Pai-Khoi is a low mountain range that extends from the extreme northern part of the Polar Urals to the CVD and continues to the Yugorsky Shar Strait. Between Pai-Khoi and the Polar Urals there are a number of intermediate elevations. Pai-Khoi is over 200 km long and 200-400 m above sea level. The highest mountain is More-Iz (467 m).
In physical and geographical terms Pai Hoi occupies the left bank of the Kara River and the Yugorsky Peninsula, administratively located on the territory of the Nenets Autonomous Okrug of the Arkhangelsk Region.
A long discussion about whether Pai-Khoi is an independent ridge, a continuation of the Urals, its lateral branch, or even connected by origin with the Timan Ridge, ended only in the middle of this century. After the geological structure of Pai-Khoi and the Polar Urals was carefully studied, it turned out that these geographical areas are directly connected and Pai-Khoi should be considered a northwestern continuation of the Urals, a link, m in a single Ural-Novaya Zemlya folded region.
According to its orographic structure, Pai-Khoi is a rather complex mountainous country, consisting of several parallel mountain ranges and adjacent plateaus. This entire territory belongs to the tundra zone, among which gentle peaks rise with stony placers, and sometimes rocks. The dismemberment of Pai-Khoi and the obliteration of its forms have been repeatedly emphasized by researchers. E. K. Hoffman wrote that Pai-Khoi “has a series of unconnected, rounded and covered with turf mountains, on which stony caps are visible only in some places ...”. Pai-Khoi is described in approximately the same way by S. V. Kertselli, who pointed out that this range “does not represent a continuous mountain range”, but is a series of “separate narrow, low hillocks elongated along the line of the entire range”. The local population is well aware of the orographic dissection of Pai-Khoi. So, according to Kertselli, "reindeer" distinguish Big Stone- the central part of the ridge, Maly Kamen (in the Komi - Zola-Iz) - its extremely southern ridge, the Sea Range - part of Pai-Khoi from Mount Morepai to Yugorsky Shar.
The geographical name Pai-Khoi should have been written Pe-Khoi, but the traditional form, coming from A. I. Schrenk and E. K. Hoffman, has established itself. For the first time this name, apparently, was witnessed by Schrenk during his famous trip to the Polar Urals in 1837. He writes that the Samoyeds (Nenets) call the western extension of the Urals Paigoi, that is, the “Rocky Range”, and the Western Samoyeds (obviously, Kanin and Malozemelsky Nenets) Khabiygoem, that is, the "Ostyak Range", because the Ostyaks (Khanty) roam around it.
Somewhat later, the name Pai-Khoi, translating it as “Stone Ridge”, is repeatedly given by Hoffmann, the leader of the North Ural expedition of 1847-1850, who, like Schrenk, personally visited these places and received first-hand information from his Nenets guides and Komi-Zyryans (Izhemtsev).
The explanation of the name Pai-Khoi, which we find in Schrenk and Hoffmann, must be considered the only correct one: Nenets pe - “stone”, “rock”, hoi - “mountain”, “ridge”, therefore, Pai-Khoi really means in translation into Russian "Stone Ridge". The transfer of the Nenets pe to the Russian share was explained by Hoffmann, who wrote that the Nenets share is pronounced almost the same as the Russian share. Schrenk also transfers the Nenets pe to the Russian share and, in addition, notes the voicing p to b after the nasal consonant m, which appears at the place of the voiced glottal stop - Peumbay, Suvvumbay, etc.
Indeed, in the Nenets word pe, the vowel is pronounced quite close to the Russian a in combination with e, sometimes also with an overtone and. Since Pai-Khoi is covered with rocky tundra with rocks, the explanation of the oronym given by Schrenk and Hoffman satisfies all the requirements, however, another etymology has recently been proposed - "Slanting Range" taking into account the Nenets share - "curve", "oblique" (see "Dictionary of terms and other words found in Nenets geographical names"). This etymology is wrong.
Another Pae-Khoi - "Stone Ridge" (for Russians - Stone) is located in the northern part of the Kanin Peninsula. This ridge is low, but also rocky, and in some places rocky.
The oronymy of Pai-Khoi originally consisted exclusively of Nenets names, as shown in the works of A. I. Shrenk and E. K. Hoffman, as well as on the map of the famous Hungarian traveler A. Reguli, who visited the Pai-Khoi region in 1844. However, at present, the oronymic system of Pai-Khoi, reflected in cartographic sources, has changed a lot. As far back as the 19th century, the Komi-Zyryans (Izhemtsy) regularly began to graze reindeer in these places. Later, they constantly performed the duties of guides for topographic and geological expeditions. As a result, some Nenets names were completely or partially translated into the Komi language (cf., for example, Kuz-Iz).
Oronimy Pai-Khoi is divided into two regions: northeastern and central Pai-Khoi (north of the Oyu River) and southwestern Pai-Khoi (south of the Oyu River).
Pai-Khoi is an old, heavily destroyed mountain range in the center of the Yugorsky Peninsula, stretching for about 200 km from the northern part of the Polar Urals to the Yugorsky Shar Strait. Part of the ridge is located on Vaigach Island, which separates the Barents Sea and the Kara Sea.
The highest point of the ridge is Mount More-Iz, its height above sea level is 423 m. The mountain is located about 40 km southeast of the village. Amderma. The mountain itself is flat, the rounded forms of the hill consist of the remnant of the glacier - the moraine. In the Nenets language, the mountain is called Vesei-Pe - "Old Man's Mountain". Pai-Khoi is composed of crystalline schists and sedimentary sandstones, marls and limestones.
For the first time for Europeans, the Pai-Khoi Ridge was discovered and its first geological and biological description was compiled by a research expedition led by Hoffmann Ernst Karlovich (1847-1853). She also described the ethnography of the region. The Yugorsky Peninsula is a large peninsula in the extreme northeast of Europe, between the Barents and Kara Seas, in the Nenets Autonomous Okrug of the Arkhangelsk Region of Russia.
In physical and geographical terms, Pai-Khoi occupies the left bank of the Kara River and the Yugorsky Peninsula, in administrative terms it is located on the territory of the Nenets Autonomous Okrug of the Arkhangelsk Region. A long discussion about whether Pai-Khoi is an independent ridge, a continuation of the Urals, its lateral branch, or even connected by origin with the Timan Ridge, ended only in the middle of this century. After the geological structure of Pai-Khoi and the Polar Urals was carefully studied, it became clear that these geographical areas are directly connected and Pai-Khoi should be considered the northwestern continuation of the Urals, a link in the single Ural-Novaya Zemlya folded region.
According to its orographic structure, Pai-Khoi is a rather complex mountainous country, consisting of several parallel mountain ranges and adjacent plateaus. This entire territory belongs to the tundra zone, among which gentle peaks rise with stony placers, and sometimes rocks. The dismemberment of Pai-Khoi and the obliteration of its forms have been repeatedly emphasized by researchers. E. K. Hoffman wrote that Pai-Khoi “has a series of unconnected, rounded and covered with turf mountains, on which stony caps are visible only in some places ...”.
Pai-Khoi is described in approximately the same way by S. V. Kertselli, who pointed out that this range “does not represent a continuous mountain range”, but is a series of “separate narrow, low hillocks elongated along the line of the entire range”. The local population is well aware of the orographic dissection of Pai-Khoi. So, according to Kertselli, "reindeer hunters" distinguish Big Stone - the central part of the ridge, Small Stone (among Komi - Zola-Iz) - its extremely southern ridge, Sea Range - part of Pai-Khoi from Mount Morepai to Yugorsky Shar.
The geographical name Pai-Khoi should have been written Pe-Khoi, but the traditional form, coming from A. I. Schrenk and E. K. Hoffman, has established itself. For the first time this name, apparently, was witnessed by Schrenk during his famous journey to the Polar Urals in 1837.
He writes that the Samoyeds (Nenets) call the western extension of the Urals Paigoy, that is, the "Rocky Range", and the Western Samoyeds (obviously, the Kaninsky and Malozemelsky Nenets) Khabiygoy, that is, the "Ostyak Range", because the Ostyaks (Khanty) roam around it . Somewhat later, the name Pai-Khoi, translating it as “Stone Ridge”, is repeatedly given by Hoffmann, the leader of the North Ural expedition of 1847-1850, who, like Schrenk, personally visited these places and received first-hand information from his Nenets guides and Komi-Zyryans (Izhemtsev).
How to get there
You can get to the More-Iz mountain on foot or on ATVs in summer, in winter - on snowmobiles from the village. Amderma. The journey around the base of the hill takes one day.
Pai Hoi (in Samoyedic "Stone Ridge") - the ridge of the Arkhangelsk province., Mezensky district, begins to the east of Bolsh. Iodnea, stretches towards the WNW, parallel to the coast of the Kara Sea, having reached the Yugorsky shar, passes the island of Vaygach. P.-Khoi appears to be an uplift, completely independent of the Ural Range, from which it is separated by 50 versts by a continuous, swampy and lake-covered plain. The exterior view of the range is a series of unconnected, rounded and turfy mountains, on which stone caps are visible only in some places, rising only in two places to 1000 feet. over the tundra adjacent to the mountains. Pai-Khoi, like the Urals, consists of uplifted Paleozoic layers, which is why the appearance of their rocks is similar to each other. The greatest width of the ridge is between Yumbo-Pai and Pai-dai (between 69° and 70° N latitude). high points P.-Khoya is made up of mountains: Vozay-Pai (1312 feet), Pense-Pai (1045 feet), Big Yodney (1073 feet) and Small Yodney (1005 feet). P.-Khoi, approaching the Yugorsky Shar, gradually lowers and the last rocks, falling into the Shar in steep walls, barely reach 100 feet. height. Snow in August comes across here only occasionally. Through P.-Khoi you can go to the tundra anywhere. Wed "Northern Urals and the P.-Khoi coastal range. Researches of the Ural expedition (St. Petersburg, 1853-56).
encyclopedic Dictionary F. Brockhaus and I.A. Efron. - St. Petersburg: Brockhaus-Efron. 1890-1907 .
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Coordinates: Coordinates: 69°00′00″ s. sh ... Wikipedia
Ridge in the north. parts of the Polar Urals; Nenets ao. The name is from Nenets, pe stone, khoi ridge (stone ridge) or Nenets, share curve, oblique (oblique ridge). The first interpretation is preferable. Geographical names of the world: Toponymic dictionary ... Geographic Encyclopedia
Mountain range in Russia, in the northern part of the Polar Urals. Length over 200 km, height up to 467 m. * * * PAI KHOI PAI KHOI, a mountain range in the northern part of the Polar Urals. The length of St. 200 km, height up to 467 m ... encyclopedic Dictionary
Mountain range in the northern part of the Polar Urals. The length of St. 200 km, height up to 467 m ... Big Encyclopedic Dictionary
PAI KHOI, a mountain range in the northern part of the Polar Urals. The length of St. 200 km, height up to 467 m. Source: Encyclopedia Fatherland ... Russian History
Pai Hoi- Pai Khoi, a mountain range in the northern part of the Polar Urals, in the Nenets Autonomous Okrug. It stretches for 200 km to the Yugorsky Shar Strait. Height up to 467 m (Moreiz). It is composed of crystalline schists, sandstones, marls, limestones. On the… … Dictionary "Geography of Russia"
Pai Hoi- Sp Pái Chòjus Ap Pay Khoy L klng. Urale, RF Nencų apygarda … Pasaulio vietovardziai. Internetinė duomenų bazė
Pai Hoi- ridge in the sowing. parts of the Polar Urals; Nenets ao. The name is from Nenets, pe stone, khoi ridge (stone ridge) or Nenets, share curve, oblique (oblique ridge). The first interpretation is preferable... Toponymic Dictionary
A mountain range stretching from the northern part of the Polar Urals to the Yugorsky Shar Strait. The length is about 200 km. Height up to 467 m (mountain Moreiz). It is composed of crystalline schists, sandstones, marls, limestones. On the slopes of mokhovo ... ... Great Soviet Encyclopedia
Characteristic Length 110 km Basin area 1160 km² Kara Sea basin Watercourse Mouth Lyamin 3rd Location 83 km to the left ... Wikipedia
Books
- Northern Urals and Pai-Khoi coastal range
- Northern Urals and Pai-Khoi coastal range. Volume 1, . Northern Urals and the Pai-Khoi coastal range: Issled. Expeditions, equipment. Imp. Rus. geogr. island in 1847, 1848 and 1850. T. 1F 15/14: St. Petersburg: type. imp. Acad. Sciences, 1853-1856: ...
Orography and hypsometry. The Urals, elongated in the submeridional direction, are subdivided into the Pai-Khoi upland (average heights are 200-400 m, the maximum in More-Iz is 467 m), the Polar Urals (500-1000 m, Payer - 1472 m), the Subpolar Urals (500- 1500 m, Narodnaya town - 1895 m), Northern Urals (500-1000 m, Konzhakovsky Kamen town - 1569 m), Middle Urals (300-500 m), Southern Urals (500-1000 m, Yamantau town - 1640 m), Mugodzhary (200-500 m, Bolshoi Boktybai - 657 m). With a small width mountain belt(50-150 km, up to 15 parallel ridges) the Cis-Urals stand out with a number of hills smoothing the transition from the Russian Plain to the Urals; the Urals proper, consisting of axial (usually nameless) ranges, western and eastern macroslopes; Trans-Urals (narrow - no more than 200 km strip of plains 200-300 m high, sharp orographic boundary).
Geological development and structure. By fixist notions The Ural is a Hercynian folded structure within the vast Ural-Tienshan (or Ural-Mongolian) folded belt. Its development began in the Precambrian, when the accumulation of the most ancient (Archean, Proterozoic, Lower Cambrian) pre-Ural strata that later underwent metamorphism and are currently represented by gneisses, schists, quartzites, and amphibolites. The strata named by N.S. Shatsky stand out in particular. Riphean group (Ancient explorers called the Ural Riphean). In its composition, in addition to metamorphic, terrigenous (conglomerates, sandstones, siltstones) and carbonate (limestones, dolomites, marbles) rocks are widespread. The development of preuralids ended with the Baikal folding. The folds of preuralides extended from the northwest to the southeast. This orientation has been preserved to this day in the Timan Ridge and a number of other structures.
Starting from the Ordovician, the formation and development of the Ural geosyncline, oriented submeridionally, and the accumulation uralide . In the western part of the Urals, the Caledonian folding appeared within the miogeosyncline (non-volcanogenic zone of the geosyncline). The Hercynian folding covered the eastern part and reworked the Caledonian structures of the western Urals. Within the eastern part, there was a eugeosyncline, in which igneous processes and rocks play a significant role.
currently dominated mobilist ideas about the development of the Urals. The geosynclinal process is considered as a result of the “diving” of the oceanic crust of the West Siberian paleoocean under the East European plate of the continental type (subduction). As a result of tectonic crowding, the thickness of the earth's crust increased many times over. The processes caused by the subsidence of the oceanic crust into the zones of metamorphism and melting contributed to the formation of the granite-metamorphic layer. As a result, the crust of the oceanic type was reborn into a continental one. Quite often, the subduction of the oceanic block was replaced by obduction, that is, its thrusting onto the hard edge of the East European Plate. As a result, numerous fragments of the ancient ocean floor are observed on the peaks of the Urals. A significant range of horizontal movement of tectonic covers and ridges is revealed. The roots of the structures are located on the eastern slope of the Urals, and they themselves are often moved to the axial zone, and sometimes to the western slopes. The ancient bottom of the paleoocean consisted of basalt and sedimentary layers. The remains of the first are blocks) consisting of ultrabasic and basic rocks (ophiolite plates), the second are blocks of carbonate rocks (originally carbonate oceanic silts), which are called olistoliths and olistostromes.
As a result of the Hercynian folding and the uplift of a large area, the maritime regime was replaced by a continental one, and the Ural Mountains appeared. According to the laws of isostasy (balance), there was a sinking of the land to the west of the emerging mountains. The resulting Cis-Ural trough was flooded by the waters of lagoons, at the bottom of which, in the Late Carboniferous - Permian, in some places - in the Triassic, mountain destruction products accumulated and molasse deposits formed. All geostructures of the Urals and the deep faults separating them are oriented submeridionally. Geostructures have the form of bands in plan, successively as they move to the east, replacing each other in space. On the border with the Russian plate, there is the Cis-Ural marginal foredeep. Asymmetry is revealed in its section: the eastern flank is deep and steep, the western flank is much less concave. In the process of its development, the trough was constantly advancing to the west, to the eastern edge of the Russian plate. East of the trough, there is an alternation of anticlinoria (Central Ural, East Ural, Zauralsky) and synclinoria (Magnitogorsk-Tagilsky, East Uralsky), and in the eastern part these structures come to the surface only in the south, and in the north they are overlain by the younger cover of the West Siberian Plate.
Minerals. Specificity geological structure causes a wide variety of minerals in the Urals. At short distances, the composition of rocks containing various complexes of minerals changes dramatically. Magmatogenic and metamorphogenic deposits are confined to the East Ural anticlinorium rich in intrusions of various compositions. The granitoid intrusions are associated with deposits of magnetites (skarn deposits of the Magnitnaya, Vysokaya, Blagodat’ mountains), gold in quartz veins, copper, and polymetals. Deposits of chromium, platinum, nickel, cobalt, asbestos, talc, and diamonds are associated with intrusions of basic and ultramafic composition. Alkaline intrusions are due to aluminum deposits. In Bashkiria, in the Riphean strata, there are numerous deposits of siderite, magnetite ores and brown iron ore.
Deposits of sedimentary genesis gravitate towards the Cis-Ural trough. Among them are Solikamskoe (potassium and magnesian salts), Krasnokamskoe and Sol-Iletskoe (rock salt), Vorkuta, Kizelovskoe ( coal), oil and gas fields on the border with the Russian plate. Bauxites (“Little Red Riding Hood”) are mined in ancient weathering crusts. Placer deposits of gold, emeralds and other precious stones have long been known. Rich deposits of building stone are widespread.
Geomorphology. The Hercynian Ural was soon destroyed by denudation. Relief peneplanization lasted during the Mesozoic and Paleogene. Alignment surfaces with weathering crusts formed. Until now, such a surface has not practically changed in Pai-Khoi, Mugodzhary, the Trans-Ural plain of the Southern Urals and in the Middle Urals. At the end of the Oligocene-Neogene, the Urals were covered by the latest tectonic uplifts. It was divided into many blocks by an orthogonal fault system. Along the weakened fault zones, chains of lake basins are located, which is especially characteristic of the eastern macroslope, the basins of lakes and river valleys have acquired a knee-shaped shape in plan. The uplifts were differentiated, differed greatly in intensity, but were not intense everywhere. As already noted, there were almost no uplifts in the Middle Urals, in Pai-Khoi and Mugodzhary. They manifested themselves somewhat stronger in the Northern and Polar Urals. Moderate uplifts covered only the Subpolar and Southern Urals. As a result, the morphostructure of blocky and blocky-folded mountains developed in these territories. Their appearance is characterized by a table shape, steep stepped slopes and a plateau-like or slightly convex surface of the peaks. In areas of weak movements, denudation elevated plains and small hills developed.
In the Pleistocene, the Subpolar Urals was a part of the Ural-Novaya Zemlya glaciation center, the sheet glaciers covered the entire Urals located north of the 60th parallel, and to the south, mountain glaciation centers and snowfields were often found. Under such conditions, a relic glacial and cryogenic morphosculpture of the upper belt of mountains was developed. Modern glaciation has been preserved only in the Subpolar Urals, where modern glacial landforms are limitedly developed. On the other hand, at altitudes above 500 m, modern cryogenic (bald) morphosculpture is widespread. The lower belt is dominated by fluvial morphosculpture with ridge-like watersheds and sharply incised valleys. Due to the wide distribution of carbonate rocks, gypsum and easily soluble salts in many parts of the Urals, especially in the southern Cis-Urals, karst is highly developed. Kapova, Kungurskaya and other caves are especially large. Mugodzhary has arid landforms.
Climate. On the schemes of climatic zoning, the Urals does not form a single region. Its axial zone plays the role of a clear climatic division between the Russian and West Siberian plains. The gradual transformation of the incoming Atlantic air with the western transfer is replaced here by an abrupt change in its characteristics. In the temperate zone, the climate divide separates the Atlantic-continental forest region of the Russian Plain from the continental forest region of the West Siberian Plain. A noticeable increase in the degree of continentality east of the Urals is due to: a. an increase in air temperature amplitudes due to an increase in the severity of winters; b. a decrease in the amount of precipitation due to a decrease in the absolute moisture content of the Atlantic air; V. a clearer expression of the continental precipitation regime (summer maximum and winter minimum precipitation are more pronounced in the Urals than in the Russian Plain).
Throughout the year, cyclonic weather prevails over the northern regions of the Urals, and anticyclonic weather prevails over the southern regions. This is due to the best conditions for overcoming the orographic barrier by the western trajectories (with the northern component) of the Atlantic cyclones in its lowest part, the Pai-Khoi Upland. This is especially pronounced in winter under the conditions of the Kara Hollow of the Icelandic Low. The predominance of anticyclone weather over the south of the Urals is associated in winter with the formation of the western spur of the Siberian High, and in summer with the stationing of anticyclones east of the margin of the Azores High. Significant differences in the conditions of troposphere circulation also determine the difference in weather conditions. Cyclonic weather is characterized by increased cloudiness, prolonged, often drizzling precipitation, increased wind, and softening of temperatures (reducing heat in summer and frost in winter). Anticyclone weather is associated with the dominance of the downward movement of air in the central part of anticyclones, leading to cloud erosion and intensification of radiation processes in the troposphere (anomalously frosty weather sets in in winter, and abnormally hot weather in summer). They are characterized by lack of precipitation and calmness. Sharply excellent weather is observed in the peripheral sections of anticyclones, where long and strong winds are common under the influence of a sharp drop in atmospheric pressure, accompanied in winter by snowstorms and snowstorms with simultaneous softening of frosts.
Along with the western transport of air masses in spring and autumn, the meridional component of the transport increases; AB occurrences are not uncommon to the extreme south of the region; this determines the instability of the weather, unexpected frequent returns of cold weather and frosts in the spring and even (in the circumpolar and polar regions) in the summer. In the warm part of the year, the advection of heat from the neighboring regions of the Kazakh uplands and the Turan plain intensifies.
As for any mountain country, the Urals are characterized by a variegated distribution of climatic indicators across the territory: they differ markedly on slopes of different exposures, in basins, on slopes or peaks, etc. Due to the abundance of orographic basins and the increased severity of winters, they typically appear Siberian weather features, in particular, temperature inversions. On certain days of December in Zlatoust, located at the bottom of the basin, temperatures from -19 to -22 degrees were recorded, on the same dates in the Ivanovsky mine located 400 m higher, they ranged from -0.4 to -5.2 degrees; the average December temperature in Zlatoust is 2 degrees lower than in the Ivanovsky mine. In summer, with normal stratification of the troposphere with a rise of 500 m, the temperature drops by an average of 4 degrees. The widespread occurrence of temperature inversions has led to inversions in the distribution of vegetation (see related section).
Due to seasonal changes in radiation, the change of weather according to the seasons is clearly expressed, as in the entire temperate zone.
For the Urals, a regular change in climatic indicators is typical both as we move from west to east and in the meridional direction, however, the causes and patterns of changes are different. With a large length of the Urals, zonal differences are great. In the north-south direction: a. the values of total radiation and radiation balance increase; b. improved heat supply conditions; V. the amount of precipitation first increases from less than 450 mm at Pai-Khoi to over 800 mm, and then decreases to less than 400 mm at Mugodzhary; d. humidification conditions naturally worsen (from a sharp excess of moisture to excessive, optimal and insufficient moisture); e. The degree of continentality of the climate naturally increases from moderately continental to continental and even sharply continental. Changes in indicators are gradual and similar to their changes in neighboring plains. Zonal changes depend on the seasons. So, the average January temperatures change relatively little - from -22 degrees in the north to -16 degrees in Mugodzhary, but in July they increase from 7 to 25 degrees.
In the west–east direction, the changes are spasmodic in nature, due to the influence of the relief and troposphere circulation, and also change during the year. In this direction, there are sharp differences: a. precipitation and snow cover characteristics b. temperature conditions cold period of the year; V. the degree of continentality of the climate. On the plains of the Cis-Urals, on average, 500 - 800 mm of precipitation falls annually, and the snow cover is up to 60 - 70 cm. barrier of the Urals by air masses, the amount of precipitation increases with height and reaches a maximum in summer in the axial zone, and in winter - on the western macroslope and slopes of the Cis-Ural uplands (in the axial zone and in the basins of the slopes, the conditions of precipitation worsen under the influence of inversions). On the eastern macroslope and especially in the Trans-Urals, the amount of precipitation decreases (by 100–200 mm compared to the west), and three times less water accumulates in the snow cover than in the Cis-Urals.
There are no temperature contrasts between the west and east of the Urals in summer, but they are sharply pronounced in the cold season. This is largely determined by the mechanism of overcoming the mountain structure by air masses. Relatively warm and therefore lighter air that has reached the passes cannot subsequently descend to the surface of the plains of the Trans-Urals, since this is prevented by the local cold and heavy air. Under the influence of a sharp increase in the severity of winters and a decrease in precipitation and moisture supply, the degree of climate continentality also changes abruptly.
Inland waters. The Urals is a watershed between the basins of the Arctic Ocean (and in it - between the basins of the Kara and Laptev Seas) and internal flow (mainly flowing into the Caspian Lake). Within the Urals, the hydrological characteristics of the rivers are similar: they are fed mainly by snow, the flow regime is close to that of Eastern Europe. The main difference is reduced to a much larger volume of the total annual runoff of the rivers of the Cis-Urals in comparison with the Trans-Urals (in a ratio of 3: 1). Reflecting the lattice system of surface dissection, the valleys and riverbeds bend knee-like in plan.
The region stands out as a single Ural mountain-folded groundwater basin. It is characterized by the attraction of the feeding area to the axial zone of the Urals and the presence centrifugal motion water. Along the periphery of the basin, its smooth transition to the hydrogeological basins of neighboring plains is observed: in the west - East European, in the east - West Siberian, playing, especially in winter, a significant role in feeding their rivers.
The Urals is one of the lake regions of Russia. Numerous lakes of the eastern macroslope of the Middle and Southern Urals prevail, the basins of which gravitate towards the zones of tectonic faults and form up to three submeridionally oriented chains, as well as cirque lakes in the altitudinal belt of the glacial relief of the northern part of the region.
Altitudinal zonation. The biogenic components of the nature of the extended and low Urals are subject to the combined influence of both latitudinal zonality, and altitudinal zonality, and longitudinal provinciality. Since the Urals crosses a number of latitudinal zones available on neighboring plains, a regular change is observed in it. types altitudinal zonality: tundra-forest-tundra in Pai-Khoi and the Polar Urals, taiga in the Subpolar, Northern and Middle Urals, deciduous-forest-forest-steppe-steppe in the Southern Urals and semi-desert in Mugodzhary. At the same time, the mountain analogues of the plain zones are shifting much further south in the mountains in comparison with the plains. For example, mountain tundras are widespread in the Urals 100 km south of the southern border of the plain forest-tundras, and fragments of mountain tundras extend as far as the Southern Urals; the mountain belt of the Urals shifts 200 km south of the southern border of the taiga on the plains. This peculiar “hybrid” of zonality and altitudinal zonation received a special name: mountain zonation. The barrier role of the Urals led to various variants of altitudinal belts on the western and eastern macroslopes, which should be regarded as a manifestation of longitudinal provinciality.
The most primitive structure of altitudinal zonality is found in Pai-Khoi and the Polar Urals. Plain tundra and forest tundra are replaced at low (about 200 m or less) absolute heights by mountain tundra on mountain tundra soils. A number of authors single out a belt of cold bald deserts at altitudes of more than 500 m, the main characteristics of which, according to A.A. Makunina /1985/, are the following. A. The leading role of cryogenic processes of relief formation (frost weathering and gravitational processes), which form very dynamic upland terraces and rocky covers (kurums). b. The complete absence of vegetation, except for scale lichens. V. Aggressiveness of bald landscapes due to the year-round accumulation of snow and moisture (precipitation and condensate) on the colluvium and water leakage at the lower boundary of the kurums, which contributes to the growth of bald mountains. Based on a different interpretation of the term “bald mountains” as mountain peaks devoid of forest vegetation /ChESTFG, 1980/, it is better to combine mountain tundra and bald mountains in a single bald belt. In the southern part of the Polar Urals, there is a subalpine belt (sparse spruce-birch and crooked forests, dwarf birches and willows), turning on the plains into larch sparse forests (west) or dark coniferous taiga (west).
The taiga type of altitudinal zonality is most common in the Urals. The structure of altitudinal zonality becomes more complicated due to the dominant mountain-taiga belt. On the western macroslope, it is completely represented by a dark coniferous variant. In the east, as they move south, dark conifers occupy the gradually narrowing upper part of the mountain-taiga belt. At the bottom of this belt southbound accordingly, the width of the strip of light coniferous, mainly pine forests increases. The subalpine (larch sparse forests and oppressed crooked forests with alder, shrub birches, willows) and alpine (mountain tundra and alpine deserts) belts are most developed in the Subpolar and Northern Urals. At low altitudes of the Middle Urals, mountain tundra and alpine meadows are represented only by small fragments. Due to the wide manifestation of temperature inversions in the Middle and Southern Urals, an inversion of altitudinal zones occurs: mountain taiga grows on the bottoms of the basins, either an admixture of broad-leaved or broad-leaved forests (oak, linden, admixture of maple and elm up the slope) appear on the western macroslope, or light coniferous forests with broad-leaved undergrowth - on the eastern macroslope.
The largest number of altitudinal belts is represented in the Southern Urals. Below a narrow strip of dark coniferous (spruce, fir) and relatively wide, developed mainly along the eastern macroslope - light coniferous (pine, larch) mountain taiga belt successively replace each other: a belt of sparse oak crooked forests (on the western macroslope), broad-leaved oak and linden (on western macroslope) or birch (east) forests, mountain forest-steppe, mountainous West Siberian steppe along the eastern macroslope. Above the mountain taiga belt, subalpine (forest meadow with rare spruce and fir) and alpine or alpine (rare fragments of alpine meadows and mountain tundra) are fragmentarily expressed.
In Mugodzhary, the sagebrush-cereal semi-deserts of the foothills give way to mountainous ones and, on rare peaks, fragments of cereal steppes.
Physical-geographical zoning. On all regional (azonal) schemes proposed by many authors physical and geographical zoning of the USSR and Russia, the borders of the Urals are carried out in the same way. Moreover, his eastern border coincides with the boundary allocated by some authors subcontinents/Socava B . B. , Timofeev D.A., 1968, 3 - 19 pp./, which are part of the largely autonomous Asian and European lithospheric plates of the second order (together they make up the Eurasian plate of the first order). The western border of the Urals with the East European Plain is no less clearly defined. All these facts support high degree objectivity of singling out the Urals as an independent physical-geographical country. The criteria for its separation are as follows.
A. Geostructural originality of the Urals (a region of epipaleozoic, mainly epihercynian folding, from the point of view of neomobilism - a zone of interaction of two lithospheric plates) and its significant differences from geostructures neighboring territories(ancient and young platforms).
B. The morphostructural specificity of the Urals (the predominance of blocky and blocky-folded mountains) and its differences from the East European (predominance of layered plains) and West Siberian (predominance of accumulative plains) physical and geographical countries.
B. Macroclimatic criterion: climate, reflecting the impact of the orographic barrier on the nature of climate formation in the temperate zone.
D. The predominance of altitudinal zonality in the formation of biogenic components (instead of the latitudinal-zonal patterns of neighboring plains).
To distinguish units of physical and geographical zoning of the second rank - physical-geographical areas - in mountainous areas, an analysis of the types of altitudinal zonality is used. In the Urals, the types of altitudinal zonality are clearly consistent with the morphosculptural differences in the relief. The latter are perfectly expressed on the ground, which allows them to be used as indicators allocation of physical-geographical areas. To identify units of the third rank, a genetic criterion is used. Previously, the issues of identifying features of the originality of the origin of a particular territory have already been considered (see. general review). The initiating role of recent tectonics was emphasized, as well as the importance of the interrelations of components in the genesis of the nature of regions.
The scheme of physical and geographical division within the Urals is as follows.
I. Area of glacial-cryogenic relief with the development of tundra, forest-tundra, northern and middle taiga in the foothills. The following provinces are distinguished in it: a. Polar-Ural (with Pai-Khoi), b. Subpolar-Ural, c. North Ural.
II. Area of fluvial relief with development in the foothills of the southern taiga and deciduous forests. Provinces: the city of Sredneuralskaya and the village of Yuzhnouralskaya.
Sh. The area of fluvial-arid landforms with the presence of forest-steppe, steppe and semi-desert in the foothills. Provinces: e. Trans-Ural peneplain and g. Mugodzhary.
Area of glacial-cryogenic relief with a change in the foothills of zones from the tundra to the southern taiga was exposed to the impact of highly differentiated newest block uplifts - from very weak (Pai-Khoi) to moderate (Polar Urals), which led to the emergence of various high-altitude steps - an elevated plain (Pai-Khoi), low mountains (the predominant part of the region) and middle mountains (Polar Urals) . The rejuvenation of the mountain relief was most pronounced in the axial zone of the Subpolar Urals and almost did not affect the Pai-Khoi and foothills, in which the surface of the pre-Neogene peneplain is still expressed. The sculptural processing of the relief took place and is taking place in historical time in a harsh climate, which determines the impact of the ancient (Ural-Novaya Zemlya center of the Pleistocene glacier) and modern (Polar Urals) glaciation and cryogenic factors.
Stretched from the coast of the Yugorsky Shar (almost 70 degrees north latitude) to the head of the river. Kosva (59 degrees north latitude), the territory in its northern third is crossed by the Arctic Circle and is located in the polar and subpolar latitudes. The consequence of this is the relatively severe climate of the subarctic zone, the atlantic-arctic and atlantic-continental regions of the temperate zone. Noticeable climate changes as one rises to the mountains create altitudinal zonality of landscapes, which is distinguished by a primitive structure (the dominance of the alpine and subalpine belts and the development of the mountain taiga belt only in the Northern Urals). The landscape differences between the physical and geographical provinces of the region are thus determined by the combined effect of lithogenic and climatic factors within a linearly elongated territory.
Area of fluvial relief with development in the foothills of the southern taiga and deciduous forests been subjected to a particularly strong anthropogenic impact. There is a need for the restoration of primary landscapes and the use of its data in the interests of physical-geographical zoning. Under the influence of the relatively mild climate of the temperate zone, flowing waters become the main factor in the detailing of the relief. A significant contrast of neotectonic uplifts, which noticeably rejuvenated the mountainous relief of the Southern Urals and did not affect the surface of the pre-Neogene peneplain in the rest of the region, makes it possible to clearly contrast the landscape characteristics of the provinces of the Middle and Southern Urals. The altitudinal zonality is characterized by: the dominance of mountain-taiga landscapes, noticeable differences in exposure, and a rather complex structure (in the South Urals).
The area of fluvial-arid morphosculpture with the development of forest-steppe, steppe and semi-desert in the foothills. On the Trans-Ural peneplain and Mugodzhary, the newest uplifts did not appear, the pre-Neogene peneplain was preserved. The climate is distinguished by the best (within the Urals) conditions of heat supply and a noticeable deficit of moisture. Fluvial morphosculpture is represented by modern and relic forms. Arid forms are typical for Mugodzhar. The structure of altitudinal zonation is primitive, steppe and semi-desert landscapes prevail in it.
Mount Konstantinov Stone is considered the northern border of the region, and the Lyapin (Khulga) River is the border with the Subpolar Urals in the south. The area is about 25,000 km.
Mount Payer (1499 m)
Located in the Yamalo-Nenets Autonomous Okrug. Western (South) Payer (1330 m), Eastern Payer (1217 m). The highest mountain in the Polar Urals.
Mount Konstantinov stone (492 m)
Located in the Yamalo-Nenets Autonomous Okrug.
Nerusoveyyakha River
Lyadgeyakha river
Kara River
The length is 257 km. It flows in the Yamalo-Nenets Autonomous Okrug, the Nenets Autonomous Okrug and in the Komi Republic.
Mount Big Minisey (587 m)
Located about 40 km from the Arctic Ocean, it is the extreme point of the Ural Mountains.
Ridge Edeiny
It is the eastern spur of Pai-Khoi.
Waterfall Halmer-Yu
Threshold Big Buridan, Marble Gorge
Pai-Khoi Ridge (467 m)
The highest point of the ridge is Mount Moreiz (467 m). The highest points of Pai-Khoi are the mountains Vozai-Pai (400 m), Pense-Pai (318 m), Big Yodney (327 m) and Small Yodney (306 m)
Mount Grubeiz (1435 m)
Mount Han-mei (1333 m)
Ridge Oche-Nyrd (1338 m)
Mount Lyadgey
Mount Ngetenape (1338 m)
Climate of the Polar Urals
The climate of the Polar Urals is harsh, sharply continental; cold rainy autumn quickly gives way to winter, and a short cool spring - in summer. Usually, already in early September, the tops of the ridges are covered with a blanket of snow, and only in June the snow begins to melt in the mountains.
Winter - with heavy snowfalls, heavy snowstorms and snowstorms, long and very frosty. In December-February, on the foothill plains, the temperature sometimes drops to -50 ... -54 °, and in July it rises to + 31 °. In the mountains - on the most elevated plateaus, ridges and massifs, winter is about a month longer than on the plains; it lasts here 8-9 months, but frosts are weaker than on the plains, and rarely reach 45 °.
In anticyclonic - clear, calm and frosty - weather high in the mountains, a temperature inversion is observed, when it is 15-25 ° warmer at the top than in the river valleys and on the foothill plains. This is due to the fact that colder, and therefore denser and heavier air flows down from the mountains and stagnates in the valleys and on the plains. On the contrary, during the invasion of cyclones - with winds and snowfalls - it is warmer in the foothills than in the mountains: for every 100 m of altitude, the air temperature drops by about 0.6 °.
There is a lot of precipitation in the Polar Urals: in the mountains from 800 to 1200 mm per year, and on the western slope it is 2-3 times more than on the eastern one; on the plains, the amount of precipitation decreases to 400-600 mm, of which about half falls in winter, and the rest in spring, summer and autumn. The average annual air temperature in various regions of the Polar Urals varies from -5 to -8°. The coldest month is February. The average February temperature in the mountains and on the plains is about 19° below zero. Almost as cold in December, January and March.
The average temperature of these months is nowhere above -16°. It becomes much warmer only in April (from -8...-9° in the plains to -10...-12° in the mountains). In May, the snow begins to melt on the plains, they open up, but at night it is still frosty and the average monthly air temperature is negative (-2 ° on the plain, up to -5 ° in the mountains).
