Physical map of the Japanese Sea. Tuting and tidal flows
And the Japanese islands are turns that are separated by the water of the Japanese Sea from the Pacific. The Japanese sea mainly has natural boundaries, only some areas are separated by conventional lines. The Japanese Sea, although it is the smallest of the Far Eastern seas, belongs to the largest. The area of \u200b\u200bthe water surface is 1062 thousand km2, at the volume of water about 1630 thousand km3. The depth of the Japanese sea on average is 1535 m, the maximum depth is 3699 m. This sea refers to the outskirts of the ocean seas.
A small number of rivers carry their waters to the Japanese Sea. SAME large rivers Are: ore, samarga, partisan and tumnin. Mostly all this. During the year, about 210 km 3. In continuation of the year, freshwater evenly enters the sea. In July, the fullness of rivers reaches its maximum. Between and the quiet ocean, water exchange is carried out only in the upper layers.
The extreme southern of Russian Far Easterns - lies between the mainland of Asia and the Korea peninsula, and the Japanese separating it from other Pacific seas and the Ocean itself.
In the Japanese Sea, natural frontiers prevail, but in separate areas it is limited to conditional lines.
In the north, the border between the Japanese and Okhotsk seas is held along the line of the village of Sostva - M. Tyk.
In the strait of the lapere, the line is the line m. Krölon - m. Soy. In the Sangar Strait, the border goes along the line m. Syria - M. Esan, and in the Korean Strait along the line M. Nomo (about. Kyushu) - m. Fukae (about. Goto) - Oh. Chechzhudo - Korean Peninsula.
In these borders, the sea is concluded between the parallels of 51 ° 45 'and 34 ° 26' p. sh. and meridians 127 ° 20 'and 142 ° 15' in. d.
The configuration is characterized by a high length of meridian, expansion in the central and southern parts and the impression in the north.
I gave way to Bering and Okhotsk, the Japanese Sea refers to the largest and in-depth seas of our country. Its area is 1062 thousand km2, the volume is 1630 thousand km3, the average depth of 1535 m, the highest depth of 3699 m.
Geographical position and predominantly large depths point to the belonging of the Japanese Sea to the oceanic seas.
Large islands in no. Of the minor, the most significant islands: Moneron, Ribun, Risiri, Okusiri, Oshima, Sado, Okosimima, Ullyndo, Askold, Russian, Putitin. In the Korean Strait are located the islands of Tsushima. All islands, except Ullyndo, are near the shores. Most of the islands are located in the eastern part of the sea.
bay Head Japanese Sea 
GENERAL INFORMATION -
Japanese Sea (Yap. 日本 海 Niercay, Cor. 동해 Tream, "East Sea") - the sea as part of the Pacific Ocean, separated from him by the Japanese Islands and. By origin is a deep-water pseudo-sassous intra-oil depression associated with other seas and the quiet ocean through 4 Strait: Korean (TsUsimsky), Sangar (Tsguar), Laperose (Soya), Nevelsky (Mamia). Washes the shores of Russia, Japan, the Republic of Korea and the DPRK.
In the south comes the branch of the warm current of Kurosio.
cape Bruce Japanese Sea 
CLIMATE
The climate is moderate, monsoon. The north and western parts of the sea are much colder than southern and eastern. During the coldest months (January-February), the average air temperature in the northern part of the sea is about -20 ° C, and in the south about +5 ° C. Summer monsoon brings with her warm and wet air. average temperature Air of the warmer month (August) in the northern part of approximately +15 ° C, in the southern regions about +25 ° C. In the fall, the number of typhoons caused by hurricane winds increases. The largest waves have a height of 8-10 m, and with typhoons, maximum waves reach a height of 12 m.
Flow
Surface flows form a circuit, which consists of a warm Tsushimsky flow in the East and Cold Primorsky in the West. In winter, the temperature of surface waters from -1-0 ° C in the north and northwest rises to + 10- + 14 ° C in the south and south-east. Spring heating entails a fairly rapid increase in water temperature throughout the sea. In summer, the water temperature on the surface rises from 18-20 ° C in the north to 25-27 ° C in the south of the sea.
The vertical distribution of temperature is not the same in different seasons in different parts of the sea. In the summer in the northern regions of the sea, the temperature of 18-10 ° C holds in a layer of 10-15 m, then it dramatically decreases to +4 ° C on the horizon 50 m and, starting with depths 250 m, the temperature remains constant about +1 ° C. In the central and southern parts of the sea, the water temperature is quite smoothly decreased with a depth and on the horizon 200 m reaches the values \u200b\u200bof +6 ° C, starting with depths 250 m, the temperature is kept about 0 ° C.
The saltness of the water of the Japanese Sea is 33.7-34.3, which is somewhat lower than the saline of the world's ocean.
Tides in the Japanese Sea are pronounced, to a greater or lesser extent in various districts. The greatest level fluctuations are noted in the extreme northern and extreme southern regions. Seasonal fluctuations in the sea level occur simultaneously over the entire surface of the sea, the maximum level rise is observed in the summer.
rudnevo Bay Japanese Sea 
Ice setting
At ice conditions can be divided into three areas: the Tatar strait, the area along the coast of Primorye from the Cape of the Rotary to Cape Belkina and the Bay of Peter the Great. In winter, the ice is constantly observed only in the Tatar Strait and the Gulf of Peter the Great, on the rest of the water area, with the exception of closed bays and bays in the north-western part of the sea, it is not always formed.
The coldest district is the Tatar Strait, where more than 90% of all ice observed in the sea is formed in the winter season. According to many years of this data, the duration of the ice period in the Gulf of Peter the Great is 120 days, and in the Tatar Strait - from 40-80 days in the southern part of the Strait, up to 140-170 days in its northern part.
The first appearance of ice occurs in the tops of the bays and bays closed from the wind, excitement and having a desalinated surface layer. In moderate winters in the Gulf of Peter the Great, the first ice is formed in the second decade of November, and in the Tatar Strait, in the tops of the bays, the Soviet harbor, Chihachev and the Priolava of Nevelsky, the primary forms of ice are observed in early November. Early glare in the Gulf of Peter the Great (Amur Bay) comes early in November, in the Tatar Strait - in the second half of October. Later - at the end of November.
In early December, the development of ice cover along occurs faster than near the mainland shore. Accordingly, in the eastern part of the Tatar Strait at this time of ice more than in Western. By the end of December, the amount of ice in the eastern and western parts is aligned, and after reaching the parallels of Cape Surkum, the direction of the edge changes: its shift along the Sakhalin coast slows down, and along the mainland - is activated.
In the Japanese Sea of \u200b\u200bIce Pokrov reaches maximum development in mid-February. In medium ice, 52% of the area of \u200b\u200bthe Tatar Strait and 56% of Peter the Great Bay are covered.
The melting of ice begins in the first half of March. In mid-March, open water areas of Peter Great Bay and all are cleared of ice seaside coast Cape golden. The boundary of the ice cover in the Tatar Strait retreats to the north-west, and in the eastern part of the Strait at this time there is purification from ice. Early cleansing of the sea from ice comes in the second decade of April, later - in late May - early June.
FLORA AND FAUNA
The underwater world of the northern and southern regions is very different. In the cold northern and northwestern regions, Flora and the fauna of moderate latitudes were formed, and in the southern part of the sea, south of Vladivostok, the thermal faunistic complex prevails. The coast of the Far East has a mixing of heat-water and moderate fauna.
Here you can find octopus and squid - typical representatives warm sea. At the same time, the vertical walls, the scores of the acts, gardens from the brown algae - Laminarium, - all this resembles the landscapes of the White and Barents Sea. In the Japanese Sea, a huge abundance of starfish and marine hero, various color and different sizes, there are worshiors, shrimps, small crabs (Kamchatka crabs are found here only in May, and then they go further into the sea). Bright red ascages live on rocks and stones. Mollusks are the most common scallops. Sea dogs are often found from fish, sea rams.
Sea transport
Major, Nakhodka, East, Soviet harbor, Vanino, Alexandrovsk-Sakhalinsky, Kholmsk, Niigata, Tsuruga, Maizuru, Wonsan, Hynnam, Chhondzh, Busan.
Fisheries; mining crabs, trepagov, algae, sea hedgehogs; Growing scallop.
Recreation and tourism
Since the 1990s, the coast of Primorye begins to actively master the local and visitors.
The impetus was the factors such as the cancellation or simplification of the visit to the borderzon, the rise in prices for passenger traffic in the country, which made too expensive holidays of Far Easterns on the Black Sea coast, as well as a highly increased number of personal vehicles, which made the coast of Primorye for residents of Khabarovsk and the Amur region.
lighthouse Gamova Japanese Sea 
Question about the name of the sea
In South Korea, they call the "Eastern Sea" (Cor. 동해), and in the North - Korean Eastern Sea (Cor. 조선동 해). The Korean side argues that the name "Japanese Sea" was imposed on the world community of the Japanese Empire. The Japanese side, in turn, shows that the name "Japanese Sea" occurs on most cards and is generally accepted.
Straits
Korean Strait - the shed between the Korean Peninsula and Islands of the Japanese archipelago of ICI, Kyushu and the south-west tip of Honshu.
Connects Japanese and East China Sea. The length of the strait is 324 km, the smallest width is 180 km, the smallest depth on the fairway - 73 m. Tsushima island divides the Korean strait to the East (Tsushimsky Strait) and Western Passages. Japanese Sea 
Sangar's shed or shed Tsugaru (Yap. 津軽 海峡 Tsugaru-Kaiko :?) - the shed between the Japanese Islands Honshu and Hokkaido, connects the Japanese Sea with the Pacific Ocean. Strait width 18-110 km, length - 96 km. The depth of the shipping part varies from 110 to 491 m.
In the Strait there are many good anchor parking, but there are no places that are completely closed from the wind. The main flow is directed from the west to the east, the flow rate in the middle of the strait is about 3 knots. Current is often branched to several separate jets, periodically changing their direction. Tides up to 2 m.
Both shores of the mountaineers and forest covered. On the shores of Hokkaido in the Sangar Strait, there is a city of Hakodate - at the beginning of the twentieth century, the location of the Russian consulate and the port, which is most visited by Russian Amur courts. The first map of the Sangar Strait was compiled by the Russian admiral I. F. Kruzhenstern. From the south side of the Strait deep into the land of the south, the bay of the Mutzu is located, where the city of Aomori is located.
In winter, the strait does not freeze. Under the strait, the Tunnel of San is held - before commissioning the Gothar base tunnel, the longest railway tunnel in the world.
The strait of the lapere - the shed between the northern tip of the island of Hokkaido (Japan) and the southern tip of Cape Krylon ( the Russian Federation) connecting the Japanese and Okhotsk Sea.
The length is 94 km, the width in the narrow part of 43 km, the average depth of 20-40 m, the maximum depth of 118 m. In winter, the strait is covered with ice. Named in honor of the French navigator Jean Francois de Laperus, who opened the strait in 1787.
On the Japanese shore of the strait is the port of Vaccanai. In the Strait there is a rocky island of a danger stone.
Unlike the usually declared 12-mile (22 km) area of \u200b\u200bterritorial waters, Japan declares territorial rights in Soya Bay (Sōya) only for the distance of three marine miles from Hokkaido Island (5.5 km). According to the Japanese media report, this rule has been valid since the end of the 1970s in order to pass through the spills of warships and submarine US carrying nuclear weapons, there was no violation of the declared nuclear-free status of Japan. Although earlier some ministers have publicly denied that the zone width was changed for the sake of preserving nuclear-free status.
Strait Nevelsky - the shed between the mainland of Eurasia and. Connects the Tatar Strait with Amur Liman. Length about 56 km, the smallest width is 7.3 km, the depth on the fairway is up to 7.2 m.
Named in honor of G. I. Nevelsky, who opened the strait in 1849.
Under the strait during the reign of Stalin was supposed to build a tunnel.
petrova Island, Singing Sands Bay 
Detailed geography I.
The coastline of the Japanese Sea is relatively weakly cut and does not forms bays and bays, deep-smoking in land, as well as the capes, far speaking in the sea. Most simple on the outlines of more windows of the coast of Primorye and the Japanese islands. The major bays of the mainland shore include: Soviet harbor, Vladimir, Olga, Peter the Great, Postech, East Korean; on about. Hokkaido - Isicari, on about. Honshu - Toyama and Vakas. The most notable seeds - Lazarev, sandy, swivel, Gromov, died, tyk, Korsakov, Krylon, soybean, weepppa, tapping, Nude and some others.
Straits that join the Japanese Sea with the Safety Ocean, the Okhotsk and East-Chinese seas are cut through the coastal line. Straits are different in length, width and main depth, which determines the nature of the water exchange of the Japanese Sea with neighboring pools. Through the Sangar Strait, the Japanese Sea communicates directly with the Pacific Ocean. The depth of the strait in the western part is about 130 m, in the Eastern, where its maximum depths are located - about 400 m. The sheds of Nevelsky connects the Japanese and the Sea of \u200b\u200bOkhotsk. Korean Strait, separated by the islands of Kochzedo, Tsushima and Iki to the Western (the passage of Brouton with the greatest depth of about 12.6 m) and the eastern (the passage of the cruise-seater with the greatest depth of about 110 m), connects the Japanese and East-China Sea. Slim simonycles with depths of about 2-3 m connect Japanese and internal Japanese sea. So small depths of the straits at high depths of the sea are created by the conditions for its morphometric isolation from the Pacific Ocean and the adjacent seas, which represents the most important natural feature of the Japanese Sea.
cape Balcony, Vladimir Bay, Moonlight Night 
A diverse on the structure and external forms of the coast of the Japanese Sea on different sites belongs to various morphometric types of shores. From fig. 42 It can be seen that the abrasion is dominated here, mostly a little changed by the sea of \u200b\u200bthe coast, although the shores have a noticeable stretch; Changed by the sea. To lesser extent, the Japanese sea is characteristic of accumulative shores. This sea is surrounded predominantly mountainous shores. Single rocks (kecura), characteristic of the coast of the coast rise from the water. Lowest shores are found only in separate sections of the coast.
It is difficult and diverse the distribution of depths in the Japanese Sea. By the nature of the bottom relief, it is divided into three parts: North - north of 44 ° C. sh., Central - between 40 and 44 ° C. sh. And South - south of 40 ° C. sh.
The northern part of the sea is as it were a wide chute, gradually narrowing to the north. The bottom of it in the direction from the north to the south forms three steps, which are separated from one other well-pronounced ledges. The north stage is at a depth of 900-1400 m, the average at depths is 1700-2000 m, and the southern at a depth of 2300-2600 m, the surfaces of the steps slightly inclined to the south. The transition from stage to the stage sharply complicates the relief of the bottom.
The coastal shallow of Primorye in the northern part of the sea has a width of 10 to 25 miles, the edge of the scramble is approximately at a depth of about 200 m. The surface of the northern and middle steps of the central gutter is more or less aligned. The relief of the southern stage is significantly complicated by a large number of individual lifts located here - up to 500 m above the bottom surface. Here, on the edge of the southern stage, an extensive elevation of Vityaz is located on the latitude of 44 ° with a minimal depth of it 1086 m. The southern stage of the northern part of the Japanese Sea with a steep ledge breaks down to the bottom of the central brand. The resistance of the ledge is average equal to 10-12 °, in some places 25-30 °, and the height is approximately 800-900 m.
The central part of the sea is a deep closed basin, slightly stretched in the East-northeastern direction. From the West, the North and the East, it is limited to steep ledgers from the slopes of the mountainous facilities of Primorye, Korea, Hokkaido and Honsu Islands, and from the south - the slopes of the underwater elevation of Yamato.
oak Japanese Bay 
For the central part of the sea, a very weak development of coastal shames is characterized. Relatively wide shallow is observed only in the area of \u200b\u200bthe South Primorye. The edge of scratching in the central part of the sea is very clearly expressed. The bottom of the basin, located at depths of about 3,500 m, unlike the complex dismanded surrounding slopes, is completely aligned. On the surface of this plain, individual hills are noted. Approximately in the center of the basin there is an extended ridge from the north to the south, the southern part of the sea is characterized by a very difficult terrain, since the end of the major mountain Systems: Kumilo-Kamchatka, Japanese and Ryuku. The central place here is occupied by the extensive underwater elevation of Yamato, which is two elongated in the East-northeastern direction of the ridge with a closed basin located between them. From the south, the wide underwater ridge stretching in close to the meridional direction from the Oka Islands is adjacent to the Himato Hill.
In many areas of the southern sea, the structure of the underwater slope is complicated by the presence of underwater ridges. On the underwater slope of Korea between the ridges, wide underwater valleys are traced. The continental shallow near Korea almost all over the whole narrow, the width does not exceed 10 miles. In the area of \u200b\u200bKorean Strait, Korea, and Honsel, are closed and form shallow water with depths of no more than 150 m.
The Japanese Sea lies entirely in the monsoon climate zone of moderate latitudes. In this sea, the named climate type is manifested most brightly. However, under the influence of various physico-geographical factors, such as a large meridional and small latitudinal stretch of the sea, the neighborhood of cold Sea Okhotsk In the north and warm ocean in the south, local peculiarities of atmospheric circulation, etc., noticeable climatic differences are formed between different areas of the sea. In particular, the northern and western part of the sea is colder than South and East, in each of them there is a certain nature of the weather.
The synoptic conditions above the sea and the associated meteorological indicators determine the main centers of the atmosphere, the location and interaction of which they vary from the season for the season. In the cold season (from October to March), the sea is influenced by the Siberian anticyclone and the Aleutian minimum, which creates significant horizontal pressure gradients. In this regard, strong northeast winds with rates of 12-15 m / s and more are dominated over the sea. Local conditions change the wind atmosphere. In some areas, under the influence of the coast relief, there is a big repeatability of the northern winds, in others they are often observed. On the southeast coast, the correctness of the monsoon is violated, the Western and Northwestern winds are dominated here.
During the cold season, continental cyclones overlook the Japanese sea. They cause strong storms, and sometimes cruel hurricanes that continue for 2-3 days. At the beginning of the fall (September - October), tropical cyclones are torn over the sea - Typhins, accompanied by hurricane winds. Winter monsoon brings dry and cold air to the Japanese sea, the temperature of which increases from the south to the north and from the west to the east. In the coldest months (January or February), the average monthly air temperature in the north is about -20 °, and in the south of about 5 °, although there are often significant deviations from these quantities. In the cold seasons, dry and clear weather in the north-western part of the sea, wet and cloudy - on his southeast.
The warm seasons in the Japanese Sea applies to the exposure to a Hawaiian maximum and to a lesser degree of depression formerizing in the summer over Eastern Siberia. In this regard, the South and South-Western winds prevail over the sea. However, pressure gradients between the areas of high and low pressure are relatively small, so the wind speed is on average equal to 2-7 m / s. A significant strengthening of the wind is associated with access to the sea of \u200b\u200boceanic, less often continental cyclones. In the summer and early autumn (July - October) over the sea, the amount (with a maximum in August - September) Typhins are increasing, which cause hurricane winds. In addition to the summer monsoon, strong and hurricane winds associated with the passage of cyclones and typhoons, winds of local origin are observed in different parts of the sea. They are mainly due to the features of the orography of the shores and are most sensible in the coastal zone.
Summer monsoon brings with them warm and wet air. The average monthly temperature of the warmest month (August) in the northern part of the sea is approximately 15 °, and in the southern regions about 25 °. In the north-western part of the sea there are significant cooling at styers of cold air, brought by continental cyclones. In spring summer time Cloud weather prevails with frequent fogs. The monsoon type of climate with all its features (wind shifts, weather nature, etc.) is a substantially important natural traity of the Japanese Sea.
Japanese Sea, South Korea 
Another distinctive feature of this sea is a relatively small number of rivers flowing into it. The largest of them is ore, Samarga, partisan, tumnin. Almost all of them are of mountain nature. The mainland stock in the Japanese sea is approximately 210 km3 / year and it is quite evenly distributed by months. Only in July there is a slight increase in the river flow.
The originality of the geographical situation, the outlines and the sea basins separated from the Pacific Ocean and the adjacent seas with high thresholds in the straits, pronounced monsoons, water exchange through the straits only in the upper layers - the main factors for the formation of the hydrological conditions of the Japanese Sea.
Located in moderate latitudes, the Japanese Sea receives a large amount of heat from solar radiation. However, the total heat consumption for effective radiation and evaporation exceeds the flow of solar heat. Consequently, as a result of the processes flowing on the surface of the section of water - air, the sea loses heat annually. It is replenished due to heat, brought by Pacific waters entering the straits in the sea, therefore, in the average long-term significance, the sea is in a state of thermal equilibrium. This indicates a very important role of intra-wheel heat exchange, mainly the inflow of heat from the outside, in the heat balance of the Japanese Sea.
A significant natural factor is the water balance of the sea - it consists of water exchange through the straits, the revenues of atmospheric precipitation on the marine surface and evaporation from it. The main flow of water to the Japanese sea occurs through the Korean Strait - about 97% of the total annual income water. The largest flow of water is carried out through the Sangar Strait - 64% of the total flow; Through the straits of Laperose, Nevelsky and Korean flows 34%. The share of fresh components of the water balance (mainland stock, precipitation and evaporation) remains only about 1%. Thus, the main role in the water balance of the sea is playing water exchange through the straits. In the cold season (from October to April), water consumption exceeds the arrival, and from May to September - on the contrary. The negative value of the water balance in the cold time is caused by the weakening of the receipt of Pacific waters through the Korean Strait, as well as the increase in the flow through the straits of Laperose and Sangar.
Hydrological characteristics.
The effects of marked factors causes the distribution of temperature, salinity and density of water in time and in space, structure and circulation of water of the Japanese Sea.
The features of the temperature distribution of water in the sea are formed under the influence of heat exchange with the atmosphere (this factor prevails in the northern and northwestern regions) and circulation of water, which prevails in the southern and southeastern part of the sea. In general, the temperature of the water on the sea surface rises from the North-West to the southeast, while each season has its own distinctive features.
In winter, the temperature of the water on the surfaces from the negative values \u200b\u200bclose to 0 ° in the north and northwest rises to 10-14 ° in the south and south-east (Fig. 43). For this season, a well-pronounced contrast of water temperature between Western and eastern parts Sea, and in the south, he manifests itself weaker than in the north and in the center of the sea. Thus, on the latitude of the Bay of Peter the Great Several Sea temperature in the West is close to 0 °, and in the east it reaches 5-6 °. This is explained, in particular, the promotion of warm water from the south to the north on the eastern outskirts of the sea.
Spring heating entails a rather rapid increase in the surface temperature of water throughout the sea. At this time, the smoothing of temperature differences between the western and eastern parts of the sea begins. In the summer, the water temperature on the surface rises from 18-20 ° in the north to 25-27 ° in the south of the sea. Changes in latitude are relatively small. Western coast has a water temperature on 1-2 ° lower than the eastern, where warm waters extend from the south to the north.
The vertical temperature distribution is not the same in different seasons in different parts of the Japanese Sea. In winter in the northern and northwestern areas of the sea, the temperature of the water only slightly changes from the surface to the bottom. Its values \u200b\u200bare close to 0.2-0.4 °. In the central, especially southern and southeastern parts of the sea, the change in the water temperature with depth is expressed more noticeable. In general, the surface temperature, equal to 8-10 °, is preserved to the horizons 100-150 m, from which it smoothly decreases with a depth of about 2-4 ° on the horizons 200-250 m, then it drops very slowly to 1.0-1 , 5 ° on horizons 400-500 m, deeper the temperature, somewhat falling (up to a value less than 1 °), remains approximately the same to the bottom.
Spring heating begins to create differences in the temperature vertically in the upper layers, which over time become sharper. In the summer in the north and north-west of the sea, the high surface temperature (18-20 °) is observed in a layer of 0-10-15 m, from here it drops sharply with a depth, reaching 4 ° on the horizon 50 m, further its decrease is very slow to the horizon 250 m, where it is approximately 1 °, deeper and to the bottom, the temperature does not exceed 1 °.
In the central and southern parts of the sea, the temperature is rather smoothly smoothly with a depth and on the horizon 200 m is equal to about 6 °, it drops somewhat cooler and on the horizons 250-260 m reaches 1.5-2.0 °, further its decrease occurs slowly and on the horizons 750-1500 m, in some areas on the horizons 1000-1500 m, it reaches a minimum equal to 0.04-0.14 °, hence the temperature increases to the bottom to the values \u200b\u200bof 0.28-0.26 °, and sometimes and up to 0.33 °. The formation of the intermediate layer of minimal temperature values \u200b\u200bis presumably binding to the immersion cooled in the harsh winter waters of the northwestern part of the sea. This layer is quite stable and is observed all year round.
The average salty of the sea sea, equal to about 34.09, is slightly lower than the same size in the world ocean, which is associated with the insulation of the deep water of the sea from the Pacific Ocean. Under the influence of surface water exchange with adjacent seas and the quiet ocean, precipitation, ice formation and melting of ice, the influx of mainland waters and other factors fold there are certain features of salinity distribution for seasons in various parts of the sea.
In winter, the largest salinity of the surface layer (approximately 34.5) is observed in the south, which is explained by the predominance of evaporation over precipitation here (see Fig. 43, b). The smallest salinity on the surface (about 33.8) is observed along the southeastern and south-west coast of the sea, where some desalination is caused by abundant precipitation. For most of the sea, salinity varies from 34.08 to 34.10. In the springtime, in the north and north-west, the desalination of surface waters is caused by melting ice, and in other areas it is associated with increasing precipitation. Comparatively high (34.60-34.70) salinity remains in the south, where at this time the influx of more salted waters is intensified through the Korean Strait.
In summer, the average salinity on the surface varies from 31.5 ‰ in the north of the Tatar Strait to 34.5 ‰ off the coast. Honshu, where at this time the evaporation prevails over precipitation. In the central and southern areas of the sea, the precipitation significantly exceeds evaporation, which causes desalination of surface waters here. By autumn, the amount of precipitation decreases, the sea begins to cool, in connection with this salinity on the surface increases. Over time, the winter distribution of salinity comes.
The vertical stroke of salinity is characterized in general, relatively small, but different from the season for the season and from the place to the place of change of its values \u200b\u200bin depth. In winter, at most parts of the sea, a homogeneous salinity is observed from the surface to the bottom, equal to about 34.08-34.10 ‰ (see Fig. 43, b). Only in coastal waters, the weakly expressed minimum salinity in the surface horizons is traced, below which salinity increases slightly and then it remains almost the same to the bottom. At this time of the year, the change in the salinity by vertical on most of the sea does not exceed 0.6-0.7, and in its central part does not reach 0.1.
Spring and further desalination of surface waters begins to form the main features of the summer distribution of salinity vertically. In summer, the minimum salinity is observed on the surface as a result of noticeable desalination of surface waters. In the subsurface layers, salinity increases with depth, and noticeable vertical salinity gradients are created, equal to about 0.03 in the north and in the south and about 0.01 in the central part of the sea. Maximum salinity at this time occurs on the horizons of 50-100 m in the northern and southern regions and on the horizons 500-1500 m in the southern. Below the mentioned layers salinity decreases slightly and almost does not change to the bottom, remaining within 33.93-34.13. In summer, the salinity of deep water water 0.1 is lower than in winter. An increase in surface salinity in the fall begins the transition to the winter distribution of salinity vertically.
The density of the water of the Japanese Sea depends mainly on temperature. The highest density in winter, and the lowest - in summer. In the northwestern part of the sea, the density is always higher than in South and Southeast. In winter, the density on the surface is quite homogeneous throughout the sea, especially in its northwestern part. In the southeastern regions, this homogeneity decreases from north to south. In the spring, the homogeneity of the values \u200b\u200bof the surface density is broken due to different heating of the upper layer of water. In the summer, the most highly horizontal differences in the magnitudes of the surface density. They are particularly significant in the field of water mixing with different characteristics. The vertical distribution of the density is characterized in the winter of approximately the same values \u200b\u200bfrom the surface to the bottom in the north-western part of the sea. In the southeastern areas, the density increases slightly on the horizons of 50-100 m, its increase is very increasing to the bottom. Maximum density is marked in March.
island of Reineke, Petra Great Bay
In summer, the change in density with the depth is expressed quite difficult and unequal from the place to the place. In the north-west of water, the density is noticeably percent. It is small on the surface, sharply rises on the horizons 50-100 m, deeper density increases more smoothly. In the southwestern part of the sea, the density increases markedly in the subsurface (up to 50 m) layers, on the horizons 100-150 m it is somewhat homogeneous, below the density is quite smoothly and slightly increases to the bottom. This transition occurs on the horizons 150-200 m in the North-West and on the horizons 300-400 m in the south-east of the sea.
In the fall, the density begins to level out, which means the transition to the Winter type of density distribution with depth. Spring-summer density stratification causes a rather steady state of water of the Japanese Sea, although in different areas it is expressed in varying degrees. In accordance with this, more or less favorable prerequisites are created in the sea for the occurrence and development of mixing.
The predominance of winds of relatively small force and even their significant increase in the passage of cyclones in the conditions of a sharp change of waters in the north and north-west of the sea allows wind stirring to penetrate here to horizons of about 20 m. In less stratified waters of southern and southwestern districts, the wind mixes the upper layers To the horizons 25-30 m. Autumn stability decreases, and the winds are enhanced, but at this time of the year the thickness of the upper homogeneous layer increases due to the density mixing.
Autumn-winter cooling, and in the north and gland formation cause intensive convection in the Japanese Sea. In the northern and northwestern parts of the sea, the rapid autumn cooling of its surface develops a powerful convective mixing, which for a short time covers more and deeper layers. With the beginning of the Introduction, this process is enhanced and in December convection penetrates to the bottom. At large depths, it spreads to the horizon of 2000-3000 m, where it limits the deep Japanese water. In the southern and southeastern areas of the sea, cooled in autumn and in winter to a lesser extent than the said parts of the sea, convection is distributed mainly to the horizons 200 m. In the areas of a sharp change, the depths convection enhances the waters of water in the slopes, as a result of which the density mixing penetrates The horizons of 300-400 m. Below it limits the density structure of water, and the ventilation of the bottom layers is ensured by a combination of turbulence, vertical movements and other dynamic processes.
Features of the distribution of oceanic characteristics along the sea area and with depth, well-developed mixing, the influx of surface waters from adjacent pools and isolation from them deep seawater form the main features of the hydrological structure of the Japanese Sea. The whole thickness of its waters is divided into two zones: superficial (to the depth of average 200 m) and deep (from 200 m to the bottom). The water of the depth zone is characterized by relatively homogeneous physical properties in their entire mass throughout the year. The water of the surface zone under the influence of climatic and hydrological factors changes its characteristics in time and space is much more intense.
In the Japanese Sea, three aquatic masses are distinguished: two in the surface area - the surface Pacific, characteristic of the southeastern part of the sea, and the surface Japanese, peculiar to the north-western part of the sea, and one in the deep zone - the deep Japanese water mass. In terms of its origin, these aquatic masses are the result of the transformation of Pacific waters entering the sea.
The surface Pacific aqueous mass is formed mainly under the influence of the Tsushimsky current, it has the greatest volume in the south and south-east of the sea. As it moves to the north, its thickness and distribution area gradually decrease and approximately around 48 ° C. sh. Due to the sharp decrease in the depths, it is seduced into shallow water. In winter, when the Tsushim Code weakens, the northern border of the Pacific Water is located about 46-47 ° C. sh.
Surface Pacific Water is characterized by high temperature values \u200b\u200b(about 15-20 °) and salinity (34.0-35.5). In the water mass under consideration, several layers are distinguished, the hydrological characteristics of which and the thickness change during the year. Surface layer, where the temperature changes from 10 to 25 ° during the year, and salinity from 33.5 to 34.5. The thickness of the surface layer varies from 10 to 100 m. The upper intermediate layer, the thickness of which changes from 50 to 150 m during the year. It marked significant temperature gradients, salinity and density. The lower layer with a thickness of 100 to 150 m. During the year, the depth of the occurrence, the boundaries of its propagation change, the temperature from 4 to 12 °, salinity from 34.0 to 34.2 ‰. Bottom intermediate layer with very minor vertical temperatures, salinity and density gradients. It separates the surface Pacific Water Mass from the depth Japanese.
winter on the Japanese Sea 
As the Pacific Water moves to North gradually changes its characteristics under the influence of climatic factors and due to stirring it with the underlying deep Japan-water water. As a result of the cooling and collapsion of the Pacific Water on latitudes 46-48 ° C. sh. Surface Japanese aqueous water mass is formed. It is characterized by relatively low temperatures (an average of about 5-8 °) and salinity (32.5-33.5). The whole thickness of this aqueous mass is divided into three layers; Surface, intermediate and deep. As in the Pacific, in the surface Japanese water, the greatest changes in hydrological characteristics occur in the surface layer. The temperature here changes from 0 to 21 ° here, salinity from 32.0-34.0, and a layer thickness from 10 to 150 m and more. In the intermediate and deep layers, seasonal changes in hydrological characteristics are insignificant. Winter Surface Japanese water takes large squareThan in summer, due to intensive receipt to the sea at this time of Pacific Waters.
The deep Japanese water is formed as a result of the transformation of surface waters, descending into depths due to the process of winter convection due to the total cyclonic circulation. Changes in the characteristics of the depth Japanese sea water vertically extremely small. The main mass of these water has a winter temperature of 0.1-0.2 °, in the summer of 0.3-0.5 °; Saltness during the year 34.10-34.15.
The nature of the circulation of the sea is determined not only by the influence of winds acting directly above the sea, but also the circulation of the atmosphere over northern The Pacific Ocean, since the strengthening or weakening of the influx of Pacific waters depends on this circulation. In the summer, the south-eastern monsoon helps to enhance the circulation of sea water due to the receipt of a large amount of water. In winter, the steady northwestern monsoon prevents the flow of water into the sea through the Korean Strait, causing weakening the circulation of water. The impact of the bottom relief is also a great influence on the circulation of the sea.
Through the Korean Strait in the Japanese Sea, the Western Branch of Kurosio and a wide stream applies to the northeast along the Japanese islands. This flow is called the Tsushimsky flow. As a result of the influence of the Relief of the bottom, in particular, the pile of yamato, in the central part of the sea there is a division of the stream of Pacific waters into two branches and the formation of the divergence zone, especially well-pronounced in the summer. In this zone, the rise of deep waters. Having reinforced the hill, both branches are connected in the area located on the north-west from the Noto Peninsula.
On the latitude of 38-3-39 ° from the northern branch of the Tsushimsky flow, a small flow is separated to the West, to the Korean Gulf area and goes into countercase along the Beretov Korea. The removal of the main mass of Pacific waters from the Japanese Sea occurs through the straits of Laperose and Sangan, part of the same waters, reaching the Tatar Strait, gives rise to a cold seaside flow moving south. South Petra Gulf of Great Seaside current turns to the east and merges with the northern branch of the Tsushimsky flow. The insignificant part of the water continues to move south to the Korean Gulf, where it flows into the countercase, formed by the waters of the Tsushimsky flow. Thus, moving along the Japanese islands from the south to the north, along the shores of Primorye from north to south, the water of the Japanese Sea form a cyclonic circulation with a center in the north-western part of the sea. In the center of the cycle is also possible to rise water.
In the Japanese Sea, two areas of front sections are distinguished. The main polar front is formed by the warm and salty waters of the Tsushimsky flow and the cold less salted waters of the seaside flow. The second front is formed by the waters of seaside flow and coastal waters, which in summer have a higher temperature and low salinity than the waters of the seaside flow. In winter, the polar front passes several southerly parallels of 40 ° C. sh., and the Japanese islands front goes almost in parallel to them before the northern tip about. Hokkaido. In the summer, the front is approximately also, slightly shifting to the south, and at the shores of Japan to the West. The second front is located near the coast of Primorye, passing in parallel.
Tides in the Japanese Sea are pronounced quite clearly. They create mainly the Pacific tidal wave. It enters the sea mainly through the Korean and Sangar Strait, it spreads to the northern seas in the sea and in combination with their own tide defines the main features of this phenomenon. In this sea, semi-sufficient, daily and mixed tides are observed. In the Korean Strait and in the north of Tatar - semi-sufficient tides, on eastern Bank Korea, on the coasts of Primorye, Honsu Islands and Hokkaido - Daily, in the Gulf of Peter Great and Korean - mixed.
The character of the tide corresponds to tidal flows and level fluctuations. In the open areas of the sea, hemphisy tidal flows with rates of 10-25 cm / s are mainly manifested. More complex tidal flows in the straits, where they have and very significant speeds. Thus, in the Sangar Strait of the velocity of tidal flows, 100-200 cm / s reaches 100-200 cm, in the strait of the lapere - 50-100 cm / s, in Korean - 40-60 cm / s.
Tidal level fluctuations in different parts of the sea are far from the same. The greatest level fluctuations are noted in the extreme southern and northern areas of the sea. In the southern entrance to the Korean Strait, the magnitude of the tide reaches 3 m. As it moves to the north, it is quickly reduced and the pasta does not exceed 1.5 m. In the middle of the sea, the tides are small. Along the eastern shores of Korea and the Soviet Primorye before the entrance to the Tatar shed, they are not more than 0.5 m. The same magnitude of tides from the Western shores Honshu, Hokkaido and. In the Tatar Strait, the magnitude of the tides of 2.3-2.8 m. The increase in the values \u200b\u200bof the tides in the northern part of the Tatar Strait is due to its funnel-shaped form.
In addition to the tidal in the Japanese Sea, other types of level fluctuations are traced. In particular, its seasonal oscillations are well expressed here. They belong to the monsoon type, as the level is experiencing seasonal changes simultaneous throughout the year throughout the sea water area. In the summer (August-September) there is a maximum rise in the level on all shores of the sea, in winter and early spring (January-April) there is a minimal position of the level.
In the Japanese Sea, there are salaries-niggling level fluctuations. During the Winter Monsoon, the Western Coast of Japan may increase by 20-25 cm, and the mainland shore is to fall on the same value. In the summer, on the contrary, the coast of North Korea and Primorye, the level rises by 20-25 cm, and Japanese coast The same amount decreases.
Strong winds caused by the passage of cyclones and especially typhoons over the sea, develop a very significant excitement, while monsoons cause less strong excitement. In the northwestern part of the sea in the autumn-winter time, northwestern excitement prevails, and in the spring and summer - the eastern directions. Most often, there is an excitement of 1-3 points by force, the repeatability of which changes from 60 to 80% for the year. In winter, strong excitement prevails (6 points or more), the repeatability of which is about 10%. In the southeastern part of the sea, thanks to the sustainable North-West Musson, an excitement from the North-West and the North develops in winter. In summer, the weak, most often south-western excitement. The largest waves have a height of 8-10 m, and with typhoons, maximum waves reach a height of 12 m. In the Japanese Sea, giant tsunami waves were noted.
The north and northwestern parts of the sea adjacent to the mainland shore, annually are covered with ice for 4-5 months, the area of \u200b\u200bwhich occupies about a quarter of the space of the entire sea. The appearance of ice in the Japanese Sea is possible in October, and the last ice is delayed in the north sometimes until mid-June. Thus, the sea completely free from ice is only during the summer months - July, August and September.
The first ice in the sea is formed in closed bays and the bays of the mainland shore, for example, in the Soviet harbor bay, De-Castries and Olga bays. In October-November, Ice Pokrov is mainly developing within the bays and bays, and from the end of November - the beginning of December ice begins to form in the open sea. At the end of December, the Introduction in the coastal and open areas of the sea is distributed to Peter Great Bay. Speak in the Japanese Sea of \u200b\u200bWide Distribution does not have. Previously, it is formed in the Gulf of De-Castries, the Soviet harbor and Olga, in the Bay of Petra Great Bay and wake the digest appears after about a month.
Every year only the northern bays of the mainland coast are completely freezing. To the south of the Soviet harbor, digest in the bays unstable and during the winter can be repeatedly wake up. In the western part of the sea, floating and stationary ice appears earlier than easter, further applies to the south and more stable than the same latitudes in the eastern part of the sea. This is explained by the fact that the western part of the sea in winter is under the prevailing effect of cold and dry air masses spreading from the mainland. In the east of the sea, the influence of these masses weakens significantly, at the same time the role of warm and wet marine masses increases. The greatest development of ice cover reaches around the middle of February. From February to May, conditions conducive to melting ice (on-site) are created to May. In the eastern part of the sea, the melting of ice begins earlier and happens more intense than the same latitudes in the West. The architecturality of the Japanese Sea is experiencing significant changes from year to year. Cases are possible when the Iceer of the One Winter is twice and more exceeds the Iceticity of the other.
Hydrochemical conditions. The natural features of the Japanese Sea and, above all, the explicit of the deep part of its brand from the Pacific Ocean form the distinctive features of the hydrochemical conditions in it. They are primarily manifested in the distribution of oxygen and biogenic substances in the space of the sea and depth. In general, the sea is richly dissolved oxygen. In the western part, its concentration is somewhat larger than in the eastern, which is explained by the reduced water temperature and the relative wealth of the phytoplankton of the Western regions of the sea. The oxygen content decreases with depth. However, for the Japanese Sea, in contrast to the other seas of the Far East, characterized by the high oxygen content (up to 69% saturation) in the bottom waters and the absence of an oxygen minimum in the depth layers. This is due to intense vertical water exchange within the sea itself.
Economic use. For the Japanese Sea, the high development of the two industries of the national economy is characterized: fish with a large variety of fishery and sea transport objects with a developed network of transport. The fish farm combines fishing (Sarddin, Mackerel, Sair and other species) and mining of non-breaking facilities (marine mollusks - mussels, scallops, squid; algae - laminaria, sea cabbage, angellation). "Soviet Union". Although it leads fishery in the Antarctic, but the products enters the fisheries enterprises of Vladivostok. In the Japanese Sea, active work on breeding mariculture has begun - the most promising method of using marine biological resources.
On the shores of the Japanese Sea, in Vladivostok, the Trans-Siberian Highway ends. Here is the most significant transshipment vehicle, where cargo exchange between the railway and sea transport occurs. Further, in the Japanese sea, loads are followed by maritime courts in different foreign and Soviet ports, as they come from other ports in the ports of the Japanese Sea: Soviet harbor, Nakhodka, Vanino, Alexandrovsk-on-Sakhalin, Kholmsk. These ports provide sea transport not only in the Japanese sea, but also beyond. Recently, the Vanino and Kholmsk ports on Sakhalin are bound by an sea ferry crossing that even more strengthened transport role Japanese sea.
Studies in the Japanese Sea are held for a long time, therefore it refers to the most seized seas not only the Far East, but throughout our country. Nevertheless, there are still many not solved problems for all oceanological aspects. With respect to hydrological problems, the most significant: the study of the quantitative characteristics of water exchange through the sheds, the formation of thermohalin conditions in the deep layers of the sea, vertical movements of water, the patterns of ice drift; Development of forecasts of the passage of typhoons and tsunamis. All these are only examples of the main directions for which the Japanese Sea studies will be conducted with the purpose of its further development.
___________________________________________________________________________________________
Source of information and photo:
Social team
http://tapemark.narod.ru/more/18.html
Melnikov A. V. Geographical names of the Far East of Russia: Toponymic Dictionary. - Blagoveshchensk: Interra-Plus (InterRa +), 2009. - 55 s.
Soviets S. A., Japanese Sea // Encyclopedic Dictionary of Brockhaus and Efron: In 86 volumes (82 tons and 4 additional). - St. Petersburg., 1890-1907.
Shamraev Yu. I., Shishkin L. A. Okeanology. L.: Hydrometeoizdat, 1980.
Japanese Sea in the book: A. D. Dobrovolsky, B. S. Zavodin. Sea of \u200b\u200bthe USSR. Publishing House Mosk. University, 1982.
Japanese Sea. Japan Foreign Ministry.
Wikipedia website.
Magidovich I. P., Magidovich V. I. Essays on history geographic discoveries. - Enlightenment, 1985. - T. 4.
http://www.photosight.ru/
Photo: V. Plotnikov, Oleg Slor, A. Marakhovts, A.Shpakat, E. E.Fremov.
Physico-geographical characteristics and hydrometeorological conditions
The Japanese Sea is located in the northwestern part of the Pacific Ocean between the mainland shore of Asia, Japanese Islands and Sakhalin Island in geographic coordinates 34 ° 26 "-51 ° 41" S.Sh., 127 ° 20 "-142 ° 15" V.D. In its physico-geographical position, it refers to the outskirts of the oceanic seas and fell apart from adjacent pools with shallow water barriers. In the North and Northeast, the Japanese Sea connects to the Okhotsk Sea straits Nevelsky and Laperose (Soya), in the East - with the Pacific Ocean of Sangar (Tsguar) by the Strait, in the south, with the East-Chinese Sea Korean (Tsushimsky) Strait. The smallest of them of the Strait - Nevelsky has a maximum depth of 10 m, and the deepest Sangan is about 200 meters. The greatest influence on the hydrological regime of the basin is rendered by subtropical waters entering the Korean shed from the East-China Sea. The width of this strait is 185 km, and the greatest depth of the threshold is 135 m. The second largest water exchange is a Santan Strait, has a width of 19 km. The strait of the lapere, the third largest water exchange, has a width of 44 km, and the depth is up to 50 m. The area of \u200b\u200bthe marine surface mirror is 1062 thousand km 2, and the total volume of the sea is 1631 thousand km 3.
The nature relief DNA The Japanese Sea is divided into three parts: North - north of 44 ° C.Sh., Central - between 40 ° and 44 ° S.Sh. and south - south of 40 ° S.Sh. The surface of the Northern Batymmetric stage, which is a wide gutter, smoothly rising to the north, is merged by 49 ° 30 "S.Sh. with the surface of the Tatar Strait, the bottom of the central part with the depths to the sea (up to 3700 m) has a smooth bottom and elongated From the west to the east, northeast. From the south, its border is determined by the underwater hill of Yamato. The southern part of the sea is the most difficult terrain of the bottom. The main geological note here is the underwater elevation of the Yamato, formed by two stretched in the East-northeast direction by the ridges and located between They are closed with a closed basin. Between the hill of Yamato and the slope of about. Honshu extends the brand Honsu with depths of about 3000 m. In the southwestern part of the sea, there is a less deep Tsushimskaya Basin. In the area of \u200b\u200bthe Korean Strait, the Korean Peninsula, and about. Honshu, merging, form shamery with depths 120-140 m.
A feature of the morphology of the bottom of the Japanese Sea is a weakly developed shelf, which stretches along the shore of the strip from 15 to 70 km for most of the water area. The most narrow shelf strip width from 15 to 25 km is marked along the southern coast of Primorye. The larger development of the shelf reaches in the bay of Peter the Great, in the northern part of the Tatar Strait, the East Korean Gulf and in the Korean Strait area.
The total length of the coastline of the sea is 7531 km. It is weakly cut off (with the exception of Peter the Great Bay), sometimes almost straightforward. The few islands are predominantly close to the Japanese Islands and in the Gulf of Peter the Great.
The Japanese Sea is located in two climatic zones: subtropical and moderate. Within these zones, two sectors are distinguished with different climatic and hydrological conditions: the harsh cold northern (winter is partially covered with ice) and soft, warm, adjacent to Japan and the shores of Korea. The main factor forming the climate of the sea is the monsoon circulation of the atmosphere.
The main barical formations that determine the atmospheric circulation over the Japanese Sea are Aleutian depression, the Pacific subtropical maximum and the Asian Atmosphere Center, located above the mainland. Changes in their position during the year causes the monsime nature of climate in the Far East. In distribution atmospheric pressure Over the Japanese Sea, determined by the main barical formations, the following features are found: the total reduction in the pressure from the west to the east, increasing the pressure from the north to the south, the increase in the excess of winter pressure values \u200b\u200bover the summer in the direction from the northeast to the south-west, as well as sharply pronounced Seasonal variability. In the annual pressure of the pressure for most of the sea is characterized by the existence of a maximum pressure in winter and a minimum in the summer. In the northeast part of the sea - near the North Half about. Honshu, oh. Hokkaido and the southern shore of Sakhalin have two maximum pressure: the first - in February and the second - in October, at a minimum-flyer. The amplitudes of the annual stroke of pressure, as a rule, decrease from the south to the north. Along the mainland coast of the amplitude decreases from 15 MB in the south to 6 MB in the north, and along the shores of Japan - from 12 to 6 MB, respectively. The absolute amplitude of pressure fluctuations in Vladivostok is 65 MB, and on about. Hokkaido - 89 MB. Southeast, in the central and southern parts of Japan, it increases to 100 MB. The main reason for increasing the amplitudes of pressure fluctuations in the southeastern direction is the passage of deep cyclones and typhoons.
The features of atmospheric pressure distribution described above are determined general characteristics wind regime Over the water area of \u200b\u200bthe Japanese Sea. The mainland coast in the cold season, strong winds of the North-West direction with speeds of 12-15 m / s are dominated. The repeatability of these winds from November to February is 60 - 70%. In January and February, the repeatability of the prevailing winds in separate points of the coast comes to 75 to 90%. From the north to the south of the wind speed, gradually decrease from 8 m / s to 2.5 m / s. Along the island eastern coast The winds of the cold season are not so distinctly expressed in the direction of the mainland shore. Wind speeds are less here, but also on average decrease from north to south. Each year at the end of summer and at the beginning of the fall, tropical cyclones (typhoon) accompanied by hurricane winds come to the Japanese sea. During the cold season, the repeatability of the storm, caused by deep cyclones of the winds increases sharply. In the warm period of the year over the sea, the southern and southeastern winds are dominated. The repeatability of them is 40 - 60%, and speed, like in winter, are on average descending from north to south. In general, wind speed in the warm season is significantly less than in winter. In transition seasons (in spring and autumn), the directions and wind speed undergo significant changes.
For open areas of North-Western areas of the sea, the winds of the North-Western and Nordic directions are predominant. In the direction of the southwest, the winds turn from the north-western to Western, and in areas adjacent to South Sakhalin and Hokkaido, from the north-western to the northern and even northeast. In the warm season of such a natural painting of the general structure of the wind field, it is not possible to install for the entire sea. However, it is found that the winds of the eastern and northeastern are dominated in the northeast areas, and in the southern southern directions.
In the Japanese Sea air temperature It is naturally changing both from north to south and not east from the West. In the northern, more severe climatic zone, the average annual temperature is 2 °, and in the south, in the region of subtropics - + 15 °. In the seasonal during the air temperature, the minimum takes place in the winter months (January - February), and the maximum in August. In the north, the average monthly temperature of January is about -19 °, and the absolute minimum is -32 °. In the south, the average monthly temperature in January is 5 °, and the absolute minimum -10 °. In August, in the north, the average temperature is 15 °, and the absolute maximum is + 24 °; In the south, respectively, 25 ° and 39 °. Changes in the West to the East have a smaller amplitude. The west coast throughout the year is colder than the east, and the differences in temperatures increase from the south to the north. In winter, they are greater than in summer, and on average are 2 °, but on some latitudes can reach 4 - 5 °. The number of cold days (with an average temperature below 0 °) sharply decreases from the north to south.
In general, the sea is negative (about 50 W / m) the annual radiation balance of heat on the surface, which is compensated by the constant inflow of heat with the waters entering the Korean Strait. The water balance of the sea is determined mainly by its water exchange with adjacent basins through three straits: Korean (inflow), Sangar and Laperose (stock). Compared with the amount of water exchange through the straits, the contribution to the water balance of precipitation, evaporation and mainland is negligible. The mainland stock in connection with its insignificance has its influence only in the coastal areas of the sea.
The main factors defining hydrological mode The Japanese Sea is the interaction of its surface water with the atmosphere against the background of changing climatic conditions and water exchange through spirits with adjacent water basins. The first of these factors is decisive for the northern and northwestern part of the sea. Here, under the influence of North-Western monsoon winds, bringing from the mainland areas in the winter season, cold air masses, surface waters as a result of heat exchange with the atmosphere are significantly cooled. At the same time, in the shallow water areas of the mainland coast, the Bay of Peter the Great and Tatar Strait is formed by ice cover, and convection processes develop in the surrounding areas of the sea. Convection covers significant layers of water (to depths of 400-600 m), and in some abnormally cold years reaches the bottom layers of deep-water basin, ventilating cold, relatively homogeneous deep aqueous mass, which is 80% of the total volume of the sea. Throughout the year, the northern and northwestern parts of the sea remain colder than southern and southeast.
Water exchange through the straits has a dominant effect on the hydrological regime of the South and Eastern half of the sea. Through the Korean Strait of the subtropical waters of the Kurosio branch throughout the year the southern areas of the sea and water adjacent to the coast of the Japanese islands right up to the Laperose Strait, with the result that the water of the eastern sea of \u200b\u200bthe sea is always warmer than Western.
This section summarizes the basic information about the spatial distribution and variability of temperature and salinity of sea water, water masses, currents, tides and ice conditions of the Japanese Sea, based on published works and analyzing the graphic material of the atlas. All values \u200b\u200bof air and water temperature are given in degrees Celsius (O C), and salinity - in ppm (1 g / kg \u003d 1).
On the horizontal water temperature distribution maps on the surface of the North and southern part of the sea are clearly divided by thermal front, the position of which during all seasons of the year remains approximately constant. This front separates the warm and salty waters of the southern sector of the sea from colder and collapsible waters of the northern part of the sea. The horizontal temperature gradient on the surface of the front across the front changes from the maximum values \u200b\u200bof 16 ° / 100 km in February, to the minimum - 8 ° / 100 km in August. In November-December, the secondary front is formed in parallel with the Russian coast in parallel with a gradient of 4 ° / 100 km. The temperature difference within the entire sea water area in all seasons remains almost constant and equal to 13-15 °. The warmer month is August, when temperatures in the north are 13-14 °, and in the south, in the Korean Strait, reach 27 °. The lowest temperatures (0 ... -1.5 0) are characteristic of February, when ice is formed in the northern shallow areas, and in the Korean Strait, the temperature decreases to 12-14 °. The magnitudes of seasonal changes in the water temperature on the surface are generally increasing from the south-east to the north-west of the minimum values \u200b\u200b(12-14 0) from the Korean Strait - to the maximum (18-21 0) in the central part of the sea and the hall. Peter the Great. Regarding average annual values, negative temperature anomalies occur in the period from December to May (during the winter monsoon), and positive - from June to November (Summer Monson). The strongest cooling (negative anomalies to -9 °) occurs in February in the region 40-42 ° C.Sh., 135-137 ° V.D., and the greatest heating (positive anomalies of more than 11 °) is observed and August near Peter Bay Great.
With an increase in the depth of the range of spatial changes in temperature and its seasonal oscillations on different horizons is significantly narrowed. Already on the horizon 50 m, seasonal fluctuations in temperature do not exceed 4-10 0. The maximum amplitudes of temperature fluctuations at this depth are marked in the southwestern part of the sea. On the horizon 200 meters, the average monthly values \u200b\u200bof the water temperature at all seasons increase from 0-1 0 in the north of the sea - up to 4-7 ° in the south. The position of the main front here does not change relative to the surface, but its meandrement is manifested in a plot between 131 ° and 138 ° V.D. In the central part of the pool to the north of the main front, the temperature on this horizon is 1-2 0, and the south - increases with a jump to 4-5 °. At a depth of 500 m, the temperature within the entire sea varies slightly. It is 0.3-0.9 ° and practically does not experience seasonal variations. The zone of the front partition at this depth is not manifested, although in the region adjacent to the coast of Japan and Korea, there is a certain increase in temperature due to heat transfer into deep layers by vortex formations that are actively emerging in this area of \u200b\u200bthe sea.
From the regional features of the horizontal temperature distribution, it is necessary to note the Area Zones, vortex education and coastal fronts.
APVELING W. southern Coast Primorye is intensively developed in late October - early November, but some cases of its fleeting manifestation can be identified in September - early October. The diameter of the cold water stains in the Apuvelling zone is 300 km, and the temperature difference between its center and the surrounding waters can reach 9 0. The emergence of the appellaling is due not only to the amplification of deep-sea circulation, but also mainly a monsoon change of winds, which is confined precisely by this time interval. Strong northwestern winds, which are met with mainland, create favorable conditions for the development of the Apwelling in the area. In late November, under the influence of cooling, it is destroyed by stratification in the area of \u200b\u200bthe Apwelling zone and the temperature distribution on the surface becomes more uniform.
In the coastal zone of the northwestern part of the Japanese Sea (in the area of \u200b\u200bthe seaside flow), the frontal section is formed at the beginning of summer amid the overall increase in the temperature of the surface layer. The main front runs parallel to the coastline. In addition to it, there are secondary fronts oriented perpendicular to the shore. In September-October, the main front is present only in the northern part of the sea, and the southerly observed separate stains of cold water, limited by fronts. It is possible that the appearance of cold water cells off the coast is due to the rapid cooling of the surface layer in shallow regions. These waters, after the final destruction of the thermocline, are distributed in the direction of the open part of the sea in the form of continuous intrusions.
The most actively vortex formations are formed on both sides of the front and, covering a significant waters, anomalies contribute in the field of horizontal temperature distribution.
Lack of water treatment of the Japanese Sea with neighboring pools at depths of more than 200 m, as well as active ventilation of the deep layers due to the autumn-winter convection in the northern and northwestern regions, lead to a clear separation of water thickness for two layers: near-surface Active layercharacterized by seasonal variability and depthwhere both seasonal and spatial variability are almost not traced. According to existing estimates, the boundary between these layers is located at the depths of 300-500 m. Extreme depths (400-500 m) are confined to the southern part of the sea. This is due to the descending water movement observed here in the center of the extensive anticyclonic meander of the East Korean flow, as well as with variations of the position of the front zone on its northern and eastern borders. To the horizon of 400 m, seasonal temperature fluctuations off the coast of Japan are traced, which is a consequence of the lowering of water in anti-cyclonic cyphans, which are formed by the interaction of the Tsushimian flow with a mainland slope. The high values \u200b\u200bof the depth of the penetration of seasonal temperature fluctuations (up to 400-500 m) are found in the Tatar Strait. It is mainly due to convective processes and a significant seasonal variability of surface water parameters, as well as with the intro-permanent variability of the intensity and spatial position of the branch of the Tsushimian flow. At the coast of the Southern Primorye, seasonal variations of water temperature are manifested only in the upper three hundred-meter layer. Below this border, seasonal temperature fluctuations are almost not traced. As can be seen on the vertical cuts of the temperature field, the characteristics of the active layer undergo significant changes not only in seasonal progress, but also from the area to the district. The water of the deep layer occupying about 80% of the sea volume is weakly stratified and have a temperature of from 0.2 to 0.7 °.
The thermal structure of water of the active layer consists of the following elements (layers): Upper quasomorbon layer (VKS), seasonal layer jump Temperature I. basic thermocline. Characteristics of these layers in various seasons at the water area have regional differences. At the shores of Primorye, in the summer, the lower border of the VKS is at a depth of 5-10 m, and in the southern seasons it is plugged to 20-25 m. In February, the lower border of the VKS in the southern sector is at depths of 50-150 m. Seasonal thermocline is intensified From spring by summer. In August, the vertical gradient in it reaches a maximum - 0.36 ° / m. In October, seasonal thermocline is destroyed and merged with the main, located throughout the year at depths of 90-130 m. In central areas of the sea, marked patterns are maintained against the background of a general reduction in contrasts. In the northern and northwestern part of the sea, the main thermocline is weakened, and sometimes missing at all. Seasonal thermocline here begins to form with the beginning of spring waters and exists until the winter period, when it is completely destroyed by convection within the entire water stratum water.
Horizontal salinity distribution
Large-scale features of salinity distribution on the surface are determined by the water supply of the sea with neighboring sea pools, precipitation and evaporation balance, ice formation and melting, as well as a continental flow in coastal areas.
In the winter season, for the most part of the sea, the salinity of water exceeds 34, which is due mainly by the receipt of high-headed water (34.6) from the East-China Sea. Less salted waters are concentrated in the coastal areas of Asian mainland and islands, where their salinity decreases to 33.5 ‰ -33.8. In the coastal areas of the southern half of the sea, the minimum salinity on the surface is observed in the second half of summer and at the beginning of autumn, which is associated with storm sediments of the second half of summer and the desalination of the waters made from the East Kamchatka Sea. In the north part of the sea, in addition to the summer-autumn lowering, the second minimum of salinity is formed in the period of melting of the ice of the Tatar Strait and Petra Great Bay. The highest values \u200b\u200bof salinity in the southern half of the sea are on the spring-summer season, when the festive fever is intensified at this time of the Pacific Waters from the East-China Sea. It is characteristic of the gradual delay of salinity maxima from the south to the north. If in the Korean Strait, the maximum comes in March-April, then the northern coast of O. Chonse is observed in June, and the Laperose Strait in August. Along the mainland coast, the maximum of salinity takes place in August. The most saline waters are located at the Korean Strait. In the spring, these features are mainly maintained, but the region of low salinity values \u200b\u200bin coastal areas due to ice melting and increasing mainland, as well as the amount of precipitation increases. Next, by the summer, following the flow of the East-China Sea, the common area of \u200b\u200bsalinity in the water area of \u200b\u200bthe sea decreases through the Korean Strait of the Surface Waters of the East-Chinese Sea, the common area of \u200b\u200bsalinity. In August, the range of salinity variability within the entire sea is 32.9-33.9. At this time, in the north of the Tatar Strait, salinity decreases to 31.5, and in some sections of the coastal zone - up to 25-30. In the fall, when the northern winds enhance the northern winds, there is a split and mixing the water of the upper layer and there is some increase in salinity. The minimum seasonal changes in salinity on the surface (0.5-1.0 ‰) are marked in the central part of the sea, and the maximum (2-15) - in the coastal areas of the North, North-Western part and in the Korean Strait. At high depths, along with a common increase in salinity values, a sharp decrease in the range of its variability occurs in space and time. According to the monthly miniature data, at a depth of 50 meters, seasonal changes in salinity in the central part of the sea do not exceed 0.2-0.4, and the north and south of the water area - 1-3. On the horizon 100 m, horizontal changes in salinity are laid in the range of 0.5 ‰, and on the horizon 200 m (Fig. 3.10) in all seasons of the year they do not exceed 0.1, i.e. The values \u200b\u200bare characteristic of deep waters. Some big values \u200b\u200bare observed only in the southwestern part of the sea. It should be noted that the horizontal distributions of salinity at depths, large 150-250 m, have a great similarity: the minimum salinity is confined to the northern and northwestern parts of the sea, and the maximum - to the southern and southeast. At the same time, the slain front expressed at these depths completely repeats the outlines of thermal.
Vertical distribution of salinity
The vertical structure of the salinity field in various parts of the Japanese Sea is characterized by a significant variety. In the north-western part of the sea, there is a monotonous increase in salinity with a depth of all seasons of the year, with the exception of the winter, when it is almost constant in the thickness of the waters. In the southern and south-eastern part of the sea, in the warm period of the year, the intermediate layer of increased salinity formed highly salted waters (34.3-34.5), arriving through the Korean Strait, is clearly distinguished below the tempered surface waters. The kernel is located at the depths of 60-100 m in the north and are somewhat deeper - in the south of the sea. To the north, salinity in the kernel of this layer decreases and on the periphery reaches the values \u200b\u200bof 34.1. In the winter season, this layer is not expressed. At this time of the year, the changes in the salinity vertically at most of the water area do not exceed 0.6-0.7. In a limited area, located east of the Korean Peninsula at depths of 100-400 m, an intermediate layer of reduced salinity is distinguished, which is generated in the winter season due to the immersion of surface waters in the front partition zone. The salinity in the kernel of this layer is equal to 34.00-34.06. Seasonal changes in the vertical structure of the salinity field are well noticeable only in the upper 100-250-meter layer. Maximum depth The penetration of seasonal oscillations of salinity (200-250 m) is noted in the zone of the waters of the Tsushimsky flow. This is due to the peculiarities of the intra-partial stroke of salinity in the subsurface Pacific waters entering the sea through the Korean Strait. At the top of the Tatar Strait, near the coast of Primorye, Korea, as well as in the south and south-west area. Peter the Great Seasonal Saltry Variations are manifested only in the upper 100-150 meter layer. Here, the influence of the water treatment of the Tsushimsky flow is weakened, and the introgenous changes in the salinity of the surface layer of waters associated with the processes of ice formation and the river drain are limited to the waters of the bays and the bays. This area with minimal values \u200b\u200bof the depth of the manifestation of seasonal salinity oscillations is mixed with higher values, the origin of which is associated with penetration to the north-western shores of the sea of \u200b\u200bthe branches of the high-headed waters of the Tsushimsky flow. The overall view of the vertical structure of the salinity field give spatial sections of the distribution of this characteristic and the table values \u200b\u200bgiven in the atlas.
Water masses
In accordance with the specific features of the spatial-temporal variability of the temperature and salinity, the thickness of the Japanese sea water consists of various water masses, the classification of which is produced mainly by extreme elements of the vertical distribution of salinity.
By vertical The water masses of the open part of the Japanese Sea are divided into superficial, intermediate and deep. Surface The aqueous mass (its varieties: PSA - subarctic, PVF - front zones, PST - subtropical) is located within the top mixed layer and is limited to the bottom of the seasonal thermoclin. In the southern warmth sector, it (PST) is formed as a result of mixing waters coming from the East-China Sea and coastal waters of the Japanese islands, and in the cold northern (PSA) - mixing of coastal areas with the waters of open areas of the seafront of the sea. As shown above, during the year, the temperature and salinity of surface waters are changed in a large range, and their thickness ranges from 0 to 120 m.
Located below intermediate The water layer for most of the sea in the warm period of the year is distinguished by a water mass of high salinity (its species: PPST - subtropical, PPSTT - transformed), the core of which is located at depths of 60-100 m, and the lower boundary at a depth of 120-200 meters. The salinity in its kernel is 34.1-34.8. In the local area to the east of the coast of the Korean Peninsula at depths of 200-400 m, an aqueous mass of low (34.0-34.06) salinity is distinguished.
Depth The aqueous mass is commonly referred to as the water of the Japanese sea itself, covers the entire bottom layer (deeper than 400 m) and is characterized by homogeneous temperature values \u200b\u200b(0.2-0.7 °) and salinity (34.07-34.10). The high content of dissolved oxygen in it indicates the active update of the depth layers of surface waters.
IN coastal areas The north-western part of the sea due to a significant resistance to the mainland flow, exacerbation of tidal phenomena, windupwlings and winter convection formed a specific coastal structure of water, represented by a combination of surface water vertical (PP) less salted than water adjacent to the Open Sea regions, and having more significant Temperature fluctuations, as well as subsurface waters (PPSA) of higher salinity and low temperatures that are formed during the winter convection. In some areas (Tatar Strait, Petra Great Bay) during intensive gland formation in winter, high-grade (up to 34.7 ‰ and very cold (up to -1,9 0) is formed (DSh). Navigating from the bottom, it can reach the edges of the shelf And flush along the continental slope, participating in the ventilation of the deep layers.
On the part of the shelf, where the cutting of the mainland stock is small, weakening or even the destruction of water stratification with tidal stirring occurs. As a result, a weastratified shelf structure is formed, consisting of relatively cold collaborated surface shelf water mass (PSH) and relatively warm and collapsible shelf modification of deep water (GSH). With certain directions of predominant winds, this structure is distorted by the appearance of the Apwelling. In winter, it is destroyed by a more powerful mechanism - convection. The water mixing in the zones of tidal mixing is involved in the circulation existing in the northwestern part and distributed beyond the limits of the area of \u200b\u200btheir education, usually considering as "waters of seaside flow".
| Characteristics of the structures of waters and water masses in the north-western part |
||||
| Japanese Sea (Numerator - February, denominator - August) |
||||
| Structure of water |
Water masses |
Salmon depths, m |
Temperature, |
Saltness, ‰ |
| Cubtropical |
0-200 |
> 8 |
33,9-34,0 |
|
| 0-20 |
> 21 |
33,6-33,8 |
||
| missing |
missing |
missing |
||
| 30-200 |
10-15 |
34,1-34,5 |
||
| Depth |
>200 |
0-2 |
33,9-34,1 |
|
| >200 |
34,0-34,1 |
|||
| Polar zones |
0-50 |
3 - 6 |
33,9-34,0 |
|
| 0-30 |
18-20 |
33,5-33,9 |
||
| missing |
missing |
missing |
||
| 30-200 |
33,8-34,1 |
|||
| Depth |
>50 |
0-2 |
33,9-34,1 |
|
| >200 |
33,9-34,1 |
|||
| Subarctic |
0-NO |
0-3 |
33,6-34,1 |
|
| 0-20 |
16-18 |
33,1-33,7 |
||
| Depth |
0-NO |
0-3 |
33,6-34,1 |
|
| 33,9-34,1 |
||||
| Coastal |
missing |
missing |
missing |
|
| 0-20 |
16-19 |
>32,9 |
||
| 0-NO |
-2 - -1 |
>34,0 |
||
| missing |
missing |
|||
| missing |
missing |
missing |
||
| 1 - 5 |
33,2-33,7 |
|||
| Convection zones |
0-NO |
-1 - 1 |
33,7-34,0 |
|
| on the shelf |
||||
| Shelf |
missing |
missing |
missing |
|
| 0-20 |
33,0-33,5 |
|||
| missing |
missing |
missing |
||
| 33,4-33,8 |
||||
Note: In February, the surface and deep aquatic masses of the subarctic structure do not differ in their thermohalin characteristics.
Water and flow circulation
The main elements of the circulation of the water circulation shown in the atlas are the warm flows of the southern and eastern and cold flows of the North-West sectors of the sea. Warm flows are initiated by the influx of subtropical waters entering through the Korean Strait, and are represented by two threads: the Tsushima flow consisting of two branches is a calm-mourn and more turbulent, moving under the coast of Honshu, and the East Korean flow that propagates a single stream. Along the coast of the Korean Peninsula. On a latitude of 38-39 ° S.Sh. The East Korean current is divided into two branches, one of which, rich from the north of the elevation of Yamato, should be in the direction of the Sangsko Strait, the other, deviating to the southeast, part of the waters closes the anti-cyclonic circulation from the southern coast of Korea, and the other is merged with the moth branch. Tsushim's current. The combination of all branches of the Tsushim and East Korean currents into a single stream occurs at the Sangan Strait, through which the removal of the main part (70%) of the incoming warm subtropical waters occurs. The rest of these waters is moving further to the north in the direction of the Tatar Strait. When the lap was reached, the bulk of this stream is made from the sea and only a minor part of it, spreading within the Tatar Strait, gives rise to a cold flow spreading in the southern direction along the mainland coast of Primorye. Divergence zone at 45-46 ° C.Sh. This flow is divided into two parts: the Northern - Liminal (Schrank) The current and southern - the seaside flow, which south of Peter the Great Bay is divided into two branches, one of which gives the beginning of the Cold North Korean current, and the other turns to the south and, in contact with The northern flow of the East Korean flow, forms a large-scale cyclonic circulation with a center at 42 ° S.Sh., 138 ° V.D. Over Japan's hollow. The cold North Korean current reaches 37 ° C.Sh., and then merges with a powerful flow of warm East Korean flow, forming, together with the southern branch of the seaside flow, the zone of the front partition. The least pronounced element of the general circulation scheme is the West Sakhalin Current, the following in the southern direction from the latitude of 48 ° C.Sh. Along the southern coast about. Sakhalin and carrying part of the flow of water of the Tsushimsky flow separated from him on the water area of \u200b\u200bthe Tatar Strait.
During the year, the marked features of the circulation of waters are almost preserved, but the capacity of the main currents changes. In winter, due to the decrease in the flow of water, the speed of both branches of the Tsushimsky flow does not exceed 25 cm / s, and the coastal branch has a greater intensity. The total flow width of about 200 km is saved in summer, but speeds increase to 45 cm / s. The East Korean current is also intensified in the summer when its speeds reach 20 cm / s, and the width is 100 km, and it fades in winter to 15 cm / s and is reduced by width up to 50 km. Cold flow rates during the year do not exceed 10 cm / s, and their width is limited to 50-70 km (with a maximum in summer). In transition seasons (spring, autumn), the characteristics of the flows are average values \u200b\u200bbetween summer and winter. The speed of flows in layer 0-25 is almost constant, and with a further increase in depths, up to half of the surface value at a depth of 100 meters are reduced. The atlas contains water circulation schemes on the surface of the Japanese Sea in various seasons obtained by settlement methods.
Tidal phenomena
Tidal movements in the Japanese Sea are formed primarily half-tidal wave M, which is almost purely standing, with two amphidromic systems located near the borders of the Korean and Tatar straits. Synchronous fluctuations in the tidal profile of the sea level and tidal flows in the Tatar and Korean straits are carried out under the law of a two-zone seishium, whose bullfight covers the entire central deep part of the sea, and the nodal lines are located near the boundaries of the specified straits.
In turn, the interconnection of the sea with adjacent basins through three main straits contributes to the formation of induced tide in it, whose influence, based on the morphological features (shallow water of the sheds compared to the depth of the sea), affects the straits and areas directly adjacent to them. Sea is observed semi-sufficient, daily and mixed tides. The greatest level fluctuations are noted in the extreme southern and northern areas of the sea. In the southern entrance to the Korean Strait, the magnitude of the tide reaches 3 m. As it moves to the north, it is quickly reduced and the pasta does not exceed 1.5 m. In the middle of the sea, the tides are small. Along the eastern shores of Korea and the Russian Primorye before the entrance to the Tatar strait, they are not more than 0.5 m. The same magnitude of tides from the Western shores Honshu, Hokkaido and South-West Sakhalin. In the Tatar Strait, the magnitude of the tides 2.3-2.8 m. The increase in the values \u200b\u200bof the tides in the northern part of the Tatar Strait is due to its funnel-shaped form.
In the open areas of the sea, hemphisy tidal flows with rates of 10-25 cm / s are mainly manifested. More complex tidal flows in the straits, where they have and very significant speeds. Thus, in the Sangar Strait of the velocity of tidal flows, 100-200 cm / s reaches 100-200 cm, in the strait of the lapere - 50-100 cm / s, in Korean - 40-60 cm / s.
Ice Conditions
At ice conditions, the Japanese Sea can be divided into three districts: the Tatar Strait, the area along the coast of Primorye from the Cape of the Rotary to Cape Belkina and the Bay of Peter the Great. In winter, ice is constantly observed only in the Tatar Strait and the Gulf of Peter the Great, on the rest of the water area, with the exception of closed bays and bays in the northwestern part of the sea, it is not always formed. The coldest district is the Tatar Strait, where more than 90% of all ice observed in the sea is formed in the winter season. According to many years of this data, the duration of the ice period in the Gulf of Peter the Great is 120 days, and in the Tatar Strait - from 40-80 days in the southern part of the Strait, up to 140-170 days in its northern part.
The first appearance of ice occurs in the tops of bays and bays closed from wind, excitement and having a desalched surface layer. In moderate winter in the Bay of Peter the Great First Ice formed in the second decade of November, and in the Tatar Strait, in the tops of the bays, the Soviet harbor, Chehechev and the Prioleva of Nevelsky, the primary forms of ice are observed in early November. Early glare in the Gulf of Peter the Great (Amur Bay) comes early in November, in the Tatar Strait - in the second half of October. Later - at the end of November. In early December, the development of ice cover along the coast of Sakhalin Island is faster than near the mainland shore. Accordingly, in the eastern part of the Tatar Strait at this time of ice more than in Western. By the end of December, the amount of ice in the eastern and western parts is aligned, and after reaching the parallels of Cape Surkum, the direction of the edge changes: its shift along the Sakhalin coast slows down, and along the mainland - is activated.
In the Japanese Sea of \u200b\u200bIce Pokrov reaches maximum development in mid-February. In medium ice, 52% of the area of \u200b\u200bthe Tatar Strait and 56% of Peter the Great Bay are covered.
The melting of ice begins in the first half of March. In mid-March, open water areas of Peter Great Bay and all seaside coast to Cape Golden are cleaned. The boundary of the ice cover in the Tatar Strait retreats to the north-west, and in the eastern part of the Strait at this time there is purification from ice. Early cleansing of the sea from ice comes in the second decade of April, later - in late May - early June.
Hydrological conditions Hall. Peter the Great and Coastal
zones of Primorsky Krai
Petra Great Bay is the most extensive in the Japanese Sea. It is located in the north-western part of the sea between parallels 42 0 17 "and 43 ° 20" p. sh. and Meridians 130 ° 41 "and 133 ° 02" in. The water of the Bay of Peter the Great Bay is limited from the sea of \u200b\u200bthe Linus connecting the mouth of the river Misty (Tyumen-Ula) with a swivel cape. Along this line, the width of the bay reaches almost 200 km.
Peninsula Muraviev-Amur and the islands groupLocated to the southwest of him, Petra Great Bay is divided into two large bays: Amur and Ussuriysky. Amur bay It is the north-western part of Peter the Great Bay. From the West, it is limited to the coast of the mainland, and from the east - the Gorous Peninsula of the Muravyev-Amur and Islands, Russian, Popova, Rake, Rykorda. The southern border of the Amur Gulf is the line connecting the Cape Bruce with the islands of the whole and jaggie. The bay extends in the north-western direction by about 70 km, and its screen, which averages 15 km, ranges from 13 to 18 km. Ussuri Bay It occupies the north-eastern part of Peter the Great Bay. From the North-West, it is limited to the Amur Muravyev Peninsula, Russian Island and lying south-west of the last islands. The southern bay border is the line that connects the southern tip of the islands of jaggie and ascold.
The area of \u200b\u200bPetra Great Bay is about 9 thousand km 2, and the total length of the coastline, including islands, is about 1500 km. On the extensive water area of \u200b\u200bthe bay there are many different areas islands, focused, mainly in the western part of the bay in the form of two groups. The northern group is located south-west of the Amur Peninsula and separated from it the Bosphorus-East Strait. This group consists of four large and many small islands. The biggest in this group is the island of Russian. The southern group is the islands of the Roman Corsakov - includes eight islands and a lot of islets and rocks. The most significant in it is the island of Big Pelis. In the eastern bay there are two more large islands: Putyatina, located among the Gulf of arrows, and Askold, lying southwest of the island of Putitin.
Most significant strait It is the Bosphorus-East, separating from the Amur Amur Peninsula Russian. Straits between the islands of Roman Corsakov deep and wide; Between the islands adjacent to the Amur Muravyev Peninsula, the straits are narrower.
The coastline of Petra Great Bay is very winding and forms a lot of secondary bays and bays. The most significant of them are the bays of the village, Amur, Ussuriy, Arrows, East and Nakhodka (America). IN west shore The southern part of the Amur Gulf goes away by the Slavic Bay, the Bay of Tabunny, Narva and Provided. The coastline of the northeastern part of the Amur and the North-Western part of the Ussuri Bay is relatively weakly cut. On the eastern shore of the Ussuri Bay, the bays of Sukhodol, Andreeva, Velyakovsky, Vampat and Podyapolsky stand out. Far sitting in the sea Mausi form the rocky, mostly cloudy shores, bordered by stones. The largest out of peninsula Are: Gamova, Bruce and Amur Muravyev.
Relief DNA The bay of Peter the Great is characterized by a developed shallow water and a steep mainland slope, rugged underwater canyons. The mainland slope takes place in 18 and 26 miles south of Askold and Ramikord Islands almost parallel to the line connecting the mouth of the river Misty and Cape Rotary. The bottom in the Gulf of Peter the Great is quite even and smoothly rises from the south to the north. In the eastern part of the depth bay, the depths reach 100 m and more, and in Western do not exceed 100 m. Morustea input to the depth bay increases sharply. On the mainland slope in the bandwidth from 3 to 10 miles of depths vary from 200 to 2000 m. Secondary bays - Amur, Ussuriysky, Nakhodka - shallow water. In the Amur Bay, the bottom relief is rather smooth. From the shores of the top of the bay stretch extensive shallows. From the North-West Bank of the Island, the underwater threshold with depths 13-15 m. At the entrance to the Ussuri Bay of depths are 60-70 m, then decrease to 35 m in the middle part of the bay and up to 2-10 m at the top . In the bay, the depth of the inlet depth reach 23-42 m, in the middle part 20-70 m, and the top of the bay is occupied by shallow water with depths of less than 10 m.
Meteorological regime The bay of Peter the Great, determine the monsoon circulation of the atmosphere, the geographical position of the area, the impact of cold seaside and warm Tsushimsky (in the south) of currents. From October-November to March, due to the action of the formed bary atmospheric centers (Asian maximum of atmospheric pressure and Aleutian minimum), transferring Cold continental air from the mainland at sea (winter monsoon). As a result, in the bay of Peter the Great, frosty is installed, cloudless weather with a small amount of precipitation and the predominance of winds of the Northern and North-Western destinations. Spring wind regime is unstable, air temperature is relatively low and long periods of dry weather are possible. Summer Monsoon operates from May-June to August-September. At the same time, the transfer of sea air to the mainland and there is warm weather with a relatively large amount of precipitation and fogs. Autumn in the Gulf of Peter the Great is better time years - usually warm, dry, with a predominance of clear, sunny weather. Warm weather keeps in seven years until the end of November. In general, the steady monsime weather nature is often disturbed by intensive cyclonic activities. The passage of cyclones is accompanied by an increase in cloudiness to a continuous, livhery precipitation, worsening visibility and significant storm activity. The average annual precipitation in the region of Vladivostok reaches 830 mm. Atmospheric precipitates are minimal in January and February (10-13 mm). At the summer period accounts for 85% of the annual amount of precipitation and in August 145 mm falls on average. In some years, precipitation, comparable in terms of the amount with monthly standards, can wear a volleune, short-term nature and to lead to natural disasters.
In the annual course of mid-year monthly values atmospheric pressure The minimum (1007-1009 MB) is observed in June-July, and maximum (1020-1023 MB) in December-January. In the Amur and Ussuri bays, the fluctuation range of pressure values \u200b\u200bfrom maximum to minimum values \u200b\u200bis gradually increased by removal from coastal areas to more continental. Short-term changes in the pressure in daily course reach 30-35 MB and accompanied by sharp fluctuations in speed and wind direction. The actually registered maximum pressure values \u200b\u200bin the region of Vladivostok are 1050-1055 MB.
Average annual T. emperature air It is approximately 6 °. The most cold month of the year is January, when the average monthly air temperature in the northern part of the Amur and Ussuri bay is -16 ° ... -17 °. In the top of the Amur and Ussuri bay, the air temperature can be reduced to -37 °. The warmest month of the year is August, when the average monthly temperature rises to + 21 °.
During the winter monsoon, since October-November, March is dominated by March Winds Northern and Northwest directions. In the spring, when changing the winter monsoon on a summer, the winds are stable little. In the summer, southeastern winds prevail in the bay. The calm is more often marked in summer. The average annual wind speed varies from 1 m / s (at the top of the Amur Gulf) to 8 m / s (Askold Island). On some days, the wind speed can reach 40 m / s. In summer, wind speed is less. In the tops of the Amur and Ussuri bays, the average monthly wind speed is 1 m / s, in bays and bays - 3-5 m / s. Storms are connected mainly with cyclonic activities and are observed mainly in the cold period of the year. The greatest number of days with the storm wind is celebrated in December-January and is 9-16 per month. At the tops of the Amur and Ussuri bays, storm winds are not observed annually.
In the bay of Peter the Great come typhoon, emerging in tropical latitudes, in the Philippine Islands area. The Japanese Sea and Primorsky Krai predominantly in August-September come out about 16% of all the tropical cyclones there are emerging. The paths of their movement are distinguished by a large variety, but none repeats the trajectory of the other in accuracy. If Typhoon is not included in the bay of Peter the Great and is observed only in the southern part of the Japanese Sea, he still affects the weather in the area: there are strong rains and the wind increases to the storm.
Hydrological characteristic
Horizontal temperature distribution
The water temperature on the surface is experiencing significant seasonal variability, due to mainly the interaction of the surface layer with the atmosphere. In the spring, the temperature of the water in the surface layer on the water area of \u200b\u200bthe Bay changes in the range of 4-14 °. In the vertices of the Amur and Ussuri bay, it reaches 13-14 ° and 12 °, respectively. In general, the Amur Bay is characterized by higher temperatures than Ussuriysky. In the summer of water the bay is well warmed. At this time, in the tops of the Amur and Ussuri bay, it reaches 24-26 °, in the Gulf of America - 18 °, and in the open part of the bay - 17 °. In the fall, a temperature drop is reduced to 10-14 ° in secondary bays and up to 8-9 ° in the open part. In winter, the whole mass of water is cooled, its temperature ranges from 0 to -1.9 °. Negative temperatures occur throughout the shallow water, as well as in secondary bays. The position of isotherm 0 ° roughly coincides with the 50-meter isobate. At this time, the water of the open part of the bay is warmer coastal and characterized by positive temperature values. With increasing depth, the temperature change range decreases and already at a depth of 50 m does not exceed 3 °, and at the depths of more than 70 meters, seasonal changes are almost not manifested.
Vertical temperature distribution
In the warm period of the year (April-November) there is a monotonous decrease in temperature with depth. At this time, a layer of seasonal thermocline is formed on the subsurface horizons - everywhere, except for shallow water, where the whole waters are well warmed and mixed. In the fall from the beginning of the action of the winter monsoon and cooling, there is a rise of cold deep waters on the shallow water and at a depth of 40 m, a second layer of temperature jump is formed. In December, both layers of leaping the temperature under the influence of convection are destroyed, and the entire winter period (from December to March) the temperature remains constant within the entire thickness of the bay water.
Saltness distribution
The orographic conditions of the bay and the impact of mainland create a kind of distribution mode and salinity variability. Water in some coastal areas of the bay is designed to a saltwater, and in open areas is close to the salinity of the seaside seafridge. The annual stroke of salinity is characterized by a minimum summer and maximum winter. In the spring, the minimum values \u200b\u200bof salinity on the surface are confined to the top of the Amur Gulf, where they are 28. At the top of the Ussuri Bay, salinity is 32.5, and in the rest of the water area rises to -33-34. In the summer, the surface layer is subjected to the greatest college. At the top of the Amur Gulf, the salinity is 20%, and in general in coastal waters and secondary bays, it does not exceed 32.5 and increases in open areas to 33.5. In the autumn, the horizontal distribution of salinity is similar to the spring. In winter, at the entire water area, the salty is close to 34. At depths of more than 50 meters, salinity changes within the water area of \u200b\u200bthe bay in the range of 33.5-34.0.
With an increase in the depth of salinity, as a rule, increases (spring-autumn) or remains constant (winter). In the bottom layer of the bay due to the process of coalion during the formation of ice in the winter months, high density water with a temperature of less -1.5 °, and salinity of 34.2-34.7, are formed. In extremely ice years, high-detailed waters, spreading at the bottom reaches the edges of the shelf, roll along the slope and the deep-water seaside layers are ventilated.
Water masses
In the winter season, in the bay of Peter the Great Water in its characteristics within the limits of the entire thickness correspond to the deep water mass of the Japanese Sea (temperature is less than 1 °, salinity - about 34 ‰). In the bottom 20 meter layer during this period of time, aqueous mass of high density with low (up to -1.9 °) temperature and high (up to 34.8) salinity, which already disappears in mid-March, mixing with the surrounding waters.
In the summer season due to the increase in the inflow of heat and mainland, the water stratification occurs. In coastal areas, especially in the zones of freshwater receipts from the mouth of the rivers, the estuhaous aqueous mass of low (on average 25 ‰) salinity is highlighted, high (on average 20 °) in the summer season and depth of distribution to 5-7 meters. Water masses of open areas of the bay seasonal thermoclinin are divided into: superficial coastal, extremely spreading from the surface to a depth of 40 m and summer having indices: temperature - 17-22 °, salinity - 30-33 ‰; subsurface - to a depth of 70 m with a temperature of 2-16 ° and salinity of 33.5-34.0 ‰; And the deep shelf - below the horizon of 70 m to the bottom with a temperature - 1-2 ° and salinity of about 34.
Flow
Circulation of waters in the Gulf of Peter the Great is formed under the influence of the constant currents of the Japanese Sea, adorid-tidy, wind and stock currents. In the open part of the bay, the seaside flow is clearly traced, which spreads in the south-west direction with a speed of 10-15 cm / s. In the southwestern part of the bay, it turns to the south and gives the beginning of the North Korean flow, the most pronounced on the subsurface horizons. In the Amur and Ussuriysk bays, the influence of the seaside flow is clearly manifested only in the absence of wind, when anticyclonic water circulation is formed in the Ussuri bay, and in Amur - cyclonic. The wind, pensor phenomena and the flow of the River River (in the Amur Gulf) cause a substantial restructuring of the flow field. The schemes of the main components of the total flows of the Amur and Ussuriy bays, shown in the atlas, show that the greatest contribution to the wind flows, which in the winter season increase the anticyclonic circulation in the Ussuri bay, and in the summer they change it to cyclonic. When cyclones passing the speed of total flows on the surface can reach 50 cm / s.
Tidal phenomena
The semi-radical tidal wave is included in the bay of Peter the Great from the southwest and spreads to the secondary bays, Wissury and America. She rises bay over time less than one hour. The time of the complete water of semi-suite tide is slowed down in closed bays and secondary bays separated by the islands and peninsulas. The maximum possible amount of tides (within a day) in the bay is 40-50 cm. The most well-tidal level fluctuations are developed in the Amur Gulf, in its northwestern district, where the maximum level of level is somewhat higher than 50 cm, and less - in the Ussuri bay and the strait between about. Putyatina and the mainland (the magnitude of the tide is up to 39 cm). Tidal flows in the bay are insignificant and their maximum speeds Do not exceed 10 cm / s.
Ice Conditions
Ice regime The district practically does not interfere with regular navigation throughout the year. In the bay of ice are found in the winter season in the form of soldering and drifting ice. The beginning of the ice formation begins in mid-November in the Bays of the Amur Gulf. At the end of December, most Amur Bay and partly of the Ussuri Bay are completely covered with ice. In the open part of the sea there is a drifting ice. Maximum development Ice Pokrov reaches at the end of January - mid-February. Since the end of February, the ice environment is facilitated, and in the first half of April, it usually takes full cleaning of the water area of \u200b\u200bthe ice from ice. In the harsh winters, especially in the first decade of February, ice reaches a big cohesion, which eliminates the possibility of swimming vessels without the use of icebreaker.
Hydrochemical characteristics
In this version of the atlas, the hydrochemical characteristics are presented in the form of distribution maps on different horizons of medium-rigorous values \u200b\u200bof dissolved oxygen content (ML / L), phosphates (μm), nitrates (μm), silicates (μm) and chlorophyll (μg / L) for winter, spring , summer and autumn without additional description. In the source of the data used (WOA "98), the time frame of the hydrological seasons is defined as follows. Winter: January-March. Spring: April-June. Summer: July-September. Autumn: October-December.
Hydraulic-acoustic characteristics
The main changes in the speed of sound speed as seasonal and spatial occur in the layer of 0-500 m. The difference in the sound velocity values \u200b\u200bin the same season on the surface of the sea reaches 40-50 m / s, and at a depth of 500 m - 5 m / from. The maximum values \u200b\u200bare marked in the southern and southeastern parts of the sea, and the minimum - in North and Northwest. The range of seasonal changes in the speed of sound in both zones is about the same and reaches 35-45 m / s. The front zone passes from the southwest to the northeast through the central part of the sea. Here in the layer of 0-200 m, the maximum horizontal gradients of the sound velocity values \u200b\u200bat any time of the year (from 0.2 ° C in summer) are observed. At the same time, the maximum changes in the sound speed values \u200b\u200bhorizontally is observed in the summer at a depth of 100 m.
The vertical distribution of sound speed in the southern and southeastern sea can be allocated:
- upper homogeneous layer, the thickness of which changes from 50 to 150 m during the year, with the sound velocity values \u200b\u200bof more than 1490-1500 m / s;
- a layer of jump speed values \u200b\u200bwith large negative gradients (on average 0.2-0.4 С~¹), propagating to a depth of 300 m;
- layer 300-600 m with minimal values \u200b\u200b(and gradients) of sound speed;
- deeper than 600 m is a constant increase in sound velocity values, mainly due to an increase in hydrostatic pressure.
The axis of the PZK is located at the depths of 300-500 m, and the coast of Japan is 40º s. sh. It drops to 600 m. The sound channel spreads from the surface to the bottom.
In the northern and northwestern part of the sea, a homogeneous layer, but with minimal sound speed values \u200b\u200b(less than 1455 m / s) is formed in winter and is associated with winter convection. The layer thickness can reach 600 m, while the surface audio channel is formed. During the rest of the year, changes in the speed of sound with depth are characterized by negative gradients increasing from spring to autumn to 0.5-0.8 С~¹ in a layer of 0-100 m, minimal gradients in a layer thick up to 500 m and further increasing the speed of sound when constant gradient value. The axis of the PZK with the minimum sound velocity values \u200b\u200bof 1455-1460 m / s in this part of the sea in winter goes to the surface, and from spring to autumn gradually falls to the depth of 200-300 m. When moving to the south in the front area, the axis of the PZK sharply plug up to 300 m . In the central part of the sea, the width of the sound channel does not exceed 1000-1200 m in winter, in the spring increases to 1500 m, and in the summer and at the beginning of the autumn determines only the depth of the place.
Japanese Sea (Yap. 日本 海 nihonkay, Cor. 동해 tonah - "East Sea", in the DPRK is known as 조선동해, 朝鮮東海 choson-Tonah - "East Korean Sea") - the outskirts of the Pacific Ocean, separated from him by the Japanese Islands. From the neighboring Sea Sea is separated from Sakhalin Island, from the next yellow sea - the Korean Peninsula. By origin is a deep-water pseudo-sassous intra-oil depression associated with other seas and the quiet ocean through 4 Strait: Korean (TsUsimsky), Sangar (Tsguar), Laperose (Soya), Nevelsky (Mamia). Washes the shore, and. In the south comes the branch of the warm current of Kurosio.
Area - 1062 thousand km². The greatest depth is 3742 m ( 41 ° 20 's. sh. 137 ° 42 'in. d.). The northern part of the sea freezes in winter.
Climate
Japanese Sea, Antipenko Island
The climate of the Japanese Sea is moderate, monsoon. The north and western parts of the sea are much colder than southern and eastern. During the coldest months (January-February), the average air temperature in the northern part of the sea is about -20 ° C, and in the south about +5 ° C. Summer monsoon brings with her warm and wet air. The average temperature of the air temperature itself (August) in the northern part of approximately +15 ° C, in the southern regions about +25 ° C. In the fall, the number of typhoons caused by hurricane winds increases. The largest waves have a height of 8-10 m, and with typhoons, maximum waves reach a height of 12 m.
Flow
Surface flows form a circuit, which consists of a warm Tsushimsky flow in the East and Cold Primorsky in the West. In winter, the temperature of surface waters from -1-0 ° C in the north and northwest rises to + 10- + 14 ° C in the south and south-east. Spring heating entails a fairly rapid increase in water temperature throughout the sea. In the summer, the water temperature on the surface rises from 18-20 ° C in the north and up to 25-27 ° C in the south of the sea. The vertical distribution of temperature is not the same in different seasons in different parts of the sea. In the summer in the northern regions of the sea, the temperature of 18-10 ° C holds in a layer of 10-15 m, then it dramatically decreases to +4 ° C on the horizon 50 m and, starting with depths 250 m, the temperature remains constant about +1 ° C. In the central and southern parts of the sea, the water temperature is quite smoothly decreased with a depth and on the horizon 200 m reaches the values \u200b\u200bof +6 ° C, starting with depths 250 m, the temperature is kept about 0 ° C.
Salinity
The saltness of the water of the Japanese Sea is 33.7-34.3, which is somewhat lower than the saline of the world's ocean.
Riding
Tides in the Japanese Sea are pronounced, to a greater or lesser extent in various districts. The greatest level fluctuations are noted in the extreme northern and extreme southern regions. Seasonal fluctuations in the sea level occur simultaneously over the entire surface of the sea, the maximum rise level is observed in the summer.
Ice setting
Bay Thymam on about. Honshu is one of the largest bays of Japan
At ice conditions, the Japanese Sea can be divided into three districts: the Tatar Strait, the area along the coast of Primorye from the Cape of the Rotary to Cape Belkina and the Bay of Peter the Great. In winter, the ice is constantly observed only in the Tatar Strait and the Gulf of Peter the Great, on the rest of the water area, with the exception of closed bays and bays in the north-western part of the sea, it is not always formed. The coldest district is the Tatar Strait, where more than 90% of all ice observed in the sea is formed in the winter season. According to many years of this data, the duration of the ice period in the Gulf of Peter the Great is 120 days, and in the Tatar Strait - from 40-80 days in the southern part of the Strait, up to 140-170 days in its northern part.
The first appearance of ice occurs in the tops of the bays and bays closed from the wind, excitement and having a desalinated surface layer. In moderate winters in the Gulf of Peter the Great, the first ice is formed in the second decade of November, and in the Tatar Strait, in the tops of the bays, the Soviet harbor, Chihachev and the Priolava of Nevelsky, the primary forms of ice are observed in early November. Early glare in the Gulf of Peter the Great (Amur Bay) comes early in November, in the Tatar Strait - in the second half of October. Later - at the end of November. In early December, the development of ice cover along the coast of Sakhalin Island is faster than near the mainland shore. Accordingly, in the eastern part of the Tatar Strait at this time of ice more than in Western. By the end of December, the amount of ice in the eastern and western parts is aligned, and after reaching the parallels of Cape Surkum, the direction of the edge changes: its shift along the Sakhalin coast slows down, and along the mainland - is activated.
In the Japanese Sea of \u200b\u200bIce Pokrov reaches maximum development in mid-February. In medium ice, 52% of the area of \u200b\u200bthe Tatar Strait and 56% of Peter the Great Bay are covered.
The melting of ice begins in the first half of March. In mid-March, open water areas of Peter Great Bay and all seaside coast to Cape Golden are cleaned. The boundary of the ice cover in the Tatar Strait retreats to the north-west, and in the eastern part of the Strait at this time there is purification from ice. Early cleansing of the sea from ice comes in the second decade of April, later - in late May - early June.
North-West Bank of the Japanese Sea, in the District City District
Flora and fauna
The underwater world of the northern and southern regions of the Japanese Sea is very different. In the cold northern and northwestern regions, Flora and the fauna of moderate latitudes were formed, and in the southern part of the sea, south of the heat-watering fauna complex prevails. The coast of the Far East has a mixing of heat-water and moderate fauna. Here you can meet octopus and - typical representatives of the warm seas. At the same time, the vertical walls, the scores of the acts, gardens from the brown algae - Laminarium, - all this resembles the landscapes of the White and Barents Sea. In the Japanese Sea, a huge abundance of starfish and marine hero, various color and different sizes, there are worshiors, shrimps, small crabs (Kamchatka crabs are found here only in May, and then they go further into the sea). Bright red ascages live on rocks and stones. Mollusks are the most common scallops. Sea dogs are often found from fish, sea rams.
Sea transport
Vladivostok, Golden Horn Bay
Fishing and sea-culture
Fisheries; mining crabs, trepagov, algae, sea hedgehogs; Growing scallop.
Recreation and tourism
Since the 1990s, the coast of the Japanese Sea near the coast of Primorye begins to actively master the local and visitors. The impetus was the factors such as the cancellation or simplification of the visit to the borderzon, the rise in prices for passenger traffic in the country, which made too expensive holidays of Far Easterns on the Black Sea coast, as well as a highly increased number of personal vehicles, which made the coast of Primorye for residents of Khabarovsk and the Amur region.
International legal status
According to Article 122 of the UN Convention on the Law of the Sea, the Japanese Sea is the semi-jammed sea. Article 123 of the Convention provides for the duty of states to cooperate and coordinate their activities on the management of marine resources, but due to the conflict situation between, and currently coordination is not carried out.
The question of the naming of the sea
In South Korea, the Japanese Sea is called "Eastern Sea" (Cor. 동해), and in the North - Korean Eastern Sea (Cor. 조선동 해). The Korean side claims that the name "Japanese Sea" was imposed on the world community of the Japanese Empire, since in 1910-1945 Korea was occupied and the government of the country could not express at the time of approval by the International Hydrographic Society (IHO) in 1929 the publication of the Ocean borders and Seas ", the view of Korea was not taken into account.
Currently, Korea does not insist on the only version of the name "East Sea", but only recommends the cartoizers to use both names in parallel before the dispute settlement. This led to the fact that the number of countries using both names on their cards at the same time is constantly increasing.
The Japanese side, in turn, shows that the name "Japanese Sea" occurs on most cards and is generally accepted and insists solely on the use of the name "Japanese Sea".
Notes
- Atlas on the oceanography of Bering, Okhotsk and Japanese seas. Far Eastern Branch of the Russian Academy of Sciences. Archived on August 22, 2011.
- Limits of Oceans and Seas (Special Publication No. 23): [ english ] : [Arch. April 17, 2013] / International HydroGraphic Organization. - 3rd EDN. -: imp. Monégasque, 1953. - 39 p.
- «». East Sea. The name used for two millennia.
- Japanese Sea. Japan Foreign Ministry. Checked January 25, 2010. Archived August 22, 2011.
Literature
- Soviets S. A. Japanese Sea // Encyclopedic Dictionary of Brockhaus and Efron: at 86 tons. (82 tons and 4 add.). - St. Petersburg. , 1890-1907.
- Istshin Yu. V. Japanese Sea. - M.: Geographiciz, 1959. - 80 s. - 25,000 copies. (region)
- Shamraev Yu. I., Shishkin L. A. Oceanology: a textbook for hydrometeorological technical schools / Ed. A. V. Nekrasova, I. P. Karpova. - L.: Hydrometeoisdat, 1980. - 382 p.
- Plants and animals of the Japanese Sea. - Vladivostok, 2006.
- Sokolovsky A. S. et al. Fish of Russian water of the Japanese Sea. - Vladivostok, 2007.
- // BIOT OF THE RUSSIAN WATER OF THE Japanese Sea. - Vladivostok, 2004. - T. 1, Ch. 1 (Russian version).
- Crustacean (branchist, thin-penetration, mealsids, eufauxides) and sea spiders // Biota of the Russian Waters of the Japanese Sea .. - Vladivostok, 2007. - T. 1, Ch. 2 (Eng. Improved version).
- Brachiopods and Foronids // BIOT OF THE RUSSIAN WATER OF THE Japanese Sea. - Vladivostok, 2005. - T. 3.
- Caprolelides (sea goats) // Biota of the Russian Water Japanese Sea .. - Vladivostok, 2006. - T. 4.
- Free-lived sucontogy crustaceans and facetectures // BIOT OF THE RUSSIAN WATER OF THE Japanese Sea. - Vladivostok, 2006. - T. 5.
- Turbellaria-polyclades, leeches, oligochettes, Echiuines // BIOT OF THE RUSSIAN WATER OF THE Japanese Sea. - Vladivostok, 2008. - T. 6.
- Japanese Sea: Encyclopedia / Aut. and Sost. I. S. Zonne and A. G. Kolynaya; Ed. A. N. Kosareva. - M.: International. Relationship, 2009. - 420, C.: Il., cards., Port. - Bibliogr.: With. 418-420 (51 Names). - 1000 copies.
Links
- Japanese Sea ( physical Card., scale 1: 5 000 000) // National Atlas of Russia. - M.: Roskartography, 2004. - T. 1. - P. 283. - 496 p. - 3000 copies. - ISBN 5-85120-217-3.
- Japanese Sea in the book: A. D. Dobrovolsky, B. S. Zubodin. Sea of \u200b\u200bthe USSR. Publishing House Mosk. University, 1982.
- Description of the Japanese Sea.
The nature of our planet is beautiful and amazing. You can admire her beauties indefinitely.
One of the most attractive, unknown, unpredictable elements for a person at all times was water. Among the diversity of rivers, seas and oceans, the Japanese Sea, whose resources belong to several countries are playing a large role in their development.
Description
This sea belongs to the pool of the Pacific Ocean. Along with Bering and Okhotsky, it is listed by one of the large and deep seas of Russia. It is of great importance in the implementation of transport and freight transport, is a source of mineral resources. The Japanese Sea is also characterized by a high level of production of fishing species.
Its area stretches on the territory of about 1,100 square kilometers, the volume is 1700 cubic kilometers. Medium depth The Sea of \u200b\u200bJapan is 1550 meters, the greatest is more than 3,500 meters.
The sea is connected to other seas and ocean straits. Nevelsky connects it with the Okhotsk Sea, Korean with East Chinese. Simonoski shares the Japanese and internal Japanese seas, as well as with the quiet ocean, communicates with the help of the Sangar Strait.
Location
The Japanese Sea runs between the mainland of Asia and the Korean Peninsula. Washes a landing of several countries: Russia, Japan, DPRK, Republic of Korea.
The characteristic of the Japanese Sea is also the presence of small islands, such as Popov, Okushiri, Russian, Oshima, Putyatin, Sado and others. Basically, the accumulation of the islands is concentrated in the eastern part.
The water form bays, this is, for example, the Soviet harbor, Isicari, Peter the Great. And also the capes, the most famous Cape Lazarev, Korsakov, soy.
The Japanese Sea has many shipping ports. One of the most significant are Vladivostok, Nakhodka, Alexandrovsk-Sakhalin, Tsuruga, Chhong, and others. They organize the carriage of goods not only in the Japanese sea, but also beyond its borders.
Climate
The weather characteristics of the Japanese Sea are a moderate and subtropical climate, stable wind.
The geographical position and high length divided it into two climatic parts: the North-West and Southeast Zone.
The temperature of the water in different parts depends on the circulation of flows, heat exchange with the atmosphere, the season, as well as from the depths of the Japanese Sea. In the northern and western parts, the water and air temperature is significantly lower due to the influence of the Cold Okhotsk Sea. To the eastern and southern zones, water and air masses who came from the Pacific Ocean are important, so temperature indicators are significantly higher.
In winter, the sea is subject to hurricanes, storms, the duration of which can be several days. The autumn period is characteristic strong windswhich form high, powerful waves. In the summer, steady warm weather prevails in both climatic zones.
Characteristic water
In winter, the temperature of the water in different areas is very different. For the northern part, the ice coating is characterized, whereas in the southern part the approximate temperature is 15 degrees.
In the summer, the northern waters of the Japanese Sea warm up to 20 degrees, southern - to 27.
The water balance consists of two important components: the amount of precipitation, evaporation of water from the surface, the exchange of water, which is performed using the sheds.
The salinity consists of resources of the Japanese Sea, water exchange with other seas, the quiet ocean, the amount of precipitation, the melting of ice, the time of year, some other factors. The average salinity is about 35 ppm.
The transparency of water depends on its temperature. In winter, it is higher than in the warm period of the year, so in the northern part density always has great indicators than in the southern part. According to this principle, the saturation of water oxygen is distributed.
Development of transport paths
The role of the Japanese Sea in the organization of cargo transportation is very large for both Russia and other countries.
Sea transport and cargo transportation is highly developed with great importance for Russia. In the city of Vladivostok, Trannybirsky railway path. There is a unloading of railway and loading of marine transport. In the future, by sea routes, passengers and cargo are sent to other ports of different countries.
Fisheries
The fish resources of the Japanese Sea are characterized by high productivity, manifold, which includes a large number of fish species. Its water can accommodate more than 3,000 inhabitants. Their settlement depends on climate conditions in different areas.
In the warm southeastern part there is a mining of mackerel, seirs, sardines, stavrids, anchovs, cambals, some other species of fish. You can also meet a large number of octopus. Squids and crabs live in the central regions. In the north-west, salmon calm, pollock, cod, herring occurs. The sea is also replete with trepagas, mussels, oysters.
Recently, the production has been actively developing on which cancers, sea erochs are breeding, and cultivation of algae, sea cabbage, laminarium, mollusks, scallops. These aquacultures are also resources of the Japanese Sea.
In addition to commercial species, the Japanese Sea is rich in other inhabitants. Here you can find sea skates, dolphins, whales, seals, coushlots, blesses, small species of sharks and other types of marine residents.
Ecology
Like the resources of the Japanese Sea, environmental problems need a separate study. The impact of the vital activity of the population on the environment in different areas is different.
The main source of pollution is the reset of industrial and domestic wastewater. The greatest negative impact has the release of radioactive substances, products of oil refining, chemical and coal industries, metalworking. Waste of various production flows into the water of the Japanese Sea.
Mining and transportation of oil is associated with large risks for the environment. In case of leakage, the oil stain is quite difficult to eliminate. It causes tremendous damage to the ecology of the sea and its inhabitants.
Transportation waste of numerous ports, sewer docks of cities falling into the sea, also cause considerable harm.
Water studies of the Sea of \u200b\u200bJapan show quite high pollution. The composition includes many chemical elements dropped by production, as well as heavy metals, phenol, zinc, copper, lead, mercury, ammonium nitrogen compounds and other substances. All this contributes to enormous pollution of ecology.
The leaders of the countries with which the sea borders, conduct directed operational and preventive actions in order to preserve unique nature, cleanliness and its inhabitants. It is necessary to control, stop, hard to punish cases of emissions in the water of chemical and oil waste. Enterprises and sewer docks are required to equip with cleansing filters.
These control measures will be able to prevent environmental pollution, protect numerous inhabitants from death, as well as to preserve people's health.
The Japanese Sea is one of the most valuable resources that need not only actively use, but also to protect against the negative consequences of people's vital activity.
The information provided will help to evaluate the resources of the Japanese Sea, study its characteristics, find out the inhabitants, find out environmental aspects.
The study of this sea has been conducted for a long time. Nevertheless, there are many questions and problems requiring research and measures aimed.
