Pai Hoi Ridge. Pai-hoi See what "Pai-Hoi" is in other dictionaries
It consists of several parallel mountain ranges and adjacent plateaus.
The name of the Pai-Khoi ridge comes from the Nenets words Pe-Khoi, meaning “stone ridge”.
Pai-Khoi stretches in length from southeast to northwest for as much as 200 kilometers - from the northern part of the Polar Urals to the Yugorsky Shar Strait. Part of the ridge goes further - under the waters of the strait, traced on the island of Vaygach. Pai-Khoi is separated from the Polar Urals by a 40-kilometer stretch of tundra.
The height of the ridge, heavily destroyed by time and nature, is small - from 200 to 400 meters above sea level. The highest point of Pai Khoi is Mount More-Iz(467 m), is located near the left bank of the Talota River, 70 km east-southeast of the Yugorsky Shar Strait. It is interesting that the older name of the mountain (Nenets) is Vasaimbai (or Vazai-Pai, Vesey-Pe) - Starikov Rock, Mount Startsev. The modern name of the peak - More-Iz - arose in the 19th-20th centuries from the Komi reindeer herders. Consists of the Russian word “sea” (from the top you can see the Kara Sea) and the Komi word “iz” - “stone”, “mountain”.
The most significant peak of the mountain range near the sea is mountain Syvym-Pe(translated from Nenets as “winter stone”), is located in the extreme north-west of the Yugra Peninsula. Researcher A.I. Schrenk wrote about it: “Suvvumbai is a winter rock, so named after the many lakes that, being in its vicinity, abound in fish and wild geese, so that Samoyeds, stocking up on food supplies here during the summer, can easily winter in this place.”
The most mysterious peak of Pai-Khoi is located in the extreme west of the ridge, near the sea. Its name - Sirtya-Pe, which means “Sirtya Mountain” from Nenets. The Sirtyayakha River - “Sirtya River” - begins nearby. Sirtya is a legendary people from Nenets legends. These are little people who live underground and sometimes come to the surface. Russians, including those in the Urals, have similar legends (about the white-eyed miracle). Apparently, some extinct people used to live here.
Pai Khoi on the map of the 1847-48 expedition.
Pai Khoi is composed of siliceous and clayey shales, sandstones and limestones.
The mountain range is heavily dissected by rivers. In fact, it is not a continuous mountain range, but a series of individual hills.
The vegetation here is sparse, mountain-tundra. Below the slope there are mosses and lichens, and in some places you can see willow and dwarf birch. Altitudinal zonation is not observed.
The climate on Pai Khoi is harsh and cold - subarctic. The duration of winter is 230 days. The average annual temperature is only -9º. This is the kingdom of permafrost.
The first scientist to visit the Pai-Khoi area was a biologist and mineralogist, an employee of the Imperial Botanical Garden A.I. Schrenk. This happened in August 1837. However, he did not see a single ridge in these bare hills. Based on this trip, the work “Journey to the North-East of European Russia” was published in 1855.
In 1848, Pai Khoi was visited by a scientific expedition of the Russian Geographical Society under the leadership of E.K. Hoffman. A geological and biological description of the ridge was compiled. The results of the expedition were published in the work “Northern Urals and the Pai-Khoi Coastal Range.”
Let me give just a small excerpt from this book:
“Here it is clear that the mountains do not lie in a continuously extended ridge of rocks, like the Urals, as it seemed from the banks of the Kara, but that they form a system of many long chains of mountains and hills, which do not lie parallel to one another, do not follow one another; on the contrary, each of them, being separated from the others by the tundra, has its own special longitudinal chain... Pai-Khoi can be called a ridge, cut to the very bottom by many deep valleys, in which swamps and lakes have formed, covering the rocky soil.”
It is interesting that one of the expedition members bought a black fox from the Samoyeds, which was sitting here on a chain. And he even brought her to St. Petersburg.
M.V. Malakhov in his review of the Urals wrote:
“With the end of the Urals, as if in its place, at the same latitude or somewhat to the south, on the western side of the ridge, there is a long branch, directly heading to the Yugorsky Bay and the Vaigach Island. This branch, like the Timan Mountains, was not known until very recently, until 1853-6, and was described by the Ural expedition under the name of the Pai-Khoi Coast Range. It ends at the shore of the Ugra Bay and is separated from the Urals by vast, swampy tundra.
The silent and eternally dull, monotonous tundra stretches across an immense expanse, drowning in the north in the waves of an inhospitable sea, and on the other side bordered by the ever-green taiga.
Only the stern Pai-Khoi, crashing into the very ocean, violated the usual, humiliated character of the tundra and sadly and unfriendlyly the area looks around at the desolate lowlands. All living things flee from this icy kingdom, even a hard stone, forged like damask steel, and even that crumbles into dust and, with the help of fierce winds, spreads into fine sand. Resin moss and cuckoo flax are almost the only objects of the plant kingdom, except that occasionally, a little further south on the river bank you will see a skinny flower and a squat spruce and birch tree.
Pai-Khoi, this is the northernmost ridge of mountains, which, although it represents a partly independent treeless rise, is separated from the Ural ridge by mossy taiga, although it gradually deviates from the general direction, nevertheless, it serves as its last link.”
Administratively, Pai-Khoi is located in the Nenets Autonomous Okrug of the Arkhangelsk Region, on the Yugra Peninsula. Getting to Pai Khoi is not easy; you need to book a transfer by all-terrain vehicle or helicopter.
Pai Hoi (in Samoyed "Stone Ridge") - the ridge of the Arkhangelsk province, Mezensky district, begins to the east of the Bolshoi. Iodneya, stretches in the direction of the WNW, parallel to the shore of the Kara Sea, having reached the Yugorsky ball, it passes to Vaygach Island. P.-Khoy appears to be a rise completely independent of the Ural ridge, from which it is separated by 50 versts by a continuous, swampy plain covered with lakes. The appearance of the ridge is a series of unconnected, rounded and turf-covered mountains, on which only in some places are visible rock caps, rising only in places in two per 1000 feet. over the tundra adjacent to the mountains. Pai-Khoi, like the Urals, consists of uplifted Paleozoic strata, 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° north latitude). The highest points of P.-Khoy are the following mountains: Vozay-Pai (1312 ft.), Pense-Pai (1045 ft.), Bolshoi Iodney (1073 ft.) and Small Iodney (1005 ft.). P.-Khoy, approaching the Yugorsky Shar, gradually decreases and the last rocks, falling into the Shar with steep walls, barely reach 100 feet. height. Snow occurs here only occasionally in August. Through P.-Khoi you can go to the tundra anywhere. Wed. "Northern Urals and the P.-Khoi coastal ridge. Research of the Ural expedition (St. Petersburg, 1853-56).
Encyclopedic Dictionary F.A. Brockhaus and I.A. Efron. - S.-Pb.: Brockhaus-Efron. 1890-1907 .
See what "Pai-Hoi" is in other dictionaries:
Coordinates: Coordinates: 69°00′00″ N. w... Wikipedia
Ridge in the north parts of the Polar Urals; Nenets Autonomous Okrug The name is from Nenets, pe stone, khoy khrebet (stone ridge) or Nenets, pai krivoy, kosoy (oblique ridge). The first interpretation is preferable. Geographical names of the world: Toponymic dictionary... Geographical 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. Length St. 200 km, height up to 467 m... encyclopedic Dictionary
Mountain range in the northern part of the Polar Urals. Length St. 200 km, height up to 467 m... Big Encyclopedic Dictionary
PAI KHOI, a mountain range in the northern part of the Polar Urals. Length 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 shales, sandstones, marls, and limestones. On the… … Dictionary "Geography of Russia"
Pai Hoi- Sp Pái Chòjus Ap Pai Khoy/Pay Khoy L klng. Urale, RF Nencų apygarda … Pasaulio vietovardžiai. Internetinė duomenų bazė
Pai Hoi- ridge in the north. parts of the Polar Urals; Nenets Autonomous Okrug The name is from Nenets, pe stone, khoy khrebet (stone ridge) or Nenets, pai krivoy, kosoy (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 (Mount Moreiz). It is composed of crystalline shales, sandstones, marls, and limestones. On the slopes of mokhovo... ... Great Soviet Encyclopedia
Characteristics Length 110 km Basin area 1160 km² Basin Kara Sea Watercourse Estuary Lyamin 3rd · Location 83 km to the left ... Wikipedia
Books
- Northern Urals and the Pai-Khoi coastal ridge
- Northern Urals and the Pai-Khoi coastal ridge. Volume 1, . Northern Urals and the Pai-Khoi coastal ridge: Research. Expeditions, equipment. Imp. Rus. geogr. island in 1847, 1848 and 1850. T. 1F 15/14: St. Petersburg: typ. imp. Academician Sciences, 1853-1856:...
Orography and hypsometry. Elongated in the submeridional direction, the Urals are divided into the Pai-Khoi hill (average heights 200-400 m, maximum in the city of More-Iz - 467 m), Polar Urals (500-1000 m, Payer - 1472 m), Subpolar Urals (500- 1500 m, Narodnaya - 1895 m), Northern Urals (500-1000 m, Konzhakovsky Kamen - 1569 m), Middle Urals (300 - 500 m), Southern Urals (500 - 1000 m, Yamantau - 1640 m), Mugodzhary (200-500 m, Bolshoi Boktybay – 657 m). With a small width of the mountain belt (50-150 km, up to 15 parallel ridges), the Cis-Urals are distinguished with a number of hills that smooth out the transition from the Russian Plain to the Urals; the Urals proper, consisting of axial (usually nameless) ridges, 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 ideas The Urals is a Hercynian folded structure within the huge Ural-Tyanshan (or Ural-Mongolian) fold belt. Its development began in the Precambrian, when the accumulation of the most ancient (Archaean, Proterozoic, Lower Cambrian) took place. pre-Ural strata that later underwent metamorphism and are currently represented by gneisses, crystalline schists, quartzites, and amphibolites. Particularly prominent are the strata named by N.S. Shatsky Riphean group (Ancient researchers called the Urals Riphean). In its composition, in addition to metamorphic ones, terrigenous (conglomerates, sandstones, siltstones) and carbonate (limestones, dolomites, marbles) rocks are widespread. The development of the pre-uralids ended with the Baikal folding. The pre-uralid folds extended from northwest to 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 of uralid . In the western part of the Urals, 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 magmatic processes and rocks play a significant role.
Currently dominate mobilist ideas about the development of the Urals. The geosynclinal process is considered as a result of the “subduction” of the oceanic crust of the West Siberian paleoocean under the East European continental plate (subduction). As a result of tectonic clustering, the thickness of the earth's crust increased many times over. The processes caused by the subsidence of the oceanic crust into zones of metamorphism and melting contributed to the emergence of a granite-metamorphic layer. As a result, the oceanic type crust degenerated into continental one. Quite often, the subduction of an 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 nappes and overhangs 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 uplift of a large territory, the marine regime was replaced by a continental one, and the Ural Mountains appeared. According to the laws of isostasy (equilibrium), the land to the west of the emerging mountains subsided. The resulting Cis-Ural trough was flooded by the waters of lagoons, at the bottom of which in the Late Carboniferous - Permian, and in sections - in the Triassic, the products of mountain destruction accumulated and molasse deposits were formed. All geostructures of the Urals and the deep faults separating them are oriented submeridionally. The geostructures have the form of stripes in plan, successively replacing each other in space as they move to the east. On the border with the Russian plate there is the Pre-Ural foredeep. Its section reveals an asymmetry: the eastern wing is deep and steep, the western wing is much less bent. In the process of its development, the trough constantly moved westward, to the eastern edge of the Russian Plate. To the east of the trough, there is an alternation of anticlinoriums (Central Ural, East Ural, Trans-Ural) and synclinoriums (Magnitogorsk-Tagil, East Ural), and in the eastern part these structures come to the surface only in the south, and in the north they are covered by a younger cover of the West Siberian plate.
Minerals. The specific geological structure determines the wide variety of minerals in the Urals. Over short distances, the composition of rocks containing various mineral complexes changes dramatically. Magmatic and metamorphogenic deposits are confined to the East Ural anticlinorium, rich in intrusions of various compositions. Associated with granitoid intrusions are deposits of magnetites (skarn deposits of the Magnitnaya, Vysokaya, and Blagodati mountains), gold in quartz veins, copper, and base metals. Deposits of chromium, platinum, nickel, cobalt, asbestos, talc, and diamonds are associated with mafic and ultramafic intrusions. Aluminum deposits are responsible for alkaline intrusions. In Bashkiria, in the Riphean strata, there are numerous deposits of siderite, magnetite ores and brown iron ores.
Deposits of sedimentary origin gravitate towards the Cis-Ural trough. Among them are Solikamskoye (potassium and magnesium salts), Krasnokamskoye and Sol-Iletskoye (rock salt), Vorkutinskoye, Kizelovskoye (hard coal), oil and gas fields on the border with the Russian plate. Bauxite (“Little Red Riding Hood”) is 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 Urals were soon destroyed by denudation. The peneplanation of the relief lasted during the Mesozoic and Paleogene. Leveling surfaces with weathering crusts formed. This surface has practically not changed to this day in Pai-Khoi, Mugodzhary, the Trans-Ural Plain of the Southern Urals and the Middle Urals. At the end of the Oligocene-Neogene, the Urals were covered by new tectonic uplifts. It was divided into many blocks by an orthogonal fault system. Along weakened fault zones there are chains of lake basins, which is especially typical for the eastern macroslope; lake basins and river valleys have acquired a knee-shaped plan. The uplifts were differentiated and varied greatly in intensity, but were not intense everywhere. As already noted, almost no uplifts appeared in the Middle Urals, in Pai-Khoi and Mugodzhary. They manifested themselves somewhat more strongly in the Northern and Polar Urals. Moderate uplifts covered only the Subpolar and Southern Urals. As a result, the morphostructure of block and block-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 have developed.
In the Pleistocene, the Subpolar Urals were part of the Ural-Novaya Zemlya glaciation center, cover glaciers covered the entire Urals located north of the 60th parallel, and to the south there were often pockets of mountain glaciation and snowfields. Under such conditions, the relict glacial and cryogenic morphosculpture of the upper mountain belt was developed. Modern glaciation has survived only in the Subpolar Urals, where modern glacial landforms are limitedly developed. But at altitudes above 500 m, modern cryogenic (char) morphosculpture is widespread. The lower zone 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 in size. Mugodzhary has arid landforms.
Climate. On climatic zoning schemes, the Urals do not form a single region. Its axial zone plays the role of a clear climatic divide between the Russian and West Siberian plains. The gradual transformation of the Atlantic air arriving with the westerly transport 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 increased severity of winters; b. a decrease in 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 clearly expressed in the Urals than on 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 Atlantic cyclones traveling along western trajectories (with a northern component) in its lowest part - the Pai Khoi Hill. This is especially pronounced in winter in the conditions of the Kara depression of the Icelandic low. The dominance of anticyclonic 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 stationary anticyclones east of the edge of the Azores High. Significant differences in tropospheric circulation conditions also cause differences in weather conditions. Cyclonic weather is characterized by increased cloudiness, prolonged, often drizzling precipitation, increased wind, and milder temperatures (in the summer the heat decreases, in the winter – frost). Anticyclonic weather is associated with the dominance of downward air movement in the central part of anticyclones, leading to erosion of clouds and intensification of radiation processes in the troposphere (abnormally frosty weather occurs in winter, and abnormally hot weather in summer). They are characterized by a lack of precipitation and calm wind. Sharply different weather is observed in the peripheral areas of anticyclones, where prolonged and strong winds are common under the influence of a sharp drop in atmospheric pressure, accompanied in winter by blizzards and snowstorms with a simultaneous softening of frosts.
Along with the western transfer of air masses in spring and autumn, the meridional component of the transfer intensifies, and occurrences of AVs to the extreme south of the region are not uncommon; This determines the instability of the weather, unexpected frequent returns of cold weather and frosts in the spring and even (in the subpolar and polar regions) in the summer. In the warm part of the year, heat advection from neighboring areas of the Kazakh hillocks and the Turan Plain intensifies.
Like any mountainous country, the Urals are characterized by a varied distribution of climatic indicators across the territory: they differ noticeably 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 manifest Siberian weather patterns, 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, at the same time 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 decreases by an average of 4 degrees. Widespread temperature inversions have led to inversions in the distribution of vegetation (see the corresponding section).
The change in weather between seasons, caused by seasonal changes in radiation, is clearly expressed, as in the entire temperate zone.
The Urals are characterized by a regular change in climatic indicators both as they move from west to east and in the meridional direction, but the reasons and patterns of changes are different. Given the great extent of the Urals, zonal differences are large. In the north-south direction: a. the values of total radiation and radiation balance increase; b. heat supply conditions are improved; V. 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. moisture conditions naturally worsen (from a sharp excess of moisture to excessive, optimal and insufficient moisture); d. The degree of continental climate naturally increases from temperate continental to continental and even sharply continental. Changes in indicators are gradual and similar to their changes on neighboring plains. Zonal changes depend on the seasons. Thus, average temperatures in January 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, changes are discontinuous, caused by the influence of relief and tropospheric circulation, and also change throughout the year. In this direction they differ sharply: a. precipitation amount and snow cover characteristics b. temperature conditions of the cold period of the year; V. degree of continental climate. On the plains of the Cis-Ural region, on average, 500 - 800 mm of precipitation falls per year, and the height of the snow cover is up to 60 - 70 cm. Due to the activation and stagnation of Atlantic (all year round) and Mediterranean (in winter in the southern half of the mountain structure) cyclones, orographic precipitation falls when overcoming 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 the slopes of the Cis-Ural uplands (in the axial zone and in the basins of the slopes, precipitation conditions 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 the snow cover accumulates three times less water than in the Cis-Urals.
Temperature contrasts between the west and east of the Urals are absent in the summer, but are sharply expressed in the cold season. This is largely determined by the mechanism by which air masses overcome the mountain structure. The relatively warm and therefore lighter air that has reached the passes cannot subsequently descend to the surface of the Trans-Ural plains, 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 availability, the degree of continental climate 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 drainage (mainly flowing into the Caspian Lake). Within the Urals, the hydrological characteristics of the rivers are similar: they are fed predominantly by snow, and the flow regime is close to that of Eastern Europe. The main difference comes down to the significantly larger volume of the total annual flow of the rivers of the Urals compared to the Trans-Urals (in a ratio of 3: 1). Reflecting the lattice system of surface dissection, valleys and river beds bend in a knee-like manner in plan.
The region stands out as a single Ural mountain-fold groundwater basin. It is characterized by the gravity of the feeding area towards the axial zone of the Urals and the presence of centrifugal movement of water. Along the periphery of the basin there is a smooth transition into the hydrogeological basins of the neighboring plains: in the west - the Eastern European, in the east - the Western Siberian, playing, especially in winter, a significant role in feeding their rivers.
The Urals are one of the lake regions of Russia. Numerous lakes of the eastern macroslope of the Middle and Southern Urals predominate, the basins of which gravitate towards zones of tectonic faults and form up to three submeridionally oriented chains, as well as tarn lakes in the high-altitude belt of the glacial relief of the northern part of the region.
Altitudinal zone. The biogenic components of the nature of the extended and low Urals are subject to the combined influence of latitudinal zonality, altitudinal zonality, and longitudinal provinciality. Since the Urals crosses a number of latitudinal zones found on neighboring plains, there is a natural change in types altitudinal zone: 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 lowland zones are shifted much further south in the mountains compared to the plains. For example, mountain tundras are widespread in the Urals, 100 km south of the southern border of lowland forest-tundras, and fragments of mountain tundras extend all the way to 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 latitudinal zonation. The barrier role of the Urals has led to different variants of altitudinal belts on the western and eastern macroslopes, which should be regarded as a manifestation of longitudinal provincialism.
The most primitive structure of altitudinal zonation is revealed in Pai-Khoi and the Polar Urals. Plain tundra and forest-tundra are replaced at low (about 200 m or less) absolute altitudes by mountain tundras on mountain-tundra soils. A number of authors identify a belt of cold alpine deserts at altitudes above 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), forming very dynamic mountain terraces and rocky covers (kurums). b. Complete absence of vegetation, except crustose lichens. V. The aggressiveness of char landscapes is caused by the year-round accumulation of snow and moisture (precipitation and condensate) on colluvium and the leakage of water at the lower border of the kurums, which contributes to the growth of char. Based on another interpretation of the term “chars” as mountain peaks devoid of forest vegetation /CHESTFG, 1980/, it is better to combine mountain tundras and chars as part of a single char belt. In the southern part of the Polar Urals, a subalpine belt can be traced (spruce-birch sparse 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 zone is most common in the Urals. The structure of the altitudinal zone is complicated by the dominant mountain-taiga belt. On the western macroslope it is entirely represented by the dark coniferous variant. In the east, as they move south, dark conifers occupy the gradually narrowing upper part of the mountain taiga belt. In the lower part of this belt in the southern direction, the width of the strip of light-coniferous, mainly pine forests increases accordingly. The sub-goltsy (larch open forests and oppressed crooked forests with alder, shrubby birches, willows) and goltsy (mountain tundra and goltsy deserts) belts are most developed in the Subpolar Northern Urals. At low altitudes of the Middle Urals, mountain tundras and alpine meadows are represented only by small fragments. Due to the widespread 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, higher up either an admixture of broad-leaved or broad-leaved forests (oak, linden higher up the slope, an admixture of maple and elm) appear on the western macroslope, or light coniferous forests with broad-leaved undergrowth - on the eastern macroslope.
The largest number of altitudinal zones is represented in the Southern Urals. Below the 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 (eastern) forests, mountain forest-steppe, mountainous West Siberian steppe along the eastern macroslope. Above the mountain taiga belt, the subalpine zone (forest meadow with rare spruce and fir) and the alpine or goltsy zone (rare fragments of alpine meadows and mountain tundras) are fragmentarily expressed.
In Mugodzhary, the wormwood-cereal semi-deserts of the foothills are replaced with height by mountain ones and, on rare peaks, by fragments of cereal steppes.
Physico-geographical zoning. In all the regional (azonal) schemes of physical-geographical zoning of the USSR and Russia proposed by many authors, the boundaries of the Urals are drawn in the same way. Moreover, its eastern border coincides with the border of those identified by some authors subcontinents/Sochava V . 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 testify in favor of a high degree of objectivity in identifying the Urals as an independent physical-geographical country. The criteria for its isolation are as follows.
A. Geostructural uniqueness of the Urals (the area of epi-Paleozoic, mainly epi-Hercynian folding, from the point of view of neomobilism - a zone of interaction between two lithospheric plates) and its significant differences from the geostructures of neighboring territories (ancient and young platforms).
B. Morphostructural specificity of the Urals (predominance of block and block-folded mountains) and its differences from the Eastern European (predominance of stratified plains) and Western Siberian (predominance of accumulative plains) physical and geographical countries.
B. Macroclimatic criterion: climate reflecting the impact of an orographic barrier on the nature of climate formation in the temperate zone.
D. The predominance of altitudinal zonation in the formation of biogenic components (instead of the latitudinal patterns of neighboring plains).
To identify units of physical-geographical zoning of the second rank - physical and geographical areas - in mountainous areas, analysis of altitudinal zonation types is used. In the Urals, the types of altitudinal zonation 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 identifying physical and geographical areas. To identify units of the third rank, a genetic criterion is used. Previously, the issues of identifying the unique features 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 interconnections of components in the genesis of the nature of the regions.
The physical-geographical division scheme within the Urals is as follows.
I. An area of glacial-cryogenic relief with the development of tundra, forest-tundra, northern and middle taiga in the foothills. It identifies the provinces: a. Polarno-Uralskaya (with Pai-Khoi), b. Subpolar-Uralskaya, c. North Ural.
II. An area of fluvial relief with the development of southern taiga and deciduous forests in the foothills. Provinces: Sredneuralskaya city and Yuzhnouralskaya village.
Sh. Region of fluvial-arid relief forms with the presence of forest-steppe, steppe and semi-desert in the foothills. Provinces: f. Trans-Ural peneplain and g. Mugodzhary.
An area of glacial-cryogenic relief with a change in the foothills of zones from the tundra to the southern taiga was exposed to the influence of highly differentiated new block uplifts - from very weak (Pai-Khoi) to moderate (Subpolar Urals), which led to the emergence of various high-altitude stages - elevated plain (Pai-Khoi), low mountains (the predominant part of the region) and middle mountains (Subpolar Urals) . The rejuvenation of mountain relief was most pronounced in the axial zone of the Subpolar Urals and almost did not affect Pai-Khoi and the foothills, in which the surface of the pre-Neogene peneplain is still expressed. The sculptural processing of the relief took place and is being carried out in historical times under harsh climate conditions, causing the influence of ancient (Ural-Novaya Zemlya center of the Pleistocene glacier) and modern (Subpolar Urals) glaciation and cryogenic factors.
Extended from the coast of Yugorsky Shar (almost 70 degrees N) to the sources of the river. Kosva (59 degrees N) the territory in its northern third is crossed by the Arctic Circle and is located in polar and subpolar latitudes. The consequence of this is the relatively harsh climate of the subarctic zone, the Atlantic-Arctic and Atlantic-continental regions of the temperate zone. Noticeable climate changes as one rises into the mountains create an altitudinal zonation of landscapes, characterized 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). Landscape differences in the physical and geographical provinces of the region are thus determined by the combined influence of lithogenic and climatic factors within a linearly elongated territory.
An area of fluvial relief with the development of southern taiga and deciduous forests in the foothills has been subjected to particularly strong anthropogenic influence. There is a need to restore primary landscapes and use its data in the interests of physical and 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. The 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, allows us to clearly contrast the landscape characteristics of the provinces of the Middle and Southern Urals. The altitudinal zone is characterized by: the dominance of mountain taiga landscapes, noticeable differences in exposure and a rather complex structure (in the Southern Urals).
An 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 latest uplifts did not appear; the pre-Neogene peneplain was preserved. The climate is characterized by the best (within the Urals) heat supply conditions and a noticeable lack of moisture. Fluvial morphosculpture is represented by modern and relict forms. Arid forms are typical for Mugojar. The structure of altitudinal zones is primitive, it is dominated by steppe and semi-desert landscapes.
The northern border of the region is considered to be Mount Constantine Stone, and in the south the border with the Subpolar Urals is the Lyapin (Khulga) River. Area - about 25,000 km.
Mount Payer (1499 m)
Located in the Yamalo-Nenets Autonomous Okrug. Western (Southern) Payer (1330 m), Eastern Payer (1217 m). The highest mountain of the Polar Urals.
Mount Constantine Stone (492 m)
Located in the Yamalo-Nenets Autonomous Okrug.
Nerusoveyakha River
Lyadgeyakha River
Kara River
Length 257 km. It flows in the Yamalo-Nenets Autonomous Okrug, the Nenets Autonomous Okrug and the Komi Republic.
Mount Big Minisey (587 m)
Located approximately 40 km from the Arctic Ocean, it is the extreme point of the Ural Mountains.
Edeyniy Ridge
It is the eastern spur of Pai-Khoi.
Halmer-Yu waterfall
Great Buridan Threshold, 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)
Oche-Nyrd ridge (1338 m)
Mount Lyadgei
Mount Ngetenape (1338 m)
Climate of the Polar Urals
The climate of the Polar Urals is harsh, sharply continental; a cold, rainy autumn quickly gives way to winter, and a short, cool spring to summer. Usually, already in early September, the tops of the ridges are covered with a blanket of snow, and only in June does the snow begin to melt in the mountains.
Winter - with heavy snowfalls, strong snowstorms and blizzards, long and very frosty. In December-February on the foothill plains the temperature sometimes drops to -50...-54°, and in July 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 for 8-9 months, but the frosts are weaker than on the plains and rarely reach 45°.
During anticyclonic weather - clear, windless and frosty - a temperature inversion is observed high in the mountains, when at the top it is 15-25° warmer than in river valleys and foothill plains. This happens because colder, and therefore denser and heavier air flows down from the mountains and stagnates in the valleys and 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; on the plains, precipitation decreases to 400-600 mm, of which approximately 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 plains is about 19° below zero. Almost as cold in December, January and March.
The average temperature of these months is nowhere higher than -16°. It becomes significantly warmer only in April (from -8...-9° on the plain to -10...-12° in the mountains). In May, the snow begins to melt on the plain and open up, but at night there is still frost and the average monthly air temperature is negative (-2° on the plain, up to -5° in the mountains).
Pai Hoi- an old, heavily destroyed mountain range in the center of the Yugra Peninsula. The rocky ridges and hills that form it stretch for about 200 km from the northern part of the Polar Urals to the Yugorsky Shar Strait, and their continuation can be traced on Vaygach Island, separating the Barents and Kara Seas. Pai Khoi is located in the extreme northeast of the European part of Russia. To the west and southwest of it lies the Pechora Lowland and the Korotaikha River, to the southeast and east are the western slopes of the Polar Urals and the lower reaches of the Kara River, and to the north lies the Kara Sea. The highest point of the ridge is Mount Moreiz (Vesey-Pe) (423 m above sea level), which is the highest point on the surface of the Nenets Autonomous Okrug. Pai-Khoi is composed of siliceous and clayey shales, limestones, and sandstones. The ridge does not form a continuous mountain chain and consists of a number of isolated hills. At the same time, the western slope of Pai-Khoi is relatively short, and the eastern slope is gentle, descending towards the Kara Sea with wide sea terraces.
