayey-sandy rocks and overlying dense clays of the Baku age. The surface of these rocks becomes cracked in the coastal zone, which contributes into collapse-landslide effects. Destruction of the coast is intensive. Breadth of abrasive and collapse-landslide destruction of the coast is 4-6 m, which poses a serious threat for exploitation of coastal wells and other objects.

The sea has not reached the slope of the cliff in the south and north of peri-arch part of the Cheleken anticline. Wave energy is consumed for abrasion of the continental slope of the coast. The size of the destroyed strand in the indicated zones constituted 100-200 m in 1991-1997.

Sea waves undermine the indigenous coast with the numerous outcrops of indigenous stony rocks at the Krasnovodsk peninsula. Formation of mainly underwater cliffs commenced there. Cliff coast is already underwater to the north of the settlement Guvly-Mayak, consolidate Khazar rocks are entirely flooded, due to this abrasive activities of the sea are attenuated. Over Khazar rocks occur a large coastal bar, which was formed in the course of regression of the Caspian. This bar is composed of loose sandstone of the Recent Caspian age. In case sea levels rise further, this bar will be quickly destroyed and the sea will flood the huge salina, located to the east of the bar.

At the extent Bekdash-Omarata, cliff coast formed near the settlement Bekdash, where the sea presently undermines calcareous deposits. Coastal destruction will be more intensive in future. The breadth of the strand, flooded during sea levels rise, constituted 20 m. In case sea level increase for another 1 m, the settlement Bekdash will be partially inundated. The sea also approached to its indigenous coast in the west and north-west of the settlement Omarata. Some cliffs have wholly submerged in water and their development resumed.

Abrasive-accumulative coast is formed within the Krasnovodsk and Karabogaz spits, Turkmenbashi (Krasnovodsk) gulf and peninsula Darja. The continental slope has a sufficient inclination for development of abrasive processes, accumulative forms are produced due to washout of loose deposits by the sea. In many places, bars are formed from abrasive materials and wind processes.

We should note that some new processes – sand hill relief deflation and lessening of rugged topography, are observed in purely eolian relief. It happens mainly in places where sand hills are surrounded by salinas or sand hills are waterlogged up to the fundament. Sand balance of the sand hill relief is disturbed – expenditure surpasses supply. Formation of island and semi-island patches of sand hill sands is typical, this takes place in North Cheleken and South Cheleken gulfs.

7. Geo-morphological features

The studied area is bordering in the north with the plateau Usturt with elevation 100-170 m. Uzboy is a natural border in the south and south-east. Topography of Usturt is determined by the age of bedded plain.

The Miocene bedded plain – elevated extents of anticlinal structures and flat-topped monadnocks, covered with Sarmatian limestone platform. South Mangyshlak plateau and north-eastern Cis-Karabogazgol. South-west of Usturt includes the Krasnovodsk plateau, which has a rolling surface with the altitude 100-150 m and covered with Akchagyl limestone. It relates to Upper Pliocene bedded plain. Post Pliocene Porsykup plateau occupies a syncline with the same name, adjoining in the south-east to the gulf Karabogazgol. Cretaceous deposits are heavily rugged by the network of ravines creeping towards Karabogazgol. The basin of the gulf is a destroyed arch of an anticline. It was formed as an erosional valley in Middle Pliocene, then a salina deflation occurred. In Early Khvalyn period, the Caspian inundated this depression for the first time and Karabogazgol became an open gulf. Formation of spits, which separated the gulf from the sea, refers to Late Khvalyn period.

Kubadag-Balkhan uplift confines Usturt from south-west and is an anticline at the border of crystalline fundament along a deep fault. Major Balkhan – low mountain asymmetric range, steeply pitching in the north with the maximal altitude 1880 m. Commencement of range formation refers to the end of Jurassic and it obtained its final shape by Pliocene. There are traces of sea abrasion in the foothills of the range. Kubadag is north-western continuation of the Kubadag-Balkhan anticline, whose southern limb and axial part are cut by sea abrasion. A scarp with the altitude 220 m is facing the sea in the north of the Turkmenbashi (Krasnovodsk) gulf, its northern side is gently sloping and gradually turns to the Krasnovodsk plateau.

Minor Balkhan – a separate ridge with the length about 30 km and altitude up to 770 m, parted from Major Balkhan and Kopetdag by deep troughs, where the watercourse of the pro-Amu Darya lied in past from lowland Karakum to Cis-Caspian lowland. Northern slope of the ridge is composed of dense Cretaceous limestone, a 600 m scarp pitches into a narrow submontane plain. Southern slope is gently sloping and consists of several ridges asymmetric to the range. The ridges are composed of sloping layers of dense and loose Cretaceous and Tertiary clay-marl and gypsiferous clays and are heavily rugged by a net of deep ravines, a clayey karst is widespread. There are several abrasive and aggradation terraces of the Khvalyn Sea at western limb of the range.

Cis-Caspian marine aggradation plain is a southern part of the Turkmenistan coastal zone. It is covered with marine sediments. The Akchagyl transgression, which invaded deep into Karakum, left terraces at the altitude of 90 m. The Baku terraces lie at the altitude of 62 m. The peninsula Dardja is formed of sands, which accumulated in the Khazar period at the extent between Aktam (lower reaches of Uzboy) and the Turkmenbashi gulf.

The Khvalyn Sea flooded the Karabogazgol basin and extended it with help of abrasion between Major Balkhan and Kopetdag, moved deep inland till western Karakum, up to the longitude of Kyzyl-Arvat and approached to western foothills of Kopetdag, where it left coastal bars and marine terraces at the altitude of –16, +48 m. At the Krasnovodsk peninsula, the sea accumulated the presently fixed sand massif Barsa-Gelmes, inundated the flat clayey prolluvial-estuarine Misrian plain.

Karabogaz and Cheleken spits, surfaces of the Cheleken strait and Kelkor salina, waterlogged Atrek plain, where the main role played not deltaic bottomset deposits of the Atrek but sandy-silty marine sediments, were formed in present shape in Holocene during the Recent Caspian transgression.

Isolated eminencies of brachi-anticlinal folds are distinguished at the aggradation plain. Sandy ridges, with the height of 30-40 m at the massif Barsa-Gelmes, stretching from the north to the south sometimes for scores of kilometres, are divided by salinas, which are 1-2 km across.

Mud volcanoes are numerous in the south of the Cis-Caspian plain that tells of presence of oil in the area. A group of coniform hills of Kainak, located at the distance of 5 km from the settlement Gasankuly, continually emits gas and dense mud. The diameter of one of the volcanoes of the Keymir coniform hills reaches 85 m. Presently extinct volcano Gograndag has the altitude of 107 m above the Caspian.

8. Evolution of coastal landscapes

Evolution or alteration of Caspian coastal landscapes wholly depends on climatic conditions of the region, water level fluctuations, rates and methods of exploration and extraction of hydrocarbons and economical land use. The current changes in landscapes occurs on the background of water level fluctuations, economical and technogenic influence on the environment.

The main coastal landscapes can be seen as follows.

Rock debris and gypsiferous plateaux are spread in the north and north-east. These are large arid-denudation tablelands, laying at the altitude from 100 to 350 m. Erosion and tectonic relief of low mountains has developed in places, where folded Mesozoic basement crops out and is partially destroyed by erosion. Processes of water erosion and slight deterioration of the vegetative cover occur at the territories of Kendirly-Kasan, Usturt, Yaniel, Krasnovodsk plateaux. Rainfalls cause rill washout with the depth of 0,3 m. Evolution of the named landscapes happens very slowly and is manifested in gradual substitution of the vegetative cover, deterioration of rangeland.

Sandy plains cover vast expanses of the Caspian coast. Landscapes of Chilmamedkum, Kumsebmesh, Meshedkum sands and sands of western part of lowlands Karakum consist of fixed inland sand massifs. The main reasons of landscape alteration are caused by human activities – grazing, road and pipeline construction, tree and shrub felling. Extension of deflation areas is the ramification of these activities.

Landscapes of coastal marine sands consist of accumulative Upper Pleistocene sodded and half-sodded sands with ridgy, cellular and alveolate relief. Weak area deflation occurs on Recent Caspian and modern sandy surfaces, blanketed with shells and pebble.

Landscapes of drift sands occupy a considerable area in the central part of coastal zone – the Cheleken peninsula. They consist of massifs of bare sands in combination with solonchaks. As a result of a water level rise, the area covered by solonchaks increases and in lower areas they turn to salinas.

Eastern and north-eastern part of the territory consists of landscapes of clayey plains. The plains are flat, poorly undulating, with slope to the west. Processes of weak water erosion, which are manifested in insignificant growth of actual erosive gullies under downpours, are observed there. Landscapes are changing insignificantly.

Landscapes of riparian-marshy complexes occupy southern flat stretches of the modern delta of the river Atrek with monadnocks and hill of Khvalyn period. The main reason of evolution of this landscape is agricultural development of estuarine lands, which resulted in salinization and waterlogging of soils.

Mountain landscapes are represented with Major and Minor Balkhan and Western Kopetdag. Major Balkhan is characterised with steep cliff slopes and stony taluses. Badlands are the main feature of Minor Balkhan. Low mountain edge of Western Kopetdag are characterised with losses sandy-clayey sediments. Processes of weak and moderate erosion, manifested in formation of rain rills, growth of erosive gullies. Often uncontrolled livestock ranging leads to deterioration of the vegetative cover.

Eastern and southern reaches of the Balkan bay, south-east of North Cheleken bay, northern part of South-Cheleken bay refer to most marshy areas at the Turkmenistan coast. Vicinity of the settlement Esenguly also can be referred to marshes. Water level fluctuations have a great impact due to insignificant inclination of south-eastern coast of the Caspian Sea, and they can lead to bogging of new areas. Flooding and waterlogging causes additional pollution of surface and ground waters with toxic matters and oil products, fosters soil salinization and development of hydromorphic vegetation, deteriorates the quality of supplied water and increases sources of infectious diseases.

9. Climate

Climate formation, in the considered region and over the coast of the Caspian Sea, is conditioned by geographic location of the sea, conditions of atmospheric circulation, features of underlying surface and coastal orography. All these makes provision for large influx of solar radiation, high air temperatures, considerable humidity and low precipitation.

Meteorological conditions of south-eastern Caspian are quite different from the rest of the sea. North-western winds are prevailing in wintertime and south-eastern with predominating wind velocity not less than 10 m/s in summertime. Recurrence of gales and storms doesn’t exceed 1% in the south, and increases northward to 5-10%.

The average annual air pressure constitutes 1014 hPa in the south-east of the Caspian and increases northward to 1018 hPa.

The average annual air temperature varies from 15.8⁰C in the south of Turkmenistan to 13.6⁰C in the north. The high monthly temperature is 27⁰C throughout Turkmenistan coast, in the same time the low in the north constitutes 0.9⁰C and in the south - 4⁰C.

The absolute maximal value of air temperature is observed in Gasan-Kuli and Turkmenbashi and constitutes 45⁰C. The minimal both in the north and in the south - - 18⁰C.

Rainfall distribution in the studied area is uneven and increases southward. For instance, the annual rainfall in average constitutes 95 mm in Karabogazgol and 196 mm in Gasan-Kuli.

High air temperatures, droughts, hot dry winds, sandstorms and fogs relate to dangerous meteorological phenomena that are observed at the territory of the Turkmenistan coast of the Caspian Sea.

Based on the main meteorological figures for coastal points given below in Tables 1-6, one can see that northern winds are prevailing at the Turkmenistan coast. In the warm period of a year, the average wind velocity is higher than in the cold period. In the same time the maximal force of wind gusts is observed in wintertime.

The annual rainfall constitutes 70-80 mm in middle and northern stretches of the coast and 213 mm in the south. Fluctuation of rainfall from a year to a year can be considerable. For example, 78 mm of rainfalls was observed in Turkmenbashi in July, under the norm of 4 mm. However, at large such fluctuations are rare and they don’t influence on climate dryness.

The investigated extent of the coast is exposed to prolonged solar radiance. With it all, the total run of solar radiance at the Turkmenbashi bay is a bit higher that to the north and south of the area. Days with entirely gloomy weather aren’t observed in the warm period of a year, and the average monthly duration of solar radiance varies from 120 hours in winter to 380 hours in summer.

The maximal recorded temperature is 45⁰C, in the same time the minimal temperature constitutes - 22⁰C, which indicates the influence of continental inner regions to coastal. The hottest months are July and August and the coldest – January and February.

The humidity, due to close location of the sea, can reach 90%, however it can lower below 30% under eastern, offshore winds.

Table 1. Recurrence of wind directions (%)

Table 2. Average monthly, yearly and maximal wind velocity (m/sec).

Table 3. Monthly and yearly rainfall, mm

Table 4. Duration of solar radiance (hours) and number of overcast days

Table 5. Average monthly and extreme air temperatures, ⁰

Table 6. Average monthly and yearly humidity (%)

10. Description of hydrological network and water resources

The considered area is ascribed with lack of permanent surface flows and reservoirs in the coastal zone. Surface run-off is sometimes observed after rainfalls on a temporal network, which only formed on slopes of plateaux and separate eminencies, where. In general, there are practically no sources of fresh water in the area, this fact contributes certain difficulties to its development.

Riverine drainage of the Turkmenistan coast is represented with only one river, which flows into the sea. However, due to intense water intake for irrigation and fisheries, river run-off is extremely insignificant and water can reach the sea only during freshets. Mountain part of the basin, which is the watershed, constitutes 27 300 km², of these 20 000 km² lies at the territory of Iran. The length of the river is 669 km.

The watershed of the river Atrek is located in the Kopetdag mountain range with the maximal altitude 3 060m. The average altitude of the watershed is 1210 m. The main replenishment of the river is from melting snow and rains. Distribution of impermeable rocks in the watershed of the Atrek and often intense rains make provision for several short-term freshets, bar the main vernal freshet. Often their maximal discharges surpass that of the spring one. Ground and return waters play an important role in replenishment of the river during the low water period.

The average yearly discharge of the Gyzyl-Atrek is 8,6 m³/s, the maximal average yearly discharge reached 23,2 m³/s, the least discharge means that the river runs dry. The maximal observed discharge was 1 440 m³/s.

Three clear water reservoirs were erected in the lower reaches of the Atrek – Kyzyl-Ay, Delely and Mamedkul with the total capacity of 24m m³. The water from the Atrek is also used for filling a spawning ground with water. Fish can reach this spawning ground from the fishway Adji-yab with the throughput capacity of 1 m³/s. Both the water reservoir and spawning ground are filled with water in Spring, in low water years they may not be filled with water. The stream is not controlled in high water years and allowed for freely flowing into the sea.

The water in the Atrek is with high mineralization and in normal water periods can reach 8-10 thousands mg/l. Mineralization lowers to 1 000 mg/l during freshets.

The river Atrek is one of the most turbid rivers in Turkmenistan. The water turbidity under freshets can exceed 200 kg/m³. Due to insignificant and unevenly distributed during a year run-off, the river doesn’t have an expressed delta.

Except for the river Atrek, water from temporal watercourses, which are formed during rainfalls, also can reach the sea. They are found on the Cheleken peninsula, in the north of the Krasnovodsk bay and in the vicinity of Bekdash. However, their contribution is insignificant due to low rainfalls.

Uzboy, which is an ancient riverbed of the river Amu Darya, is of interest. The watercourse of Uzboy is quite well expressed and flows into the Balkan bay. Although, at present it is dry, it was certainly the largest stream in the east of the Caspian Sea.

11. Description of air qualities and sources of pollution

Water quality in the Caspian deteriorates because of a wide range of contaminants entering the sea directly or indirectly. Indirect pollution occurs through the atmosphere. Many industries, processing oil-chemical and other raw materials, emit considerable amount of air contaminants, which in the long run precipitate with rainfalls on sea or land, from where they flow into the sea.

Automobile transport, oil industry, oil-chemical and gas industries and power plants, which burn a lot of different fuels, are the main polluters. Content of combustion products include also such a detrimental components as nitrogen oxide, dioxide of sulphur, carbon black, dust and hydrocarbons.

Emissions of pollutants into the atmosphere from point sources constituted 884,9 thousand tons in 1998 and increased by 79% in comparison with 1995. The number of sources of pollution in the Balkan province is 1891, including organised – 1535. Altogether, 1318 thousand tons of pollution was discharged in the Balkan province. More than 91% of national discharges relates to the Balkan province.

Increase of pollution emissions happened mainly in 1998 due to exploration of the new field Eastern Khazar in the Balkan province – oil and gas production department “Goturtepe”. Majority of polluting industries is equipped with scrubbers and dust traps. These are the Turkmenbashi refinery and chemical plants in Khazar and Balkanabad. Results of the measurements that were carried out in 1998 showed the average yearly concentration of dioxide of sulphur in the city of Turkmenbashi – 4,6 MPC (maximum – 11,8 MPC).

The city of Turkmenbashi has a large airport with a landing strip that can receive all types of aircraft. In the prospect, Turkmenbashi airport can become a venue, where plains, flying from Europe to Asian countries, can land for refuelling and technical services, this inevitably will lead to an increase in air pollution. Currently, there is no control over emissions from air transport flying over the sea.

According to data of the Research-production centre for environmental monitoring of the Ministry of Nature Protection of Turkmenistan (table 7), the average annual content of major pollutants in the air in Turkmenbashi in 1997 reached the figures provided below (average daily maximum permissible concentrations of pollutants are given for comparison, mg/m³).

Table 7. Content of contaminants in the air for 1998

The biggest air polluters are the Turkmenbashi Thermoelectric Power Plant and Turkmenbashi oil-refinery and Carbon Black plant in the city of Khazar (Cheleken). Presently, a vacuum oil processing installation was introduced at the Oil Refinery. This resulted in considerable reduction of emissions.

12. Sea hydrology

12.1 Sea levels

Water level fluctuations significantly influences on the coastal communities in connection with regular flooding and drying, and corresponding changes in the ambient environment. Periods of sea level equilibrium, fall and rise were observed in this century.

From the beginning of the century (1900-1929), water level fluctuations occurred around the average altitude of – 26,2 m within 0,5 m. High sea levels and its relative stability were due to favourable climatic conditions under predominating western form of circulation, that determines high water in rivers and relative balance between water inputs into the sea and its outputs. Riverine run-off for this period considerably surpassed the norm of 1900-1996 (approximately 300 km³ per year) and was 332 km³ per annum.

The run of relatively stable water balance supplanted in 30s with the run of its deficiency. Rate of evaporation increased, low water in rivers determined drop in riverine inflow. As a result, a sharp fall of the level of the Caspian by 1,8 m happened in this period. In the same time, sea area reduced by more than 25 thousands km², water volume by 800 km³.

Dry 30s were replaced with a wet period in 40-60s, which resulted in lowering of sea level decrease to about 2 cm per year. Some stabilisation of sea levels at the level of – 28,4 m was observed in 60s, nevertheless its level lowered by 0,6 m in this period. It was explained by water intake for filling reservoirs and for irrigation of newly developed lands.

The rate of the water level fall increased again in 1970, which ensued with a fall till 1978 to the lowest level (-29m) observed during the period of instrumental observations. This happened as a result of the sharp plunge of river run-off, which reached the lowest values in this century – 240 km³ per year. The rate of evaporation constituted in average 1040 mm per year and significantly exceeded the norm (990 mm per year). The rate of yearly sea level fall in this period measured up to 8 cm.

The run of positive seawater balance and increase of its sea levels has been observed from 1978 up to date. In 1996, the sea level reached – 26,6 m, which followed by lowering and presently it levelled off at – 27,4 m.

Of course we should take into consideration the presence of the Karabogazgol gulf at the Turkmenistan coast. Given its morphological features, it is the most suitable regulator of the Caspian Sea levels. In order to prevent further lowering of the sea levels, the straight connecting the sea with the gulf was blocked with a solid ground dike. As a result, the gulf had completely dried by 1984. In the same time, the sea level was rising from 1978. The ceased water inflow into the gulf resulted in additional rise of the sea level by 2-3 cm per year. A conduit was built in 1984 for 66 m³/s, which allowed for filling of the basin by 3-3,5 km³. In this state the gulf remained till 1992, where the solid dike was opened and the gulf started to fill and by 1996 obtained its present contours.

The gulf has shrunk in connection with the observed fall of the Caspian water level. If the maximal water level in the gulf measured up to – 27,6 m in 1996, by 2000 it had not surpassed – 27,6 m. According to opinion of the Turkmenhydromet, the direct hydraulic relationship between the Caspian and Karabogazgol will be observed till the altitude of the sea level about – 28 m.

12.2 Water temperature

Water temperature variations reflect air temperature variations. The peak values coincide with July-August, the minimal with wintertime (table 8). Water temperature in the Karabogazgol gulf is a bit different from the water temperature in the open sea due to shallowness and limited water exchange with major water masses. For instance, during the warm period of the year, the water in the gulf is warmer by 5-6⁰C, than in the sea and in wintertime it is lower by 2-3⁰C.

Table 8. Average monthly and extreme water temperatures in Turkmenbashi, ⁰C

12.3 Salt content and type of seawater pollution.

Salt content of water is characterised by relative permanence. Errors happening in the course of seawater analyses and non-compliance of sampling rules can explain comparatively insignificant spread of proportions of different ions (table 9). In general, chlorine, sulphate and sodium ions were prevailing in the waters of the Turkmenbashi gulf that is representative of the Caspian Sea at large. In spite of being an enclosed body, there is a high content of oxygen in the gulf waters, which favourably fosters to development of marine organisms.

Table 9. Chemical composition of seawater, 1998

The main polluters of the Caspian at the Turkmenistan coast are oil and oil-chemical industries, communal utilities and water transport.

According to data of the Ministry of Nature Protection of Turkmenistan, the main contribution into the coastal pollution with industrial and household effluents of the studied area is made by:

• Tukmenbashi oil refinery;
• Thermoelectric Power Plant;
• Bureau “Vodokanal”;
• Association “Balkanbalyk”;
• Turkmen shipping company;
• Oil handling terminal in the settlement Urfa;
• State railways;
• Khazar plant for technical carbon;
• Bureau “Cheleken-neft”;
• Balkanabad iodine plant; and
• Bureau Turkmendemiryellari (railways).

Although, there were no evidences of increasing pollution at the Turkmenistan coast of the Caspian during last years, the state of the sea and of coastal protected strand gives rise to concerns. These concerns are linked to existing problems with technologies of drilling and exploitation of offshore oil and gas wells, production waste management and provision with necessary modern equipment.

Content of contaminants along eastern coast of the Caspian Sea has not significantly changed during the last three years. Pollution with oil products ranges from 1 MPC to 3 MPC (0,05-0,15 mg/l), phenols from 1 MPC to 3 MPC (0,001-0,003 mg/l).

Problems of environmental management and pollution prevention of the Caspian Sea doesn’t involve only economical interests, but also the main factor ensuring environmental health of the cities, districts and provinces.

Based on modern requirements to water management, the main goal of industries is to maximally reduce consumption of fresh water, lower the volume of produced wastewater and their contamination and increase efficiency of wastewater treatment plants.

Sanitary and epidemiological stations carry out laboratory studies of Turkmenistan coastal waters. The main attention is paid to visual sings: presence of oil slicks, floaters and suspensions. 363 sanitary-chemical and 345 bacteriological investigations were carried out in 1997. Results of bacteriological investigations showed that the maximal microbial contamination occurs mainly along the waterfront and to the biggest extent around outfalls of municipal sewers. Of 345 samples – 36 (10,4%) didn’t comply with standards.

Of 363 sanitary-chemical analyses – 38 were taken to study smell (normal), transparency - 38 (normal), suspended matters - 38 (normal), dissolved oxygen 38 (normal), BPK5 - 38 (7 samples didn’t comply with the norm), hardness - 38 (normal), water oxidation susceptibility – 38 (8 samples weren’t normal), chlorides - 2 (normal), oil products – 28 samples (24 samples didn’t comply with the norm), detergents – 7 (normal).

SECTION 1

SECTION 2

SECTION 3

SECTION 4