Geological monuments of nature. "geological monuments of the European part of Russia"

1. Burpala alkaline massif
2. Yoko-Dovyren gabbro-peridotite complex
3. Sections of the Akitkan Proterozoic Series along the Goudzhekit and Kunerma rivers
4. Ophiolite massif of Cape Thin
5. Botovskaya cave
6. Thermal spring Khakusy
7. Kotelnikovsky source of thermal siliceous waters
8. Allinskie springs of thermal fresh waters
9. Seismotectonic structure of Shartle
10. Insky rock garden
11. Bodies of holy bearers of the Svyatoy Nos Peninsula
12. Cheremkhoskoye coal deposit
13. Cretaceous-Paleogene weathering crust of Sarayskaya Bay
14. rift basin
15. Paleozoic complexes of the Olkhon region and the islands
16. Goryachinsky thermal spring
17. Location of the Jurassic continental biota of Ust-Baley
18. Tazheran alkaline massif
19. Marakta source of mineral waters
20. Weathering remnants and deposits of pebbles in Peschanaya Bay
21. Calcite Cave
22. Diaphtorites of the Zyrkuzun loop
23. Metasomatic complexes of Belaya Vyemka
24. Slyudyansky mining area
25. Location of rare minerals Utochkina Pad
26. Ermakovskoe fluorite-phenacite-bertrandite deposit
27. Tankhoy system of seismic dislocations
28. Seismogenic structure Snezhnaya
29. Location of the remains of the Pliocene Urunga
30. Location of early Jurassic insects Novospasskoye

• Active volcano Shiveluch
• Active volcano Klyuchevskaya Sopka
• Active volcano Bezymyanny
• Cinder cones of the Great Fissure Tolbachik Eruption
• Active volcano Ichinskaya Sopka
• Active volcano Kronotskaya Sopka
• Volcano Khangar
• Volcanic ultramafic complex of the Valagin ridge
• Active volcano Kikhpinych
• Uzon volcano caldera
• Active volcano Krasheninnikov
• Active Volcano Bolshoi Semyachik
• Valley of Geysers14 Maly Semyachik active volcano
• Active volcano Karymskaya Sopka
• Active volcano Avachinskaya Sopka
• Active volcano Gorely
• Active volcano Sopka Opala

The national heritage of any state is a lot, including a variety of monuments: historical, cultural, archaeological, natural. Among the latter are separate objects of animate and inanimate nature, whose scientific, educational, educational, historical, memorial or cultural and aesthetic significance is so great that it forces the state and the population to ensure their safety in order to pass them on from generation to generation. The monuments of inanimate nature include geological objects.

Decree of the Government of the Russian Federation No. 900 of December 26, 2001 established for the first time that the protection of geological objects of scientific, cultural, aesthetic and other significance should be carried out within the framework of the previously adopted Federal Law “On Specially Protected Natural Territories” No. 33-FZ of March 14. 1995.
Like specially protected natural areas, geological objects can be of federal, regional and local importance and protected, respectively, at the federal, regional and local levels.

Along with this, a small part of the country's geological objects is currently protected not as natural areas, but as cultural monuments (some caves, ancient mines), as well as museums-reserves (for example, the Marcial Waters museum-reserve in), which, like specially protected natural areas, are also ranked according to their significance (federal, regional and local importance).

The rank of geological objects protected and proposed for protection is not legally regulated and is determined solely by their scientific, cultural and aesthetic significance. According to these criteria, global, supra-regional, regional and local ranks of geological objects are distinguished. Only geological objects of global and supra-regional rank, protected and proposed for protection, are placed on the map.

Geological objects of global rank include objects that characterize the general patterns of development of planetary shells and the main inhomogeneities of the Earth, as well as unique on a global scale. Geological objects of supra-regional rank include objects that reflect the patterns of development of individual continents, oceans, as well as unique ones on a supra-regional scale.

AT last years the totality of geological objects of scientific, historical, cultural or aesthetic significance is called the geological heritage. The division of the geological heritage into types is carried out, as a rule, according to the subject principle.

Stratigraphic type - stratotypes, stratotype localities, reference sections of stratigraphic units of different ranks, as well as sections that characterize significant intervals of a geological section in a continuous occurrence.

Paleontological type - locations of the remains of ancient organisms or traces of their life, outstanding in terms of diversity, rarity and (or) degree of preservation of fossils.

Mineralogical type - localities with a wide variety of minerals, objects of concentration of various mineralogical and crystallographic rarities, as well as areas of modern mineral formation.

Ore-litho-petrological type - outcrops (massifs) of characteristic or rare rocks and ores with clear signs of their composition, structure and texture, as well as other clear evidence of their formation processes.

Radiogeological type - geological objects characterized by high natural radioactivity.

Neotectonic type - areas of manifestation of the newest.

Paleotectonic type - sites earth's crust, clearly reflecting in well-exposed sections the results of the manifestation of tectonic processes of the geological past.

Structural-geological type - traces of manifestations of various kinds of tectonic dislocations.

Cosmogenic type - areas of influence of cosmic impact events on the day surface and interior, as well as sections with interlayers of impact origin.

Geothermal type - objects with pronounced geothermal anomalies.

Facies-paleogeographic type - geological objects that make it possible to reconstruct facies and paleogeographic conditions of sediment accumulation.

Geocryological type - subsoil areas containing fossil ice and (or) permafrost rocks.

Technogenic type - mine workings, their dumps and artificial reservoirs, on which geological processes caused by technogenesis take place.
Historical-geological type - objects of fundamental geological research, as well as mine workings of historical significance.
Most geological sites of scientific, historical, cultural or aesthetic significance correspond to more than one type of geological heritage. Characteristic, for example, are combinations of stratigraphic, paleontological and facies-paleogeographic types, ore-litho-petrological and mineralogical types, neotectonic and geomorphological types of geological heritage, etc. Such geological objects with the manifestation of several different types of heritage are called polytype. With a certain degree of conditionality, one of the types represented on a polytype geological object can be considered dominant.

The highest level of protection for geological objects is the world level, which is determined by their location within the objects world heritage(WHS) protected in accordance with the UNESCO “Convention for the Protection of the World Cultural and natural heritage"(1972), ratified by the USSR in 1988. There are nine such objects in Russia: the Curonian Spit (together with), the Western Caucasus, the Virgin Komi Forests, the Golden Mountains of Altai, the Ubsunur Hollow (together with), Lake Baikal, Ostrov, Volcanoes of Kamchatka and Central Sikhote-Alin.

The Curonian Spit is located near the southern coast opposite the city and is continuous strip sand dunes 0.3-1 km wide, up to 68 m high, and up to 70 km long along the peninsula. The spit is accumulative, created by eolian and wave-cutting activity. In terms of the scale of manifestation of accumulative activity, the Curonian Spit has no analogues in Northern Europe.

The Western Caucasus is located in the upper reaches of the Malaya Laba and Belaya rivers and is an area of ​​development of exceptionally picturesque landforms created by alpine folding: pointed rocks, deep gorges, trough valleys, moraines, tarns, lakes, etc. The wide distribution of limestones led to the development of karst landforms, such as funnels, caves, wells and mines with underground rivers, lakes and waterfalls. Thus, the total length of underground passages in the northern part of the Fisht massif, composed of Late Callovian-Tithonian bioherm limestones, exceeds 15 km. In the sources of the Thach River there is a rich accumulation of Middle-Late Triassic ammonites, reaching 1 m in diameter.

The virgin Komi forests occupy the western slopes of the Northern and Subpolar Urals, where mainly stratigraphic objects of great scientific importance are represented. Of greatest interest is the almost continuous section of the Upper Ordovician-Upper Permian on the Kozhym River. A number of Silurian, Devonian, Carboniferous, and Permian stratotypes are described here. The remains of a diverse fauna of good preservation are represented by trilobites, conodonts, brachiopods, crinoids, bivalves, foraminifers, ostracods, and fish. The rich Early Carboniferous complex of ammonoids presented here has also gained worldwide fame. On the Kozhym River, in the form of a giant tectonic breccia with blocks up to 50-70 m in diameter, a horizon of sediment slippage from the Silurian to the Permian along the underlying Ordovician rocks is also exposed. Of the stratigraphic objects of great interest are the Yareneisky (Limbeko-Yu) Upper Ordovician-Lower Silurian section rich in diverse faunal remains, the Upper Silurian-Lower Devonian Syvyu section and the Upper Devonian West Syvyu section, the Ordovician-Silurian reef complexes on the Balbanyu River and the Upper Mesozoic Rocks Reef on the river Kozhym.

The Golden Mountains of Altai are an area of ​​development of a pronounced alpine relief. Mount Belukha (4506 m) is the highest peak in Altai. is considered as the second deepest (340 m) in Russia continental rift basin filled with fresh water. The lake area is characterized by modern tectonic activity. In the spurs of the Sailyugem Ridge, in the upper reaches of the Kalguta River, Devonian volcanic rocks of all depth facies are developed. There is also a deposit of rare metal ores and a dike complex (kalgutites) with a high content of rare alkalis.

The Ubsunur basin is located on both sides of the Mongolian-Russian border on the territory adjacent to the lake Uvs-Nur (Uvs Nuur). The basin is a neotectonic Paleogene-Pliocene graben with absolute elevations of 750 - 1500 m. The length of the basin from west to east is 600 km, from north to south - 160 km, the sides are usually steep, limited by the latest faults. A thick sequence of Paleogene-Pliocene deposits was formed in the basin, including eolian sands in the southeastern part. From paleontological objects, the locations of fossils of the Paleogene (bones of fish, turtles, reptiles and mollusks) and Neogene (rhinos, ostriches, giraffes, monkeys), characteristic of a warm climate, are known. Of interest is also the Mongun-Taiga Devonian granitoid massif, which is a large isometric batholith with small satellite intrusions located along its periphery.

Lake Baikal is the world's largest continental rift basin filled with fresh water. Its depth is 1637 m. The bottom sediments of Baikal contain information about climate change region over the past 5 million years. Lake Baikal and the adjacent territory are distinguished by an amazing abundance and variety of geological “sights”. Among them, the Slyudyansky mining region and the Tazheransky alkaline massif are of the greatest interest. The Slyudyansky mining region is one of the oldest mining regions in Russia, known since the 18th century, thanks to the deposits of giant-crystalline phlogopite, lapis lazuli, scapolite, amazonite and the purest wollastonite in the world. In total, more than 100 minerals have been described in the region, many of which form crystals that are unique in size and shape. The Tazheran alkaline massif is known for its unique mineralization associated with skarns and pegmatites. In a small area not exceeding one square kilometer, 150 minerals have been described, among which are blue diopside, red clinozoisite, purple scapolite, blue calcite, amazonite, corundum, beryl, etc.

Wrangel Island is located on the border of the East Siberian and. Of the geological objects, the most interesting are the Perkatkun rock crystal deposit and the location of the mammoth fauna of the Academy Tundra. The Perkatkunskoye deposit is located in the basin of the middle reaches of the Mamontovaya River, where rock crystals up to 13 cm long are found among the Paleozoic deposits. According to radiocarbon data, the age of tusks and other bone remains of mammoths is 3700–7710 years. A new dwarf subspecies of the mammoth Mammuthus primigenius vrangeliensis is described for the first time on this material. Apparently, Wrangel Island was the last refuge of mammoths who still lived on Earth 3700 years ago.

Volcanoes of Kamchatka are located in the junction zone of the Pacific and Eurasian tectonic plates, characterized by active volcanism. There are 30 active, more than 160 extinct volcanoes, more than 150 thermal and mineral springs. Numerous geysers, hot crater lakes, underwater hydrotherms and other manifestations of post-volcanic activity are common. The following volcanoes are of the greatest interest: Ichinskaya Sopka, Kronotskaya Sopka, Krasheninnikova, Kikhpinych, Bolshoy Semyachik, Avachinskaya Sopka, Mutnovskaya Sopka, Ksudach and Zheltovskaya Sopka.

Among the volcanic edifices, the New Tolbachik Volcanoes, which formed quite recently, during a unique fissure eruption in 1975–1976, deserve special mention. As a result of the eruption, a chain of cinder cones appeared, surrounded by basalt lava flows over an area of ​​about 50 km2. Now the volcanoes are calm, and all surrounding area is a real volcanic desert.
Among the most significant geological objects, in addition to volcanoes, on the peninsula are the famous Valley of Geysers and the caldera of the Uzon volcano, where modern hydrothermal-metasomatic changes in rocks are observed and mercury-tin-arsenic mineralization with native sulfur is formed.

The Central Sikhote-Alin is a complex territory. In scientific terms, two geological objects are of the greatest interest - the Silver and Sikhote-Alin paleovolcanoes. Paleovolcano Serebryany, located in the center of the Serebryany volcano-tectonic structure, is a polygenic stratovolcano of Danish age. In the modern relief, it is expressed in the form of an eroded paleovolcano root, which forms an array of granodiorite porphyries. The Sikhote-Alin meteorite craters represent an ellipse of scattering of a unique iron meteor shower that occurred on February 12, 1947. The scattering ellipse includes more than 100 craters created by meteorite fragments with a diameter of 0.5 to 28 m.

There are many unusual intrusions in our country, also unique geological monuments. For example, the ring massif Konder in the Far East. On the space image it has the appearance of a meteorite crater, although its nature is quite different. Ultramafic alkaline rocks of various composition were intruded here in concentric layers.

Most of the deposits of jewelry, ornamental, collection and rare minerals and rocks are also included in the monuments of inanimate nature. Among them, a special place is occupied by the Lilac stone deposit in. This is the only deposit of charoite in the world, and the taiga river Chara gave its name to this amazing stone. Products made of charoite with a thick lilac color are very famous. Worthy of mention are emeralds and other precious stones of the Aduisko-Murzinskaya zone in the Urals, rare and collectible minerals of the Ilmensky mountains of the Urals, the Khibiny and Lovozero massifs on. The amber deposit on the coast of the Baltic Sea near Kaliningrad is also unique, which has no equal in the world. Already in ancient times, amber came from here to the countries of the Mediterranean. In many museums around the world, one can admire samples of amber from the Primorsky deposit with inclusions of insects and other organisms embalmed in this fossil resin.

On the territory of Russia there are many interesting manifestations of karst, primarily caves. Surprisingly beautiful Kungur ice cave in the Urals. Sintered ice stalactites and stalagmites formed in its grottoes.
Significant areas in the north of Russia are occupied by permafrost. In the coastal cliffs of the northern seas and rivers from the delta of the Lena River to the Kolyma River, giant ice veins stand out among the loess strata. They contain tusks, bones, and sometimes whole carcasses of mammoths and other fossil animals. Some of the sections of the loess-ice strata have been studied in detail and belong to the monuments of the geological past of world significance. Another amazing phenomenon associated with permafrost processes is icing - thick ice covers in river valleys that persist throughout the summer in verdant thickets.

A special place among the geological monuments is occupied by sections of rocks, which served as the basis for the identification of new stratigraphic units and became monuments of world significance. These are sections of the Riphean, the Permian system in the Cis-Urals and the Lower Cambrian on the Lena River. The sections of the Carboniferous near Moscow are unique (the names of their stages and horizons include such settlements as Podolsk, Myachkovo, Gzhel, etc.).

Geological monuments of nature are geological objects with unique features, put under state protection and having all the necessary documents for this.
First geological monuments nature on the territory of the Krasnoyarsk Territory were approved by the decision of the Krasnoyarsk Executive Committee in 1977. They included the Aidashenskaya, Maiskaya, Kubinskaya, Karaulnaya, Lysanskaya, Bolshaya Oreshnaya and Badzheiskaya caves.
In 1981, by decision of the Krasnoyarsk Executive Committee No. 404 dated September 21, 1981, the geological outcrops "Motley Rocks" and the geological outcrop "Popigayskoye", included in the structure of the Popigai astrobleme, in the Khatangsky district of the Taimyr Autonomous Okrug, a geological section along the river Oresh in the Ermakovsky district and the landscape area "Stone Town". Later, the Museum of Permafrost in the city of Igarka, the ice-mineral complex "Ice Mountain" and the Minin Pillars were classified as geological monuments of nature.

Stratigraphic geological monuments

Section of the Dzhebash series along the Oresh River
The monument is located in the Western Sayan, between the Aradansky and Kurtushibinsky ridges, in the basin of the river. Us, on the spit of the rivers Coyard and Oresh.
The Dzhebash series is composed of monotonous green-gray and green metamorphic shales, metamorphosed sandstones, siltstones with subordinate quartzites and limestones, which are subject to intense flaking and corrugation. The base of the Dzhebash Group has not been exposed; the contacts with the overlying deposits are usually tectonic, with intrusions along the contact of sill-like bodies of ultramafic rocks.
With a common conformable occurrence of the Dzhebash series and the overlying Chinga suite, interbeds of gray argillaceous-siliceous and argillaceous-chlorite shales appear in the upper part of the former, which are also found in the lower parts of the obviously Lower Cambrian deposits of the Chinginskaya suite. At the base of the Chinga Formation, a change in the conditions of sedimentation is assumed, which was not accompanied by structural rearrangement.
According to lithological and structural-textural features, the formations of the Dzhebash series are subdivided into five sequences (a, b, c, d, e). The description of the section of the Dzhebash series was compiled on the basis of tracing it along the foot of the right slope of the river. Oresh, where sequences “b”, “c”, “d”, “e” are exposed.
Sequence “b” is composed of green-gray, green and gray, strongly flaky quartz-chlorite, quartz-calcite paraschists, metamorphosed fine- and medium-grained sandstones and shales with interlayers of marmorized limestones, quartzites and sericite-quartzite schists, orthoschists. The thickness of the sequence has not been traced, the upper boundary is conditionally drawn along the top of a well-aged quartzite horizon, the appearance of orthoschist interbeds. Unit “b” roughly corresponds to the Ishkinskaya and Syutkholskaya formations.
Unit “c” is composed of greenish-gray, gray, and yellowish-green paraschists interbedded with bluish-green albite-epidote-chlorite banded orthoschists. Dark-colored varieties predominate in the lower part of the section, while lighter ones in the upper part. The thickness of the stratum along the section is 1400 m. The stratum “c” corresponds to the tops of the Amyl Formation. The upper boundary of the stratum is clear, drawn along the bottom of the orthoschist horizon of the overlying stratum “d”, the lower boundary is tectonic with sandstones and limestones of the Ilemorovo Formation of the Middle Devonian.
Sequence "d" is composed of metamorphosed volcanic rocks of basic composition, green, bluish- and grass-green, weakly banded albite-epidote-chlorite, albite-actinolite-carbonate-chlorite orthoschists and sheared amygdalolithic porphyrites. The sequence is well sustained and can be traced over the area. Relic structures of tuffs, amygdaloidal texture in porphyrites, and spherical separation are observed in the rocks of the sequence. The thickness of the sequence is consistent and is 500 m, the upper boundary is drawn by the disappearance of orthoschists and the appearance of greenish-gray banded quartz-carbonate-chlorite schists.
Unit “e” is composed of monotonous quartz-chlorite-carbonate, quartz-carbonate-chlorite, argillaceous-chlorite paraschists with thin layers of albite-epidote-chlorite orthoschists.
The incomplete thickness of the sequence is 810 m. The upper contact of the sequence is tectonic with shales of the Chinga suite. The section of the strata in the area is well sustained. The sequence previously belonged to the Amyl Formation of the Middle Cambrian, in its lower part. The thickness of the exposed part of the section of the Dzhebash series is 3800 - 4700 meters.
The age of the Dzhebash Group is accepted as Early-Middle Riphean.
Geological monument of nature of the stratigraphic type of regional rank. The status of a natural monument of the Krasnoyarsk Territory was established by the Decree of the Regional Executive Committee No. 404 of September 21, 1981.

Root outcrops of deposits of the Dzhebash series on the river. Oresh

Cosmogenic geological monuments

Astroblema Popigaiskaya (Tract "Motley Rocks")
Popigai astrobleme (Popigai meteorite crater) is a vast territory in the east of Taimyr. It is located in the Taimyr municipal district and is geographically located in the basin of the Popigai and Rossokha rivers, about 900 km east of Norilsk.
The Popigai crater arose at the end of the Eocene epoch 35.7 million years ago. Although impact structures are also known in many other parts of the Earth, the Popigai crater is the largest Cenozoic impact structure identified so far. It is one of the ten largest craters in the world, and only six impact craters with a diameter of 100 km or more have been reliably identified on Earth, together with Popigaisky. Like other giant impact craters, it is distinguished by a complex internal structure, as well as a variety of individual elements of the internal structure, which in many cases are available for direct observation. The diversity of the composition of rocks that have undergone impact metamorphism, along with varying degrees of their transformation, makes it possible to comprehensively study the nature of impact actions on various substrates. Almost all types of rocks and newly formed minerals known in other impact craters of the World have been found here.
It should be added to this that in terms of the degree of exposure of impact breccias and impactites, which protrude to the surface over an area of ​​more than 1000 km² and also form large (up to 150 m high and many kilometers long) natural outcrops, Popigaisky crater surpasses all known impact craters by earth's surface.
The Popigai crater is the largest reservoir of technical impact diamonds, the total resources of which exceed the total reserves of all diamond-bearing kimberlite provinces in the world. By their origin, impact diamond deposits, figuratively speaking, created by the forces of heaven, have no analogues among other types of mineral deposits.
The most representative outcrops that characterize the ratio of individual varieties of impact breccias and impactites, as well as rocks that make up the base of the crater on the outer slope of the annular trench, are located in the northwestern sector of the crater. Here is the tract Motley Rocks, which is a geological natural monument of the Krasnoyarsk Territory, in which blocky allogeneic breccias, overlain by a powerful stratal body of tagamites, form high rocky ledges on the slope of the river valley. Rassokha directly below the mouth of the stream. Sakha-Yuryage. Randomly mixed blocks of various crystalline and sedimentary rocks (partly impact metamorphosed and dissected by veins of tagamites and fine clastic breccias) make up the main part of the valley slope. The varied coloration of these boulders gave the name to the tract. They are cemented by loose fine-clastic breccia (coptoclastite) containing small gneiss bombs bordered by impact glass and sometimes bombs and small glass particles.
The breccia is overlain by a remnant of a columnar tagamite bedding body that plunges up and downstream, where its apparent thickness increases. Downstream on the steep side of the river valley. Rassokha near Mount Khara-Khaya, this powerful body was uncovered almost 140 m. In the lower part of the cliff, tagamites include numerous large (up to 10-20 m) blocks of shock-metamorphosed and thermally transformed gneisses, as well as a large number of smaller fragments of these rocks and their minerals. There are no large gneiss blocks in the upper part of the exposed tagamite bedded body. Here, on a large area, an uneven roof of the tagamite layer is visible, in the deepening of which there is an irregular lens of suevites.

zuvites

The Popigai crater as a whole is a unique geological monument of nature and is a national treasure of Russia that deserves to be preserved and further comprehensively studied. All extensive information obtained in the course of his many years of research, including well cores, collections of samples, etc., is also subject to preservation.
Therefore, the decision of UNESCO to include the Popigai crater in the list of world geological heritage sites is justified.
In accordance with the Decision of the Executive Committee of the Krasnoyarsk Regional Council of Deputies No. 404 dated September 21, 1981, the Motley Rocks outcrop was recognized as a natural monument of regional significance.

Scheme geological structure Popigai impact crater

1-4 - coptogenic complex: coptoclastites (1), suevites (2), tagamites (3), polymict allogeneic megabreccias (4), 5 - Early Triassic dolerites, 6 - Permian sedimentary rocks, 7 - Cambrian sedimentary rocks, 8 - Late Proterozoic sedimentary rocks rocks, 9 - Archean metamorphic rocks, 10 - faults, 11 - ring uplift axis

colorful rocks

Tract "Motley rocks"

The site of the fall of the Pallas Iron meteorite
The natural monument "Pallas iron" is located in the Novoselovsky district on the right bank of the Krasnoyarsk reservoir in Ubeysky Bay, on top of the Meteoritnaya hill, 15 km east of the village of Koma (approximately 200 km from Krasnoyarsk).
The meteorite was found in 1749 by blacksmith Yakov Medvedev. The block of iron originally weighed 687 kg. The blacksmith delivered the block to his home in the village of Ubeyskaya (later Medvedevo, Novoselovsky district) and decided to use it for the manufacture of metal products, but the stone turned out to be unsuitable for blacksmithing. For more than 22 years, he lay in the blacksmith's yard before he was identified by the mountain master Johann Mettich.
In 1772, an unusual block was shown to Academician PS Pallas, who was in the area with an expedition. On his instructions, a sample of an unusual breed was sent to St. Petersburg, and in 1777 the entire block was delivered to the St. Petersburg Academy of Sciences. It was later split into two pieces.
In 1776, P.S. Pallas handed over one of the fragments from the find to an amateur chemist from the city of Stettin, Johann Carl Friedrich Mayer, who was the first in Europe to subject the Siberian find to a comprehensive study. He tried to unravel its nature by comparative analysis with other terrestrial natural formations, as well as artificially obtained varieties of iron and steel. But his research did not give any final results, and could not give, because at that time the composition of meteorites was not yet known.
Later, Academician E.F. Khladni took up the study of the meteorite. It was thanks to these studies that the existence of extraterrestrial matter was proved and the theory of extraterrestrial life was put forward. The data obtained by the scientist formed the basis of the then emerging science - meteoritics. Subsequently, all iron-stone meteorites became known as Pallasites.

Fragment of iron meteorite Pallas iron

In July 1980, not far from the place where the meteorite fell, according to the project of the sculptor Yu.P. Ishkhanov, a memorial sign was installed - a two-meter cast-iron disk, which depicts fallen meteorite and his flight. On July 31, 1981, the grand opening took place, which surprisingly coincided with a total solar eclipse. In 1987, by decision of the Executive Committee of the Regional Council No. 523 of December 28, 1987, it was decided to preserve the crash site, and a natural monument with an area of ​​78 hectares was created.

Obelisk in the area of ​​the fall of the Pallas iron meteorite

Geological natural monument of cosmogenic type of regional rank. The status of a natural monument of the Krasnoyarsk Territory was approved by the Decree of the Government of the Krasnoyarsk Territory No. 244-p dated May 20, 2015.

Geocryological monuments of nature

Igarsky Permafrost Museum
The museum is located in Igarka. In 1930, a research permafrost station was organized in Igarka to study the problems of permafrost. Since 1936, underground laboratories have been built to study the possibilities of using permafrost as natural refrigerators, as well as to conduct experiments on permafrost soils at constantly operating negative temperatures. Two experimental dungeons were built on the site of the permafrost station, located at the northwestern end of the old part of the city of Igarka. The area is a gentle slope in the south, south-west direction, towards the Yenisei. From the site to the Igarskaya channel 750 m. It rises 40-42 m above the low water level in the river.
The site is composed of thick strata of thin-layered clay deposits of the belt type. Ribbon silty loams and clays pass in places into silty sandy loams, and in places they include lenses of fine sand. The sandy lens exposed in the underground section looks like an area of ​​erosion filling in the main band. All this sequence belongs to the main deposits of the second Yenisei terrace in the area of ​​the city of Igarka. The permafrost on the site extends to a depth of 30-35 m. The active layer reaches 1.8-2.2 m. In some places, in some years, the permafrost remains isolated from the seasonal thawing layer by small talik layers.
The Museum of Permafrost is a unique geological and geographical object, which includes an underground working in the thickness of permafrost rocks of the Karginsky deposits of the second Yenisei terrace. The ice content of the permafrost is 35-50%.
The main exhibit in the museum of permafrost is the permafrost itself, from which the walls of the dungeon are built. In addition, it presents ice samples from the Ice Mountain outcrop, mammoth bones, and remains of relict trees. Experiments are being carried out to freeze fish and plants. Every year, observations are made of the state of the temperature regime in the dungeon.

Exhibits of the "Ice Mountain" complex in the Igarsk Permafrost Museum

frozen plants

A unique structure in permafrost to this day continues to exist in natural form, without the use of artificial installations. Their use would greatly facilitate the maintenance of the dungeon, but would forever deprive it of its true natural character. The underground in the permafrost is used for geocryological research, study of engineering structures and promotion of geological, geographical and ecological knowledge about the environment.
The Museum of Permafrost in the city of Igarka was declared a natural monument of regional significance in accordance with the Decree of the Legislative Assembly of the Krasnoyarsk Territory No. 5-116p dated March 29, 1995.

Ice-mineral complex "Ice Mountain"
The complex is located on the right bank of the Yenisei, 100 km south of Igarka, at the latitude of the Arctic Circle. On the banks of the Yenisei, 4.5 km below the mouth of the river. Bol. Denezhkino, a layer of pure underground ice comes to the surface. It was discovered in 1972 by employees of the Igarsk Permafrost Research Station of the Institute of Permafrost Science of the Siberian Branch of the USSR Academy of Sciences and named Ice Mountain. In the place where the ice layer comes to the surface, its thickness is about 10 m, and further from the coast (according to drilling and geophysical studies) it increases to 40, in some places up to 60 meters.
An analysis of various inclusions in the ice made it possible to determine the age of the most ancient part of the Ice Mountain: 43,000 ± 1,000 years. This is the time of the first Late Quaternary (Zyryansk) glaciation of the Yenisei North. The study of soils carried by an ancient glacier, as well as fungal spores, pollen of ancient plants, various organic remains, made it possible to learn a lot about the climate of that distant era.
Some permafrost experts doubt the glacial origin of this deposit. They believe that the ice body could have been formed in the same way as the majority of stratal ice deposits were formed - during the ancient long-term freezing of water-saturated soils or during the freezing of high-pressure underground sources. Thus, the question of the origin of the "Ice Mountain" remains debatable.
The study of deposits of underground ice is important not only because it expands knowledge about the geological past of the Earth. This knowledge is of practical importance in the economic development of the regions of the North. The melting of massive ice leads to the formation of deep dips, landslides, and the formation of depressions. This must be taken into account when building cities in the North, building bridges, dams, when laying roads and pipelines.
Preservation of the unique natural ice-mineral complex "Ice Mountain" is necessary for carrying out stationary research work. The ice-mineral complex "Ice Mountain" was declared a natural monument of regional significance in accordance with the Decree of the Legislative Assembly of the Krasnoyarsk Territory No. 5-116p dated March 29, 1995.

Ice layers in banded clay
Geomorphological monuments of nature

Outcrop "Red Rocks"
The Red Rocks outcrop is located 5 km east of the city of Talnakh. It is clearly seen in the outcrop how Upper Permian terrigenous deposits are overlain by a sequence of volcanogenic rocks of the trap complex formed in the Early Triassic. The complex is composed of alternating mafic lava covers and their tuffs. The lavas are represented by various diabases, sometimes by spilites; amygdalolithic varieties are present in the roof. The thickness of individual covers is usually 30-40 m. Within the outcrop, the coal brook cuts through the volcanogenic stratum, forming a waterfall up to 13 m high and a small lake. During weathering, the volcanogenic sequence acquires a bright reddish-brown color. Hence the name of the area.
Geological natural monument of geomorphological type of regional rank. In accordance with the Decisions of the Executive Committee of the Krasnoyarsk Regional Council of Deputies No. 471 dated December 19, 1984, the outcrop "Red Rocks" was recognized as a natural monument as a landscape area.

Fragment of the Red Rocks outcrop

Cave Aidashenskaya
Cave Aidashenskaya is located on the northern slope of the Arga ridge in the tract "Devichya Yama", 2 km west of the village. Mazulsky. The entrance to the cave is located on a nameless hill with an absolute elevation of 325 m.
The entrance is cone-shaped, with a section of 4.7 by 3.8 m, with a depth of 5 m to a narrowing. Then there is a narrow steep descent. The main grotto has a slightly elongated elliptical shape, 3.5-4 m wide and 7-8 m long. In section, the grotto is bell-shaped. Its height, after excavation of sediments with the remains of the material culture of the ancient inhabitants, is up to 7 m. The cave was formed about 0.5 million years ago and is a crack in the vertical layers of dolomites, limestones and marbles, which, as a result of exogenous processes, was transformed into a cave. Until the 70s. 20th century the entrance was half-blocked with earth and fragments of limestone. Numerous objects of material culture of the Late Neolithic, Bronze and Early Iron Ages were dispersed in the sediments. The cave in the past served as a cult object, where the locals threw their products to appease the gods. The first excavations in the cave were carried out by treasure hunters in the Middle Ages. At the end of the XIX century. the cave was examined by archaeologists D.S. Kargopolov and P.S. Proskuryakov. Carried out in the 70s. 20th century The excavations made it possible to extract more than 1,100 items of material culture (arrowheads, plaques, beads, harness details, etc.) stored in the Achinsk Museum of Local Lore.
The natural monument was created in order to preserve an unusual cult cave. This is a natural complex, valuable in ecological, aesthetic, scientific and educational respects. Geological natural monument of geomorphological type of regional rank. The status of a natural monument is fixed by the Decision of the Executive Committee of the Regional Council No. 351-13 of 06/08/1977.

Entrance to the cave Aydashenskaya

Cave Karaulnaya-II
Location: Eastern Sayan. Karaulnensky karst-speleological site. Cave Karaulnaya-2 is located on the left slope of the river. Guard, 5 km from the village. Successful.
Here the Yenisei valley reveals a small fold composed of platy limestones, which form cliffs visible in the coastal cliffs above and below the mouth of the Karaulnaya River. The relief of the karst area is low-mountainous. The heights of the hills reach 450 m. Exotic rocks are located near the mouth of the river. Sentry, and upstream. A narrow spoon is visible from the river valley, to the left of which a sheer limestone wall rises. At an altitude of 150 m above the bed of the river valley. Guardhouse under the rock is the vault of the light grotto of the cave. Below in the cave are the Grottoes of Enchantment and Kapelny. The cave is convenient for visiting, including tourists and novice speleologists.
Geological natural monument of geomorphological type of regional rank. The status of a natural monument is fixed by the Decision of the Executive Committee of the Regional Council No. 351-13 of 08.06. 1977




In the cave Karaulnaya-II


Calcite "Pagoda" in the cave Karaulnaya-II


Excursion to the cave

Cuban cave
The natural monument is located in a log on the left bank of the Biryusinsky Bay of the Krasnoyarsk reservoir, 200 m from the mouth of the river. Biryusy, 14 km from the village of Shumikha. The entrance shaft of the Kubinskaya cave is located at the base of a high limestone wall. The entrance to the cave is small, slit-like, vertically descending. In general, the vertical span of the cave (its known depth to the level of permanent flooding) is about 200 meters. Several grottoes are known in the cave: Fidel, Grandiose, Blue Lakes, Antresol. The grotto Grandiose is especially beautiful. Its height is 25 meters, its area is 20 mx 12 m. the western oblique course is especially rich in sinter forms.
Cave Kubinskaya is the deepest in the Krasnoyarsk Territory. Before filling the Krasnoyarsk reservoir, its depth was 274 meters. At present, at the minimum levels of the reservoir surface, it is accessible to a depth of 200 meters.
The natural monument was created in order to preserve the unique and one of the largest caves in the region. The cave has a scientific and educational value. Geological natural monument of geomorphological type of regional rank. The status of the monument is fixed by the Decision of the Executive Committee of the Regional Council No. 351-13 of 06/08/1977.

Limestones of the Kubinskaya Cave area

Beautiful streaks in the Cuban cave

Maiskaya Cave
The cave is located on the left bank of the Biryusinsky Bay, 16 km from the Krasnoyarsk hydroelectric power station, in a gorge north of the Tsarskie Vorota ridge. Light massive limestones of the Lower Cambrian are developed on the site.
The entrance to the Maiskaya Cave is located on the northern slope of the gorge in the left wing of the circus, 1 km from the Gendarme rock. Two entrances to the cave are located in the central part of the circus. The cave is connected to the surface by a well. The depth of the cave is somewhat more than 60 m and has two grottoes: the Altar and the Lower. The Altar Grotto is 12 meters high, 25 meters long and 20 meters wide. The cave is famous for its unique beauty of sinter formations.
The natural monument was created in order to preserve the unique beauty of the cave in the region. This natural complex is valuable in ecological, aesthetic, scientific and educational respects.
Geological natural monument of geomorphological type of regional rank. The status of the monument is fixed by the Decision of the Executive Committee of the Regional Council “351-13 of 06/08/1977.

Maiskaya Cave


Sinter formations in Maiskaya Cave

Badzheyskaya cave
The Badzheyskaya cave is located on the slope of a small ridge on the watershed of the Tayozhny and Stepnoy Badzhey rivers, tributaries of the river. mana. The entrance to the cave (Fig. 3.9) is located 3 km east of the village. Nutty.
The Badzheyskaya cave is confined to conglomerates, conditionally attributed to the Ordovician. It begins with an extensive well, 21 m deep. It does not have a labyrinth structure, since the passages are controlled by lines of tectonic disturbances. The cave has a main thoroughfare with side branches. The originality of the situation is created by a large lake, up to 4 m deep, and flowing into the depths of the massif along an inclined channel, with cascades Porcelain Stream. Sinter deposits in the cave are modest and few. But in general, the cave leaves cavers with excellent impressions and a desire to visit it again and again.
The cave is a scientific and educational object for speleotourism. Geological natural monument of geomorphological type of regional rank. By the Decree of the Executive Committee of the Regional Council No. 351-13 dated 06/08/77, the Badzheyskaya Cave was declared a natural monument of regional significance.

conglomerates


Lake in the Jebskaya Cave


Entrance well of Jebskaya cave

Big Oreshnaya Cave
Big Oreshnaya Cave is located in the basin of the river. Mana, on the left bank slope of the river. Mana, on the left bank slope of the river. Taiga Badzhey, 4 km from its confluence with the river. Badzhey and 3 km east of the village. Nutty.
Conglomerates, conventionally attributed to the Ordovician, form a continuous strip 40 km long and 1.5-3.5 km wide in the area where the cave is located. This strip stretches in a north-north-western direction from the right bank of the Mana, from the village. Narva to the village Dirty Kirza.
Bolshaya Oreshnaya Cave is a deep and extensive labyrinth of predominantly inclined passages and galleries in conglomerates. There are grottoes, wells, cracks, honeycomb areas, underground lakes and streams. In the Ozerny grotto, scuba divers dived into the siphon and discovered the "hydrospace" - a vast underwater space that goes beyond the bounds of the possible.
Bolshaya Oreshnaya cave is one of the longest caves in Russia among the caves formed in conglomerates. Its total length is over 40 km. This cave is a speleogigant, which allowed the Krasnoyarsk Territory to firmly hold the first place in terms of the length of caves in Russia. Speleologists have been exploring it for over 30 years, but almost every expedition has opened new dungeons.
Geological natural monument of geomorphological type. The status of the monument was fixed by the decision of the Executive Committee of the Regional Council in 1977

Entrance to the cave


Calcite wall hangings


Sinter formations

step-shaped calcite deposits

Cave Lysanskaya
Lysanskaya cave is located in the mountainous taiga area, 35 km east of the village and the railway station Shchetinkino and 30 km northeast of the village. Chibizhek. There is a logging road next to the cave. The area of ​​the established protection zone at the entrance is 1 ha, the total surface area above the cave is 20 ha.
Karst phenomena in the river basin. The Pavlovka, a right tributary of the Balakhtison, is associated with Vendian dark layered limestones (geological age is about 600 million years). The terrain is low-mountainous. The dominant peaks rise 900 - 960 m above sea level, and the relative elevations are up to 350 m. There are funnels, remnants, ledges and caves in the limestones.
The Lysanskaya cave is located on the right side of the stream of the same name, 0.5 km above its mouth. The trapezoidal entrance is raised 3 m above the bed of the stream. Lysan. In summer, a river flows through the entrance, during the flood period it falls like a waterfall through the entrance, and in winter it is dry and richly decorated with ice stalactites and stalagmites. At 40 m from the entrance, the ceiling of the gallery drops sharply, forming a half-siphon, which can be overcome in the winter low water on a rubber boat, bending down. This is followed by the lower water floor, accessible for swimming at a distance of 250 m. Here, the ceiling of the gallery goes under water to a depth of about 10 m, forming a siphon. It is overcome by speleologists-scuba divers.
The upper floor of the cave begins with a narrow winding manhole leading to the Dry and Lake galleries. Their walls are richly ornamented with sinter deposits - columns, draperies, cascades. In the Lake Gallery there are reservoirs, the banks and bottom of which are covered with beautiful calcite patterns. The walls are dressed with white draperies, and stalactites hang from the ceiling. the total length of the cave is more than 2000 m, and not all underwater galleries have been explored. There is no second such cave in the Krasnoyarsk Territory.
To protect the unique cave landscape, speleologists in the eighties concreted the entrance hole on the second floor, installing a metal hatch. But soon it was blown up by unknown persons. Only remoteness from cities and inaccessibility of the upper floor save the cave from modern vandals. The cave needs protection as an outstanding natural monument.
Geological natural monument of geomorphological type of regional rank. The status was established by the Decree of the Executive Committee of the Regional Council No. 351-13 of 06/08/1977.

In the Lysan cave




Stalactites and Helectites in the Lysan Cave


On the lake in the Lysan cave

stone town
"Stone Town" is located in the Western Sayan, 20 km west of the weather station Olenya Rechka, located on the Usinsky tract (federal highway M-54 Krasnoyarsk-Kyzyl). Here, in the mid-mountain relief, there are exotic remnants composed of granites. The relatively compact (10 x 5 km) oval distribution area of ​​these remnants is limited by the valleys of the Bolshaya and Malaya Oya rivers. All the remains are located on the southern slope of the ridge between these rivers.
Geologically, the remains of the Stone Town are located on the area of ​​the Dzhebash-Amyl morphostructural zone of the second order, the Klumys-Upper-Amyl block, the morphostructure of the third order. They are exits to the surface of the Ambulak intrusive massif.
The formation of the Dzhebash-Amyl morphostructure is due to its stable recent uplift of medium and moderate intensity with an amplitude of 200 to 1500 m, which led to the formation of mid-mountain and high-mountain relief types. Within this morphostructure, the Kulumys-Upper-Amyl block is distinguished, which spatially coincides with the southern part of the Dzhebash-Amyl structural-formational zone. The block is composed of shales of the Dzhebash series intruded by granitoid intrusions. The block is characterized by an intense regime of neotectonic movements, which led to the formation of a mid-mountain erosion-denudation relief with an absolute watershed of 1200-2000, relative elevations of up to 500-700 m.
According to the totality of morphogenetic factors, the following are distinguished here: newly formed denudation, ancient denudation, structural-denudation, erosion-accumulative relief of river valleys.
The newly formed denudation type of relief is widespread. The joint activity of complex denudation processes led to the formation of rounded flattened landforms within the middle and high mountains. This type of relief is widespread within the erosion-denudation middle mountains and in the high-mountain tier of the relief. The watershed spaces here are represented by a system of dome-shaped smoothed peaks, separated by wide saddles.
Stone Town", having many features in common with the geological natural monument "Stolby", is much smaller both in area and in size of individual remnants. Both of these geological monuments of nature are significantly subjected to anthropogenic pressure. Almost all the remnants show traces of tourist camps with significant accumulations of garbage, although on the approaches to the "Stone Town" there are boards with the inscriptions "Natural monument. protected by the state." Nevertheless, this is an excellent example of the mountain-taiga relief of the Western Sayan. From the upper remains, located on the ridge, there is a good view to the south of the Aradan ridge with snow-covered peaks. From here you can see the old Usinsky tract. Tourist organizations of the regional center Ermakovskoye conduct walking and horseback excursions from the Olenya Rechka to the Stone Town (including for schoolchildren). The natural monument is also visited by groups of water tourists rafting down the Bolshaya Oya River.
Geological natural monument of geomorphological type of regional rank. The status of a natural monument is fixed by the Decision of the Executive Committee of the Regional Council No. 404 of September 21, 1981.

Remnant of granites in the Stone Town


Remains on the ridge on the watershed of the Bolshaya and Malaya Oya rivers


Panorama of the Stone Town

minin pillars
Location: Eastern Sayan, Solgon Ridge, Krasnoyarsk Ridge.
The region as a whole is characterized by a valley low-mountain taiga landscape, mainly with sculptural landforms, but with a noticeable influence on their location of elements of the geological structure.
A feature of the considered part of the Krasnoyarsk ridge is that it is located close to the main base of erosion - the Yenisei valley and therefore is dissected very intensively and quite deeply.
The Minin Pillars are very similar to the outcrops of intrusive rocks on the territory of the Stolby Reserve. Some researchers refer to these intrusive formations as the Lutag complex, while others refer to the Shumikhinsky complex of alkaline syenites, nordmarkites, and subalkaline granites.
In most cases, the host rocks for the intrusive bodies of the complex are volcanogenic formations of the Byskar series, which break through the intrusions and metamorphose. The placement of intrusions is controlled by discontinuous dislocations that are renewed or laid down at a late stage of the region's activation. The intrusive rocks of the Shumikhinsky complex compose the largest massif within this area - Listvensky, as well as a number of small bodies on the watershed of the Gladkaya Kacha and Bol rivers. Listvenki.
The following spatial distribution of rock differences is observed in the surface section of the massif. Granites and granosyenites compose the northern and eastern parts of the massif and make up about 40% of its total area. The southern part of the massif is composed of uniform in composition and structure coarse-grained meat-red quartz syenites and nordmarkites. The western apophysis is represented mainly by porphyritic granosyenites, which are replaced by fine-grained granosyenite porphyries on a higher erosional section. Mutual transitions between the identified rock varieties are gradual and sometimes hardly perceptible.
In the area of ​​syenite development, the distribution has round-topped or wide flat watersheds, the top parts of which are characterized by numerous kurums and weathering remnants in the form of manes, ridges and pillars.
The valleys of streams, as a rule, have a V-shape, their slopes are steep, often steep and rocky, sometimes covered with stone screes. Upstream, they turn into steeply rising dry hollows, ending in steeply sloping sinkholes. In areas where rivers cut through the syenite massif, rocky outliers with bizarre outlines are noted along the slopes (Fig. 3.16).
Geological natural monument of geomorphological type of local importance. The status was established by the Decree of the administration of the Krasnoyarsk Territory No. 310-p dated 19.08. 2002
The region of the Minin Pillars has long been loved and often visited by Krasnoyarsk residents because of the bizarre shape of the syenite remnants located here, many of which have their own names. From a scientific point of view, the visual manifestation of endogenous and exogenous geological processes at this object is interesting.

Rocky outcrop of syenites

Outcrops of syenite rocks in winter

Sulomai pillars
The natural monument "Sulomaisky Pillars" is located in the Evenki municipal district of the Krasnoyarsk Territory. It is located in the lower reaches of the Podkamennaya Tunguska River, 20-30 km above the village. Sulomai, on the Tunguska Ridge of the Central Siberian Plateau.
This is a canyon with a length of about half a kilometer with steep slopes 120-150 meters high, clamping the Podkamennaya Tungusska River. The slopes of the canyon on both banks are vertical pillars of various most intricate shapes with a diameter of 6-10 meters and a height of 30-80 meters. These six-sided pillars were formed as a result of weathering of the remnants of the Lower Triassic trap formation.
Geological natural monument of geomorphological type of regional rank. The status of a natural monument is fixed by the Decision of the Executive Committee of the Regional Council No. 455 of December 25, 1985.

Sulomai pillars. Remains of traps.

Panorama of the natural monument "Sulomaisky pillars"

Sulomai pillars.

Ergaki mountain range
The Ergaki massif is located in the Ermakovsky district of the Krasnoyarsk Territory, 410 km along the M-54 highway to the south-west of the city of Abakan.
The area is confined to the central zone of the Western Sayan. The geomorphology of the region is a sharply dissected mid-mountain relief of the alpine type. The area is mountain-taiga, dissected by a river network.
Main orographic element is the axial part of the West Sayan ridge, stretching approximately in the latitudinal direction in the form of a mountain range, which includes the Kulumys ridge, the Ergaki ridges, Kutyn-Taiga. The highest absolute elevations reach 2000-2200 m. The described geological landmark is located in the Verkh river basin. Buiba, Us.
Geologically, this territory is located in the northeastern part of the Lower Paleozoic fold-block structure of the Western Sayan. Within its limits, two folded structures of regional significance are distinguished - the Dzhebash anticlinorium and the West Sayan synclinorium, the boundary between which runs along the Oisky fault. In addition, in the southeast of the territory, there is the eastern end of the Usinsky superimposed intermountain depression, composed of weakly deformed Upper Silurian and Devonian deposits.
Most of the territory is occupied by intrusive formations attributed to the Joy intrusive complex, which make up the Buiba and Berezovsky massifs and a number of small bodies, which, apparently, are satellites of the Buiba pluton.
The granitoids of the complex intrude and metamorphose Late Proterozoic, Late Silurian, and Early-Middle Devonian rocks. The age of the intrusive formations of the Joya complex in the studied area is dated as the Middle Devonian. The formation of the complex took place in four phases. They are fully represented only in the Buiba massif.
The first phase includes gabbro-diorites, diorites, quartz diorites and granodiorites. The rocks of this phase are involved in the structure of almost all massifs and small bodies. characteristic feature their is heterogeneity in composition and structure. The area occupied by them is about 80 km2.
The second phase of the formation of the complex is the main one. Adamellites, medium-grained granites, porphyritic granites with fine- and medium-grained groundmass, and coarse-grained weakly porphyritic granites are distinguished according to the compositional features, sizes of constituent minerals, and confinement to different zones. These varieties are interconnected by gradual transitions. Granites of the second phase intrude and metamorphize diorites of the first phase. The area occupied by it is about 470 km2.
The third phase is represented mainly by fine- and medium-grained granites, granite-porphyries. They are distributed only within the development of phase II granites, with which they have phase relationships. The area occupied by these formations is about 60 km2.
The fourth phase in the Joy complex is conventionally identified. It is represented by alkali-feldspar leucocratic and riebeckite granites. Granites of this phase were mapped over an area of ​​about 30 km2.
In relation to the folded structures of the enclosing strata, the massifs of the complex occupy a sharply discordant position. In plan view, they are slightly elongated in the meridional direction.
The largest of the identified massifs is Buibinsky with a total area of ​​about 600 km2. In the meridional direction, the studied part of the massif was traced for 32 km. The maximum width is up to 28 km in the northern part of the semitone, to the south it narrows to 13 km.
The Lower-Middle Devonian age of the Buiba complex is determined by the fact that it cuts through volcanogenic formations of the Kyzylbulak and Byskar series of the Lower-Middle Devonian.
In relation to the folded structures of the enclosing strata, the massif occupies a sharply discordant position. The enclosing intrusives are in the east, west and south-west the formations of the Upper Proterozoic that experienced regional metamorphism, in the south-east - the effusive rocks of the Kyzylbulak series of the Early-Middle Devonian. At contact with granitoids, the rocks of these sequences are intensely hornfelsed.
The landforms of the studied area were formed as a result of a complex interaction of various factors. These structures are based on an endogenous factor associated with arch-block movements that occurred in the Western Sayan at the border of the Tertiary and Quaternary periods and turned this area into a mountain structure.
The Quaternary history of the formation of the relief of this territory is inextricably linked with the processes of repeated glaciation, against which the erosional activity of the modern river network subsequently developed. Subsequent erosion and denudation in some areas almost completely masked the traces of past glaciations, but in most cases they are noted in fairly recent preservation.
Morphological features largely depend on the geological structure of the region. The western and extreme northeastern parts of the described territory, composed of metamorphic rocks of the Upper Proterozoic, are characterized by an extremely indented relief and steep slopes of individual ridges and peaks. The volcanic-sedimentary rocks of the Devonian and the southeastern part of the area were partially denuded and acquired a relatively smooth outline, which differs from the relief of typical alpine regions.
The central part of the region, composed of intrusive formations of the Buiba massif, is characterized by high-mountainous alpine landforms - sharp peaks, ridges, steep slopes, an abundance of kars with numerous lakes. Relative elevations reach 1000 m. Rocky peaks rise 300-500 m above the passes. Separate bald mountains and, especially, bald mountain ranges with elevations of 2000 m or more are indented by numerous deep and large cirques. The bottom of the caravans is usually at the level of modern woody vegetation (1500-1600 m). Due to the abundance of deeply incised kars, the tops of such barrens and ridges have a sharp ridge and bare rocky steep slopes. There are also flat-topped loaches /93/.
In general, this area is characterized by the predominance of denudation processes over accumulation processes. Accumulative landforms are represented mainly by glacial, deluvial-proluvial and alluvial-proluvial deposits.
Currently, river erosion is in the process of recovery. This is evidenced by the underdevelopment of the river profile, especially in the zone of the Alpine highlands. The regressive deep erosion proceeding upwards along the valleys from the lower reaches has not yet reached the upper reaches of the rivers, where the typically pronounced trough valleys are well preserved.
Rivers on different segments of their course have different transverse profiles. In the upper reaches, the transverse profile of the river. Bol. Taigish, Mal. Taigish, Nizh. Buiba and Wed. The buoy is due to the accumulation of moraines and has a trough-shaped appearance. The stepping of their longitudinal profile is explained by the transverse shafts of terminal moraines 40 to 120 m high, between which there are gently sloping and almost flat bottoms, often hilly in places of the remains of the moraines themselves. In the lower reaches, the transverse profile of these rivers is V-shaped with convex slopes, and in some places even canyon-shaped.
The difference in the profiles of different segments of the valleys reflects the features of the latest tectonic movements.
Accumulative forms of riverine origin are mainly represented by deposits of floodplain terraces up to 1.0 m high.
On the slopes of the valleys of all large watercourses, deluvial-proluvial and alluvial-proluvial plumes and alluvial fans are observed, expressed in the relief in the form of inclined surfaces, ending in ledges up to 10-15 m high. The alluvium of the tributaries takes part in the formation of alluvial fans.
Glacial landforms are developed everywhere in the area and are represented by cirques, trough valleys, sheep's foreheads, smoothed and curly rocks and moraines.
Kars are the most common landform in the highlands. The shape of the kars in cross section is cauldron-shaped or bowl-shaped with large rocky walls, the height of which reaches hundreds of meters, and gently concave bottoms. Carriages are devoid of snow and ice, covered with rock fragments coming from weathered rocky slopes. Often at the bottom of the kars there are kar lakes, fed by melting snow and giving rise to streams and rivers. In connection with repeated changes in the altitude position of the snow boundary at various stages of glaciation, caravan stairs were formed.
Under the initial car, the walls of which go straight up into the sharp ridge of the ridge, below the slope are the second, third, etc., separated from each overlying by a clearly pronounced ledge tens of meters high. The youngest are the cirques in the near-top parts. The absence of active cars indicates a higher level of the snow line at the present time.
The valleys of the upper reaches of large rivers are typical troughs. They are distinguished by straightness, smoothed, slightly concave at the base and slightly dissected sides, and sharply conspicuous, the discrepancy between the development and size of the current flow. The tributaries of these rivers also have the appearance of troughs, which break off in ledges to the thalweg of the main trough. The height of the ledges reaches 100-150 m.
The open valleys on the watersheds of the Bol rivers are a peculiar sculptural heritage of the ancient glaciation. Taigish - MS. Buiba, Mal. Taigish - Top. Buiba, Mal. Taigish - Shadat. Their origins are unknown.
Moraine forms complement the peculiar glacial landscape of the area. They are located mainly in the valleys of large watercourses and are characterized by a combination of irregular hills, ridges, ramparts, between which there are depressions filled with water or swampy areas. In the middle reaches of the river Below the confluence of its two main sources, there are several rectilinear moraine ridges elongated parallel to the sides of the valley. They have a height of 10-15 m, an average width of 10 m, and are composed of boulders of granites placed in a sandy-clayey and fine-grained mass. The material is poorly sorted. The sizes of boulders reach 3-4 m. Similar deposits are noted along the valleys of the river. Lower Buiba, Mal. Taigish, Wed. Buiba, Top. Buiba. More powerful moraine deposits are noted in the valley of the creek. Golden, whose trough valley cuts

View of Ergaki from the M-54 highway


hanging stone


Mountain range of Ergaki ridge, glacial lake

Rock "Parabola"


"Sleeping Saiyan"


Panorama of Ergaki Park

ancient moraine. These data indicate a repeated act of glaciation in the studied area.
The permafrost relief in the work area is represented by upland terraces, kurums, and remnant forms.
Upland terraces are found in the near-top parts of all ranges of the area above the tree line. Climatic conditions here are more severe than in the valleys. Terraces are located one above the other. The height of the ledges reaches 50 m, the width is 100-300 m, the steepness of the slopes is 25-450, degrees 2-50. Upland terraces are formed very slowly, which is indicated by the fact that the walls of the cairns of the last glaciation cut off both ledges and terrace surfaces. Kurums are very characteristic of the slopes of the high-mountain relief. Their source of nutrition is the bedrock that forms the slopes. Kurums are formed only under certain lithological conditions, where rocks initially form large blocks and fragments (at least 2-3 dm) in the weathering bed. Therefore, kurums do not form on shales and metamorphosed sandstones. Kurums are developed almost everywhere on the ridges and tops of mountains, on saddles, on the slopes of ridges.
The steepness of the slopes is not critical. Kurums develop on steep and gentle slopes (3-50).
Their sizes and outlines are varied in plan. The surface of the kurums is uneven, complicated by gently sloping ups and downs.
Numerous tourists are annually attracted to this area by narrow, sometimes rocky ridges on the ridge and its spurs, with pointed picturesque peaks and steep slopes, often with cliffs and talus. Tourist trails are laid on the slopes, through widespread scree, and the rocks rising among them are remnants.
The highest point of the attraction is 2260 Zvezdny Peak. Other significant peaks: Ptitsa Peak, Mount Dinozavr, Molodezhny Peak, etc.
None of the valleys is similar to the other, as are dozens of lakes bearing poetic names: Marble, Rainbow, Ice, Mountain Spirits. The names of the rocks are no less figurative: Sleeping Sayan, Hanging Stone. Ergaki translated from Turkic means "fingers". Many rocks resemble them.
A geological landmark of a geomorphological type with elements of a petrographic type.
. The status of a natural monument was established by the Decree of the Council of Administration of the Krasnoyarsk Territory No. 107-p dated April 4, 2005 No. 351-13 dated June 8, 1977.

Autumn in Ergaki

Complex geological monuments of nature

Reserve "Stolby"
The state reserve "Stolby" is located on the watershed of the Kaltat River and the Mokhovoy Creek, the left tributaries of the Bazaikha River.
Despite the fact that the Stolby reserve is a protected area, the Stolbovsky massif located on its area and the picturesque syenite rocks genetically related to it do not cease to be unique geological objects. That is why in the literature "Pillars" are described as a geological monument of nature. In our opinion, this is a monument of a complex type (petrological-petrographic, geomorphological) of federal rank, which is of great scientific and aesthetic value. It is a major tourist-excursion and sports facility.
Picturesque syenite rocks - pillars, located in the vicinity of Krasnoyarsk, have long attracted people with their grandeur. The earliest written references to the "Pillars" date back to 1823. Prokhor Seleznev, a Krasnoyarsk miner, wrote: "The rocks are very large and wonderfully created ... Perhaps they say the truth that even in other lands you will not see such." In 1842 P.A. Chikhachev described: “The rounded pyramids are arranged in pairs. You might think that these are colossal ruins of some cyclopean buildings.
The Stolby reserve is located on the watershed of the Mana and Bazaikha rivers, the right tributaries of the Yenisei. Its area is 47.2 thousand hectares. The highest absolute heights do not exceed 800 m, and most of the area has heights in the range of 400-700 m above sea level. Almost the entire territory of the reserve is covered with dark coniferous taiga. There are small steppe areas. Its flora and fauna are rich and varied. In general, this is a complex natural reserve of the taiga zone of Russia.
Syenites, alkaline syenites, intruding Upper Proterozoic and Lower Paleozoic formations in the northwestern part of the Eastern Sayan, are attributed by many researchers to the Stolbovka complex of Devonian age. Some researchers describe these rocks as part of the Shumikhinsky complex.
One of the most typical representatives this complex is the Stolbovsky massif - a petrotypical (reference) massif of the Stolbovsky complex. In plan, the array has an oval, isometric shape. Its area on the day surface is about 36 km2. The exposure of the massif is satisfactory. Primary outcrops are frequent on all watersheds within the massif. All exotic rocks of the reserve are composed of syenite rocks of this massif. In general, these breeds are quite monotonous. The central part of the massif is composed of porphyritic biotite-hornblende syenites, in some places gradually changing into syenite-diorites.
In the marginal parts, these are coarse-grained and less often medium-grained alkaline syenites and nordmarkites. Very rarely, quartz syenites and granodiorites are noted here. All transitions between these breeds are gradual, without sharp boundaries. All varieties are characterized by a mattress-like, cushion-like, large-block parting. Dikes are mainly represented by syenite-porphyries, microsyenites, and veins of aplite-like syenites. The host rocks are hornfelsed.
The age of the rocks of the massif, according to radiological data, is from 302 to 460 Ma. Some researchers describe it as Early Devonian, others as Middle Devonian.
The formation of the Stolbovsky complex is associated with Devonian tectonic-magmatic activation in the northwestern part of the Eastern Sayan. A new stage of tectonic activity in the Pliocene and Anthropogenic involved the structures of the Eastern Sayan in the processes of blocky orogeny, the formation of the modern landscape, and the emergence of certain parts of the Stolbovsky massif on the surface. Geomorphologically pronounced rocky remains, called pillars, can be considered as prepared roof irregularities or syenite apophyses in the sedimentary rocks of the frame. The latter are easily destroyed under the influence of various exogenous processes under the conditions of the development of a denudation relief.

Rock "Manskaya wall"


Rock "Grandfather"


View of the central pillars from the rock "Fourth Pillar"


Rocks "First Pillar" and "Second Pillar"

Rock "First Pillar"


Rock "Feathers"

Within the reserve, 4 regions (groups) of rocks are distinguished. The closest to the city, 1.5 km from the village. Bazaikha - Tokmakovskiy district. Here are the rocks "Takmak", "Chinese wall", "Sparrows", etc., located in an amphitheater near the small river Mokhovaya (left tributary of the Bazaikha river). In the middle reaches of the river Kaltat is another - Kaltat district. Here are the rocks "Bell towers", "Sunken boat", etc. The third district Laletinsky (Tourist-excursion) is located 12-13 km from the city of Krasnoyarsk. Here are the most famous rocks - "Feathers", Grandfather, First Pillar, Second Pillar and many others. They are also located in an amphitheater at the head of the river. Laletina. The most remote from the city are the rocks of the "Wild Pillars" area - "Fortress", "Manskaya Baba", "Wild Stone", etc., located in the upper reaches of the Dry Kaltat River.
Despite the reserved regime, "Pillars" are visited daily by hundreds of Krasnoyarsk residents, guests of the city, including climbers and rock climbers. Therefore, a tourist-excursion area has been allocated on the territory of the reserve (with an area of ​​1.4 thousand hectares). Organized access of tourists is allowed here with the obligatory observance of the regime and rules of the reserve.

Ministry of Education of the Russian Federation

Russian State University them. Them. Kant

Faculty of Geography and Geoecology

Department of Country Studies and International Tourism

Abstract on the topic:

"GEOLOGICAL MONUMENTS OF THE EUROPEAN PART OF RUSSIA"

Performed:

5th year student

part-time department

Nikitina T.V.

Kaliningrad

2007

Introduction

Murmansk region

Republic of Karelia

Arkhangelsk region

Komi Republic

Leningrad region

Pskov region

Novgorod region

Vologda Region

Tver region

Yaroslavskaya oblast

Vladimir region

Ivano region

Kostroma region

Bran region

Moscow region

Kaluga region

Tula region

Kaliningrad region

Nizhny Novgorod Region

Kirov region

Bibliography

Introduction

The problem of conservation of geological monuments of nature (GNP) is very relevant. In most countries, environmental protection activities are regulated by clear and fairly strict laws at both the state and local levels; state programs for the preservation of the national natural heritage are being implemented; the European Association for the Preservation of the Geological Heritage (ProGeo) was established, under the auspices of which a number of international symposiums, conferences and working meetings were held; a list of World Heritage Sites is being created.

In Russia, the first step towards solving the problem of preserving natural heritage at the state level was the decrees issued in 1920 by the Council of People's Commissars on the creation of the Ilmensky National Reserve, on the protection of natural monuments, gardens and parks. After the adoption in 1960 of the Law "On Nature Protection in the RSFSR", with the active participation of the VOOP and the general public, intensive identification of natural monuments, including geological ones, began. In subsequent years, the country's leadership adopted a number of legislative and regulatory acts designed to streamline and introduce into the legal framework this, which has become an avalanche, the movement.

Currently, there are about 2,000 officially registered state geological natural monuments on the territory of the Russian Federation. Most of them were proposed by local history enthusiasts, for whom the main criterion was the recreational (beautiful landscapes, exotic landforms, beautiful rocks or outcrops, etc.) or balneological (healing springs) value of objects. Much less often, the scientific value of it as an object of knowledge of the natural history of the Earth became the basis for the selection of a natural monument.

This fully applies to manifestations of rare mineralization and mineral deposits, for which the criteria for classifying natural monuments are very vague. Back in 1934, V.A. Varsanofiev and R.F. Gekker pointed out the need to preserve the "reference areas of the mineral deposit", since with the full development of the deposit it will no longer be possible to obtain full view about its structure. However, there is still no specific definition of a "reference site" as such.

The preservation of the stratotypes of the stratigraphic units is clearly insufficient. Meanwhile, on the territory of Russia there are stratotype sections of 19 stages of the common stratigraphic scale, accepted in the practice of geological work of Russian geologists and approved by the MSC. These sections fully meet the criteria developed by the UNESCO International Commission on World Heritage for geological objects of world rank. However, only a few of these sections are approved as state natural monuments. Such an attitude towards the preservation of stratotypes largely contributes to the displacement of Russian stratigraphic developments from the world stage. Even without being recognized by the international geological community, these sections, associated with the names of prominent geologists, remain monuments to the history of the development of geological science in Russia and need to be carefully preserved.

This publication is the first attempt to present a brief summary of rare and unique geological objects in our country. Its main goal is to attract the attention of the general public, scientific - first of all, to valuable natural formations of historical, scientific, aesthetic or recreational significance. These objects, created by nature over many millions of years, must be preserved in their natural form.

Any natural object, including geological, is part of a common ecosystem. The typification of geological monuments used in the work is, to a certain extent, conditional. On the basis of the main scientific interest, eight main types of GSP are distinguished: stratigraphic, paleontological, mineralogical, petrographic, tectonic, geomorphological, hydrological-hydrogeological and historical-mining-geological. In the case of approximately the same significance of two or more features, the monument is classified as complex.

In preparing the monograph, the authors encountered problems in assessing the significance (ranking) of geological monuments. The existing regulatory documents do not contain criteria for the uniqueness or value of geological objects, there is no specific definition of reference areas of mineral deposits. Meanwhile, any assessment of the significance of the GSP should be based on a system of clear, clear, unambiguous criteria and be carried out by a group of experts, ideally including specialists in all geological disciplines, as well as specialists in the field of environmental planning and management.

In addition to geological objects classified as monuments in the prescribed manner, the monograph includes objects that are proposed for classification as natural monuments. Among them are deposits of rare beryllium minerals, unique mineralogical objects of the Kola Peninsula, Murun and Tazheran massifs, stratotype sections of the stages of the General Stratigraphic Scale approved by the ISC, unique geomorphological and hydrogeological exotics.

Information about the geological natural monuments of Russia, given in this paper, represents an insignificant part of the information accumulated to date. The publication of the entire data bank requires enormous costs associated with the preparation and publication of several tens, and possibly hundreds of volumes of fundamental descriptions.

Murmansk region

1. Lake Grave

On about. Kildin, located in the Barents Sea, near the coast of the Kola Peninsula, is one of the most interesting lakes in our country, which is a natural monument of the hydrogeological type of world rank.

This is a relict lake, which was once part of the sea and was formed as a result of raising the coast. This phenomenon is quite common and usually leads either to complete desalination of newly formed lakes, or to their complete salinization. But that's what makes Lake. Mogilnoye, that such a peculiar balance of fresh and sea water has been established here over the millennia, which has created the possibility of the simultaneous development of marine, brackish-water and freshwater organisms. There is no other such reservoir not only in Russia, but possibly in the world. The area of ​​the lake is 96000 sq. m, length - 560 m, width - 280 m, the greatest depth reaches 17 m. The water is transparent green. The hydrochemical balance of salt and fresh water is maintained by seepage of sea water through a shaft up to 70 m wide and 5.5 m high, which separates the lake from the ocean. Strong desalination of the surface layers due to surface precipitation extends to a depth of 5 m. According to the degree of salinity, 4 zones are distinguished in the lake. The first three are the most populated. Among freshwater organisms, there are 13 species of rotifers, 21 species of crustaceans, etc., among marine organisms, polar jellyfish and crustaceans predominate; the second layer is inhabited by a peculiar variety of sea cod. In the lower zone, at a salinity of 33%, hydrogen sulfide is intensively released by purple bacteria. The area of ​​the GPP is 16 hectares.

2. "Lamb's forehead" at Lake Semenovsky

Near lake. Semenovsky, located within the city of Murmansk, there is a GPP of a geomorphological type of federal rank. It is an outcrop of Archean granites in the form of an asymmetric rounded convex ledge; geologists call such protrusions "ram's foreheads". These are rocks processed by the action of a glacier moving through them. Their surface is smoothed, covered with furrows and strokes. From the side, the outlines of the rocks resemble the profile of a sheep's forehead (the slope facing the direction from which the glacier moved is gentle, and the opposite one is steeper). By the shape of the outcrop and by the orientation of the furrows, one can judge the direction of the movement of the glacier, and by their depth, the relative thickness of the ice sheet. The study of such documents of the geological chronicle allowed scientists to establish that in the Quaternary period of the history of the Earth, the Kola region was the center of three glaciations: the oldest - Likhvinian, maximum Dnieper and the last - Valdai, which ended with melting and retreat of the ice sheet, which was recorded in the form of "lamb foreheads "and boulders. The area of ​​the GSP is 0.5 ha.

3. Yubileynaya pegmatite deposit

Geological monument of nature of the federal rank of the mineralogical type. The object is located in the Lovozersky district. The Yubileynaya pegmatite deposit was discovered in 1970 by geologists A.I. Merkova and A.P. Nedorezova. It contains about 50 minerals, including 12 new ones: bornemanite, vitusite, vuonnelite, zorite, ilmajokit, laplandite, lovdarite, penkvilksite, raite, sazhinite, terskite, saffranskovit. The deposit is located at the contact of lujavrite (lying side) and foyaite horizons, gently dipping to the southeast. The lujavrites of the recumbent side are not changed, their contact with the deposit is even and clear. The surface of the hanging side is uneven, foyaite is strongly corroded and contains many small cavities. Apophyses extend from the deposit into it. The structure of the vein is asymmetrically zonal. A thin feldspar rim runs along the contact with lujavrite. Above is a zone up to 0.5 m thick, composed of large blocks of microcline, eudialyte, grains of sodalite, prisms and radiant aggregates of aegirine and amphibole, coarsely formed lorenzenite individuals. Elatoliths are abundant here - herringbone cavities left after the dissolution of some skeletal crystals, which, judging by their shape, had cubic symmetry. It is most probable that the protomineral of the elatoliths was williomite. In the same zone, but closer to the center of pegmatite, there are large (up to 20 cm) radial fibrous spherical segregations of green aegirine, the so-called "bombs", very viscous and strong. Together with them, brown plates of lomonosovite are present in large quantities, often collected in fans and rosettes. The transition to the central zone is marked by a gradual change of microcline with pink granular natrolite. The central zone, which is the most richly mineralized, rarely exceeds 30 cm in thickness. The main mineral here is natrolite of a characteristic pink color, often containing tablets of snow-white microcline, black prisms of amphibole, and accumulations of later dense or free-flowing white sugar-like natrolite variety.

Among white natrolite in voids and even in foyaite at the contact with the deposit, a specific late complex of low-temperature, water-rich minerals develops: raite, zorite, penquilxite, etc.

4. Ploskogorskoe deposit of amazonite "Mountain Ploskaya"

The Gora Ploskaya deposit, the world's largest deposit of ornamental amazonite, is proposed as a mineralogical natural monument of world rank. The deposit is located on the territory of the Lovozersky district, on the watershed of the Sakharnaya and Elreka rivers, in the Western Keivy. The deposit is the most striking vein body of amazonite pegmatites in terms of its manifestation form, scale, diversity of mineral composition and complexity of mineral formation processes. Geologically, the area of ​​the deposit represents a sag of the roof of an array of alkaline granites (Lower Proterozoic), composed of gneisses and shales of the base of the Keivy series (Upper Archean), in which, on an area of ​​about 1 sq. km, there are more than a dozen pegmatite veins with a length of 10 to 300 m and a thickness of 0.5 to 30 m. Among them, the largest and mineralogically interesting is vein No. 19. Vein No. 19 has a concentric-zonal structure. The marginal zone is composed of a quartz-amazonite-albite granite-like aggregate with an obscure structure. The intermediate zone, which occupies up to 80% of the volume of the vein, is composed of a giant-grained amazonite aggregate, in which its monoblocks are 1-2.5 m in diameter, and on their border there are often plates of biotite-protolithionite up to 1-1.5 m in diameter with a thickness up to 10-20 cm. The axial zone of the vein is composed of discontinuous blocks of quartz up to 8 m thick, framed by euhedral amazonite crystals, plates and nests of protolithionite-zinwaldite, rosettes of clevelandite and containing isometric segregations of yttrofluorite up to 0.8-1.2 m. Against the background of pegmatite, segregations of fine-grained lamellar albite are observed, containing accessory Y-, Y-TR and Nb-Ta minerals, with a total number of more than 30. Among them are 6 new mineral species: wuntzpachite, keivite, Y-keivite, khinganite, Yb-khinganite, Y- cooli-okit, as well as several new, not completely identified minerals. The total number of mineral species at the site reaches 70, many of which are extremely rare, while others, such as plumbomicrolite, form crystals that are unique in size and shape. Another unique feature of vein No. 19 is the exceptional variety of amazonite varieties, which differ in tone and intensity of color, the number and shape of perthite ingrowths.

5. Amazonite deposit of Mount Parusnaya

Amazonite pegmatites of Mount Parusnaya are a geological natural monument of local importance (proposed rank federal facility). Complex type object - mineralogical and petrographic. The deposit is located in the Lovozersky district, 80 km east of the village. Lovozero. Fields of amazonite pegmatites in the central part of the Kola Peninsula were discovered in the 1920s. of our century in connection with the massifs of alkaline granites. Among the fields of amazonite pegmatites, the most grainy and typical is the Zapadno-Keivskoye. Amazonite pegmatites of Mount Parusnaya are located on the southeastern flank of the field. A series of eight echelon-shaped veins is located between the Parusnaya and Avdotya mountains. One of the explored pegmatite veins 35 m long and 4.5-6.5 m thick lies in biotite-plagioclase gneiss. The vein is characterized by an asymmetric zonal structure and is composed of large blocks of granite-pegmatite and pegmatoid from the recumbent side. Towards the hanging side in the vein, the number of quartz blocks significantly increases, to which prismatic segregations of bluish-green amazonite-perthite are confined. These segregations are up to 1.8 m long and up to 0.7 m wide. This is practically the only place in Russia where well-formed druses of short-prismatic bright blue-green and emerald-green amazonite crystals are found. Similar formations develop along cracks in block pegmatite and along veins in the vein selvedge. The sizes of crystals in druse vary from a few millimeters to 5 cm, rarely more. The veins also contain plagioclase, biotite, magnetite, fluorite, hematite, gadolinite, titanite, and other minerals.

6. Pegmatites of the Little Puncaruive Mountain

Geological nature monument of federal rank of mineralogical type; is located in the Lovozero region, in the southeastern part of the Lovozero mountain range. Ten small geological bodies (veins) are known on the northeastern slope of Mount M. Puncaruive, which contain the rarest minerals specific to alkaline pegmatites. More than 35 mineral species have been noted here. Among them are eudialyte, ramsaite, murmanite, neptunite, epistolite, chkalovite, nordite, calamine, etc. The most valuable are significant accumulations of lilac or white ussingite, a very rare pegmatite mineral.

7. Astrophyllites of Mount Eveslogchorr

Geological monument of nature of the federal rank of the mineralogical type. It is located within the Eveslogchorr tectonic zone. It is offered as a world-class GPP of complex type. It is located on the Kola Peninsula, on the territory subordinated to the Kirov city administration. The first study of recrystallized and cataclased nepheline syenites within Mount Eveslogchorr was carried out in the 1930s. employees of the Academy of Sciences under the leadership of Academician A.E. Fersman, who noted the presence of a number of minerals unusual for the Khibiny, such as spinel, corundum, rutile, anatase, clinoenstatite, and lovenite.

The Eveslogchorr tectonic zone is confined to the contact between massive aegirine rischorrites and uneven-grained nepheline syenites and foyaites. In the contact zone of rischorrites with foyaites, the rocks contain numerous xenoliths of hornfelsed volcanic-sedimentary rocks. About 150 vein formations are known within the Eveslogchorr zone, including pegmatite bodies, albite, aegirine, natrolite and other rocks, each of which is a unique object. For example, the well-known Astrophyllite stream, where pegmatites and hydrothermal veins with large crystals of fersmanite (up to 3 cm) and wadeite (up to 2 cm), the famous Eveslog-Chorr astrophyllite suns were found.

In the postmagmatic formations of the Eveslogchorr tectonic zone, for the first time for the Khibiny massif, 27 rare minerals were found. Two of them - perlialite and denisovit - were discovered in nature for the first time. To date, the vein bodies documented within the zone contain at least 120 minerals from almost all classes of mineral species.

8. Cape Ship

Geological monument of nature of federal significance of the mineralogical type. Cape Ship is located on the shores of the Kandalaksha Bay of the White Sea (Tersky coast), 16 km east of the village. Kashkarans. The first mention of amethysts from Cape Korabl dates back to the 16th century. An extensive ledge, composed of red-colored sandstones of the Terek Formation with amethyst mineralization, represents this unique deposit. Cape Korabl is a stockwork type deposit. Crushing zones of red sandstones and siltstones contain numerous quartz veinlets and leaching voids. The central part of the stockwork is cemented by quartz, carbonate and fluorite. Amethyst mineralization is developed on the walls of differently oriented cracks, mainly in the hanging side of stockworks.

In brushes, the dimensions of which reach 500 square meters. cm, crystals from the first millimeters to 2 cm predominate. The intensity of the purple color of the crystals varies not only in different parts of the deposit, but even within individual individuals from light lilac - at the base, to deep purple with a smoky tint - towards the top. Sometimes in amethyst there are needle-like inclusions of goethite. In the western part of the Cape Korable (Fluorite stock) deposit, red sandstones are intersected by numerous veinlets 5–15 cm thick, consisting of alternating bands of dark purple and white fluorite.

9. Waterfall on the Chavanga River

It is located on the territory of the Tersky district, 17 km from the village of Chavanga upstream of the river of the same name. It is a GPP of a geomorphological type of federal significance. In this area there is a sharp lowering of the relief in the form of a three-step staircase. The bedrocks composing these ledges are represented by Archean granites and gneissic granites.

The clean, transparent water of the river falls in three cascades 2.5 m high (the highest), 3 m and 4.5 m high. In general, this entire section of the river is exceptionally picturesque, one of the most beautiful in the European North of Russia. The buffer zone includes strips 500 m wide along both banks at a distance of 1 km (total area 100 ha).

10. Waterfall on the Chapoma River

In the same area there is another geomorphological monument of nature of the federal level. This is the largest waterfall in the length and height of the fall of water in the Russian north on the Chapoma River, to which paths have been laid from the village of the same name. In the bed of the river, four ledges are formed by granite-gneiss, the lower of which rises above the midstream of the river by more than 20 m. Throughout the cascade of waterfalls, the area has an exceptionally picturesque wild character due to the extremely turbulent nature of the water flow and a heap of blocks and boulders. The protected zone includes a river bed 500 m long and a shore strip 1 km wide.

11. Epidosites of Cape Upper Navolok

Outcrops of epidosite rocks of Cape Verkhniy Navolok are a geological monument of nature of the federal rank. The type of monument is complex, petrographic and mineralogical. Location of the object - Kandalaksha district, southern coast of the Kandalaksha Bay, cape on the Tolstik peninsula. In a coastal rocky outcrop 200 m long and more than 70 m wide, rocks of unique composition were uncovered, consisting almost entirely of minerals of the epidote group of various mineralogical types, habits, and orientation. The rocks are part of the Khetolambi Formation of the White Sea Archean Series. The formation is characterized by an association of biotite amphibole-bearing gneisses (often with epidote) and amphibolites interbedded or forming separate horizons. Occasionally, epidote-zoisite gneisses and shales occur in the section of the suite.

Epidote-zoisite gneisses and shales (epidosites) are gray and greenish-gray in color, granoblastic, sometimes porphyroblastic texture. The groundmass is represented by clinozoisite, with small amounts of zoisite, plagioclase, quartz, amphiboles, and garnet. The apparent thickness of the layer is about 20 m. Along with this layer of epidote-zoisite rocks, which is very interesting in its composition and geological position, the layer of fine-grained amphibolites that is exposed here is no less interesting and rare. The amphibolites of Cape Verkhny Navolok are unique in that they have retained primary features that can be used to restore the nature of underwater lava flows. The underlying thinly banded rhythmic amphibolites testify to the cyclicity of the processes of ancient sedimentation and volcanism.

12. Granitoids of Mikkov Island

Within the territory subordinated to the Kandalaksha City Council, on the island located at the outlet of the Bolshaya Kovda Bay to the Kandalaksha Bay, there is a federal petrographic type state checkpoint. Here, granitoids (the absolute age is about 2.3-2.4 billion years) appear in a natural outcrop, which are an example of the remelting of more ancient gneisses and amphibolites, the remains of which in the form of fragments and blocks have been preserved among granites. This unique object is of great interest to geologists dealing with problems of deep granite formation. The area of ​​the SNP with a buffer zone is 10 hectares.

Republic of Karelia

1. Section of the zone of marginal glacial formations

In the Muezersky district, near the village of Lendery, it is proposed to classify a unique set of classical forms of glacial relief as a geomorphological type state reserve of the federal level. The complex of marginal glacial formations is a strip of accumulative hilly-ridged relief, the relative height of which reaches 80-85 m. The hills and ridges are folded into varying degrees sorted sands with gravel, pebbles and boulders. Many forms of glacial formations have been identified here: sands, eskers, kams, moraine hills and a finite moraine landscape. Considering that many issues of the history of the glacier melting have not yet been unequivocally resolved, including the boundaries of the maximum stage of the last glaciation, it is absolutely necessary to preserve the territories where the actual evidence of the presence of the glacier is so well expressed.

2. Severinsaari Island

O. Severinsaari is located on the lake. Segozero, 10 km southeast of the village. Padany Medvezhyegorsk region. Approved in 1984 as a State Nature Reserve of a republican rank with a custom protection regime. It is proposed as a paleontological monument of nature of a federal rank.

The area of ​​the island is 0.54 hectares. In the coastal cliffs of the island, pinkish-gray dolomites of the Karelian complex of the Upper Jatulian of the Lower Proterozoic (age - about 2 billion years) are exposed, containing a unique complex of organic remains (stromatolites, microphytoliths). For some species, the location is the only one in the world.

3. Dülmec Island

In the southeastern part of the lake. Segozero, on about. Dyulmek, 10 km northeast of the village. Karelian Maselga of the Medvezhyegorsk region, in the rock outcrops, deposits of the Upper Jatulian (Lower Proterozoic) are exposed, containing a specific complex of organic remains (an analogue of the complex of organic remains in the section of Severinsaari Island). Approved in 1984 as a SPP of the republican rank, the area of ​​the monument is 0.35 ha. It is proposed as a paleontological monument of federal rank with a custom protection regime.

pink fine-grained dolomites (layer 1; 7.9 m);

gray dolomites (layer 2; 1.1 m);

· mottled lilac-pink dolomites (layer 3; 4.5 m);

light pink and cream sandy dolomites (bed 4; 7.7 m);

variegated (pink with cherry interlayers) dolomites (layer 5; 13.2 m);

pink dolomites (layer 6; 8.3 m);

pink stromatolitic dolomites (layer 7; 8.2 m);

· lilac-pink dolomites (layer 8; 2.9 m);

pink wavy-layered dolomites with peculiar dome-shaped shapes (up to 20 cm), reminiscent of buildings Collenia (line 9; apparent thickness 9 m).

4. Girvas section of the Suna river canyon

On the territory of the Kondopozhsky district, in the southern part of the village of Girvas, a section of the Precambrian strata belongs to the GBP of a complex type of federal significance. In the walls of the canyon Suna discovered the contact of sedimentary and volcanic rocks of the Lower Proterozoic. The textures of lava flows are clearly visible here: globular and columnar fragments in basalts, amygdaloidal porphyritic and massive textures. Sedimentary strata, represented by conglomerates, gravelstones and quartzite-sandstones, have preserved bedding types and ripple marks indicating the alluvial genesis of these deposits. The section is characterized by manifestations of hydrothermal minerals: epidote, chlorite, tourmaline, etc. The Girvas section attracted the attention of many prominent researchers - G.P. Gelmersen, A.A. Foreigners, V.M. Timofeeva and others. Protected zone - 6 hectares. GSP has features of stratigraphic and petrographic types.

5. Waterfall Kivach

It is located near the central estate of the reserve of the same name, belongs to the geomorphological monument of nature of the federal rank. The Kivach waterfall was the second largest flat waterfall in Europe (after the Rhine), but after the creation of a dam above Girvas in 1936, its power decreased significantly. But even now it is a majestic sight: the water falls in four ledges from a height of 10.7 m. Suna strata of loose Quaternary deposits up to the top of the diabase ridge. Throwing down from the cliff, the stream deepened the river bed in the thickness of lake loams and sandy loams below the ridge

6. Shungsky section

Geological natural monument of federal rank, type - mineralogical. The object is located in the Medvezhyegorsk district, in the village. Shunga on the northwestern shore of the lake. Putkozero. The history of Karelian shungites begins in 1785-1792, when the first fragmentary data about the "black lands" in the Olonets region appeared. In 1842, N.K. Komarov discovered large accumulations of "resinous rock" in the area of ​​the village of Shunga. In 1879, Professor A.A. Inostrantsev defined the "mineral" as "the last member in the series of amorphous carbon" and named shungite after the place of its first discovery. Currently, schungite substance is defined as non-graphitized carbon with a globular supramolecular structure in a metastable state. The presence in the structure of chain fragments that unite "elementary globules" - fullerenes, according to many authors, should be considered the main feature of shungites.

Within South Karelia, carbon-bearing rocks are included in the sediments of the Zaonezh and Suisar suites of the Lower Proterozoic and stand out in the "shungite-carbonate-shale sequence". Later it was found that the structure of carbon matter, depending on the depth of metamorphic transformations, is different in these deposits. In most cases, carbon has a degree of crystallinity ranging from graphite to crystal clear graphite.

The amorphous form of carbon, shungite itself, is common in the rocks that form the core of the Onega trough (North-Western Onega region). This is the only large shungite-bearing structure of the Early Proterozoic age in the world. Its area is almost 10,000 sq. km at a thickness of deposits containing shungite of about 1200 m.

Formations of the Zaonezhskaya suite are subdivided into two subformations: the lower - sedimentary carbonate-argillaceous and the upper - sedimentary-volcanogenic, shungite-containing.

In the area of ​​Shunga settlement, on the watershed isthmus between the lakes Putkozero and Valgmozero, on the slopes of a hill elongated from northwest to southeast, schungite rocks are traced in rocky outcrops and adits. From top to bottom along the section, black shales are observed, then, alternating, layers of black dolomite, weakly siliceous coal shale, lidite and shungite. The latter is represented by two layers. In the upper, relatively thin, interlayers and lenses of shiny dense shungite of the first difference are common. These almost monomineral formations contain up to 99.6% pure carbon. Below lies a thick layer of shungite rocks with a carbon content of up to 75%.

7. Cape Kintsiniemi

On the eastern shore of the lake Small Janisyarvi, in the area of ​​Cape Kintsiniemi, in the sides of the dolomite quarry and in the coastal cliffs of the river. Soaneki, rocks of the Pyalozero Horizon of the Middle Jatulian of the Lower Proterozoic (lower Karelian complex) are exposed, containing an unparalleled ancient (about 2 billion years) complex of organic remains (oncolites and stromatolites). The section is also parastratotypical for the Onega horizon and typical for the carbonate deposits of the Jatulian of the Ladoga region. This locality, known in the world literature under the name "Kintsiniemi", was taken under protection as a paleontological and stratigraphic natural monument of federal rank. The monument covers an area of ​​50 hectares.

In the section from bottom to top, they open:

pink siliceous dolomites (layer 1; apparent thickness 0.5 m);

· dark gray clayey dolomites (layer 2; 1 m);

· light gray quartz sandstones with rare oncolites (bed 3; 0.5 m);

· pink dolomites with interlayers of argillaceous-siliceous shales in the upper part (bed 4; 1.3 m);

gray carbonate-argillaceous shales (layer 5; 0.3 m);

· pink quartz sandstones (layer 6; 0.7 m);

· dark gray argillaceous-siliceous shales (layer 7; 0.5 m);

brownish-pink, with a greenish tint in the upper part, dolomites (layer 8; 0.4 m);

· greenish-gray tuffaceous siltstones (bed 9; 0.2 m);

· dark gray argillaceous-siliceous schists, overlain by underlying deposits with tectonic contact (layer 10; 3 m);

· pinkish-gray quartz gravel-sandstones (bed 11; 0.5 m);

pink massive dolomites (layer 12; 4.2-5 m);

pink dolomites with numerous voids and caverns and formations resembling oncolites (layer 13; 2.5 m):

Spotted sedimentary dolomitic breccia (bed 14; 0.3 m):

· cherry-gray clayey dolomites (layer 15; 0.7 m);

pinkish clastic dolomites (layer 16; 0.8 m);

· cherry-pink thin-layered dolomites with vertically oriented stromatolite structures (bed 17; 2.2 m);

Cherry-gray to black dolomite-siliceous schists (layer 18; 0.3 m):

· pinkish stromatolitic dolomites (layer 19; 40 m);

· "undivided" dolomites (bed 20; exposed in small fragments in a gentle slope of southwestern exposure; apparent thickness 15 m).

8. Martial Waters

54 km north of Petrozavodsk there is a hydrogeological natural monument of federal rank - the Marcial Waters resort. It was founded by Peter I on the basis of mineral waters, the outcrops of which are confined to the contact of pyritized carbonaceous shales of the Lower Proterozoic with Quaternary deposits.

According to the chemical composition of water - bicarbonate-sulfate calcium and magnesium, with an iron content of 36-95 mg/l. Associated elements are copper, manganese, nickel, cobalt. The enrichment of waters with iron occurs in the process of their circulation through the zones of numerous tectonic faults and the crushing zones accompanying them due to the decomposition of pyrite. The flow rate of four springs coming to the surface in the village of Dvortsy changes from 0.5 to 2.5 liters per second in summer. Martial waters are widely used in the treatment of diseases of the blood, stomach, liver, kidneys and metabolic disorders.

9. South Deer Island

South Oleniy Island, one of the islands of Lake Onega, is located in the Kizhi skerries system, 12 km east of about. Kizhi. As a state monument of nature of the republican rank, it was approved in 1981. It is also archaeological site. The island is elongated in a northwestern direction; its length is about 2.5 km, width reaches 0.5 km. The area of ​​the island is 75 hectares. In 1936-1938. employees of the Leningrad Institute of Archeology conducted archaeological excavations, as a result of which it was found that about 5 thousand years ago, in the late Mesolithic, the South Oleniy Island was a tribal burial place (cemetery) of the ancient inhabitants of the coast of Lake Onega. More than 170 graves have been discovered here. Traces of a later - Neolithic - "tool" workshop were also found on the island: primitive people came here to prepare stone tools - axes, spearheads, chisels, grinding plates, etc. In the 17th century. limestone was mined on the island for the first "iron-working" factories in Karelia. After 1917, a special stone-mining enterprise was created here - Olenyeostrovskiye lime mining. By 1956, the deposit was practically depleted and the quarry was closed. The island is composed of terrigenous-carbonate rocks of the Oleneostrovsky horizon of the Onega series of the Karelian complex of the Upper Jatulian (Lower Proterozoic - about two billion years old). The rocks are highly dislocated and compose the southwestern flank of a large anticline fold, the northeastern flank of which is submerged. In the north of the island, rocks fall to the southwest at an angle of 2-5 degrees, in its middle part - 15-20 degrees and in the south - 40-70 degrees. The section exposed on the island is a stratotype of the Oleneostrovsky horizon.

In the section from bottom to top, the following are exposed:

limestone-dolomite member

· pinkish and yellowish clastic dolomites (bed 1; apparent thickness 2 m);

· gray siliceous dolomites with numerous remains of stromatolites and oncoliths, with lenses, dome-shaped bodies, stocks and intercalations of pinkish-white marble-like limestones (bed 2; 4 m);

· gray, locally siliceous, stromatolitic dolomites with lenses and interlayers of white marble-like limestones, remains of stromatolites and oncolites (bed 3.4; 11 m);

· pink siliceous oncolite-stromatolitic dolomites with dome-shaped bodies of white marble-like limestones (bed 5; 4-5 m);

red-colored dolomite member

· yellowish clayey dolomites with remains of stromatolites and oncoliths (bed 6; 3 m);

· yellowish-pink platy dolomites with occasional interlayers of light marble-like limestones, algae remains, and stromatolite structures (bed 7; 3 m);

· pinkish-yellow siliceous thin-layered dolomites with rare stromatolite structures (layer 8; 4 m);

· gray massive dolomites without visible organic residues (layer 9; 4 m);

· pinkish-gray, siliceous in places, dolomites with rare problematic formations (bed 10; 10 m);

· pinkish-gray quartz sandstones with lenses and interlayers of sandy dolomites (bed 11; 2 m);

· pinkish and red clastic dolomites with large dome-shaped stromatolite bioherms in the upper part (bed 12; apparent thickness 17 m). The total thickness of the exposed deposits of the Oleneostrrva horizon is 65 m.

10. Ruskeala village

On the territory subordinated to the Sortavala city council, old quarries are of great interest - a monument to the history of mining in Karelia - a federal-level complex-type SNP. The famous Ruskeala marble, which was widely used in the construction of St. Petersburg, was mined here. Marble medium-grained, calcite and dolomite, white, gray and banded. It was used for facing St. Isaac's Cathedral and the Marble Palace. The deposit was formed in the Early Proterozoic and is a steeply dipping lens up to 50 m thick. The GSP has features of petrographic and historical-geological types.

11. Scapolite Hill

Geological monument of nature of federal significance of the mineralogical type. Located on about. Pusunsari (Northern Ladoga), Pitkyaranta. The environs of Pitkyaranta have been studied by geologists since the 18th century. (Alopeus, 1787), however, a detailed study of carbonate rocks was carried out in 1907 by Trustedt. According to recent data, metamorphosed limestones (skarn-like rocks of the Ladoga formation) are predominantly diopside rocks with scapolite, actinolite, tremolite, biotite, spinel, epidote, sometimes with quartz, plagioclase, and garnet. In some cases, scapolite forms large accumulations in contact with pegmatite bodies. Well-formed crystals, radially radiant aggregates of scapolite are known on the islands of Syuskynsaari and Radatchunsaari. The two largest accumulations of scapolite are located on about. Pusunsari. The scapolite hill is composed of white-pink scapolite, the crystals of which reach 40-50 cm in diameter. The apparent thickness of the scapolite vein is about 50 m. In the western part of the island there is another scapolite vein up to 15 m thick. The size of the crystals reaches 20-30 cm. Rutile is present in the scapolite in the form of small dissemination.

12. Uksinskaya ozovaya ridge

In the Pitkyaranta region, near the lake. Louhijärvi, on an area of ​​1500 hectares, esker ridges are subject to protection - a unique example of the development of a glacial landscape, a geomorphological SNR of federal rank. The central part of the system is composed exclusively of boulder material, and a fluvioglacial delta is developed at the confluence of two esker chains. The classical nature of the development of the glacial landscape and its easy accessibility make it possible to make the Uksinsky ridge an object of international geological excursions and a wide range of educational and educational tourism.

13. Valaam Island

On the territory of the State Museum-Reserve there is also an exceptionally scientifically valuable GSP of a complex type of federal rank. Here one of the youngest rocks of the eastern part of the Baltic Shield comes to the surface - the volcano-plutonic subalkaline complex of the Middle Riphean (their absolute age is about 1350 million years). The outcrops of these formations on the surface in the form of exotic rocks, coastal ledges and "ram's foreheads" make the landscape of the island unusually picturesque. The GSP is characterized by features of stratigraphic, petrographic and geomorphological types.

14. Shoksha quartzites. Shokshinskiye quartzites

In the Prionezhsky region from the end of the 18th century. Several quartzite deposits are known, among which the outcrops of these rocks near the village of Shokshi were of the greatest interest. Quartzite outcrops and old quarries (GPP of complex type of federal rank) are declared natural monuments. They are worked out in the thickness of sedimentary-volcanogenic rocks of the Lower Proterozoic, the outcrops of which are the reference and stratotype sections of Upper Karelia (Vepsian). According to the lithological composition, this sequence is divided into the Petrozavodsk series, represented by gray and grayish-green sandstones, and the overlying Shoksha series, composed mainly of red and crimson quartzites. Shoksha quartzite is a fine-grained, strong and durable decorative facing stone that can be mirror polished. Monochromatic dark crimson Shoksha quartzites, which were called "Shoksha porphyry", were especially valued. They were used to decorate the interiors of palaces and cathedrals, and architectural elements were made from them (monolithic columns of the lobby of the Old Hermitage and the middle part of the pedestal of the monument to Nicholas I in St. Petersburg). Red quartzites were also used for the manufacture of paving stones and crushed stone. Shoksha quartzites of the best quality were not found in large blocks, therefore they were especially highly valued. GSP bears the features of stratigraphic, petrographic and historical-geological types.

Arhangelsk region

1. Winter coast

On the coast of the White Sea, for about 50 km between the settlements of Nizhnyaya Zolotitsa and Bolshiye Kozly in the Primorsky region, rocks of the Ust-Pinezh and Mezen formations of the Valdai Series of the Upper Proterozoic are exposed in the coastal cliffs, containing the remains of the most ancient non-skeletal fauna. This is the largest and most representative locality of remains known in Eurasia. Metazoa . It is proposed as a world-class paleontological GSP with a custom protection regime. The best-known outcrop, up to eight kilometers long, is located between the Medvezhiy stream in the north and Ivovik in the south. The section reveals a thickness of gently dipping southbound weakly consolidated argillite-like clays, siltstones and sandstones up to 100 m thick. Numerous imprints of remains of non-skeletal organisms are found mainly in the lower and uppermost parts of the section; the scree contains rare imprints, presumably related to the middle part of the sequence.

2. Condozero

On the border of the Belomorsko-Kuloi Plateau and the Pinego-Kuloi Lowland, there is a lake proposed for protection as a hydrogeological type State Nature Reserve of the federal level. It belongs to the group of a rare type of meromictic lakes, the water mass of which in all seasons of the year is divided into two layers of different density, which do not mix. During the summer, below a depth of 8 m from the surface, the water temperature does not exceed 3 degrees. Higher it sharply increases and at a depth of 3 m in July reaches 20 degrees. In the bottom relief, 3 depressions are distinguished, filled with black silt with a hydrogen sulfide odor. The water is mineralized, calcium sulphate in composition. The mineralization of water on the surface is 612 mg/l, and in the bottom layers - 2019 mg/l.

3. White Sea Mountains (Iva Gora)

In the Mezensky district, on the right bank of the river. Soyany, 57 km southwest of its confluence with the river. Kuloy, located Willow Mountain. In the coastal cliff up to 100 m high, Upper Permian deposits are exposed, in which unique remains of the entomofauna (new species, genera and families of insects) are found. The section is also a stratotype of the Ivagorian beds. It is proposed as a paleontological SNP of federal rank with a custom protection regime. The red-colored rocks of the Ufimian stage are overlain by the deposits of the Kazanian stage, represented at the base by a member (4 m) of bluish-gray to black sandy marls with numerous charred plant remains and insect imprints (Ivagorsky layers). These layers are overlain by brownish-gray calcareous sandstones with rare remains of Kazanian bivalves and brachiopods. The section is completed by a member (19 m) of loose weakly cemented sandstones that do not contain organic residues. The collection of insects from the Ivagorian layers was collected in 1927 by M.B. Edemsky and edited by A.Z. Mytnikov in 1935

4. Big Gate Canyon

Within the boundaries of the Nenets National Okrug on the Northern Timan, a geological monument of nature of a complex type of federal rank is a section of the valley of the river. White. The canyon was formed where the river cuts through the thickness of basalt flows and interlayers of volcanic-sedimentary rocks (conglomerates, tuff sandstones, siltstones and mudstones) of Upper Devonian age with a total thickness of up to 220 m that separate them.

The famous agate mineralization of Northern Timan is associated with porous basalts. The composition of agate-bearing nodules is chalcedony, less often onyx, with a bizarre patterned pattern. Along with agate, there are unique geodes of rock crystal, amethyst and smoky quartz. The agate-bearing layer lies horizontally. Its exits to the surface look like narrow and long strips along both sides of the canyon. In the process of weathering, many agate concretions are washed out of the rootstock and deposited in the alluvium of the coastal spits of the river. White. GSP is characterized by features of mineralogical, stratigraphic and geomorphological types.

5. Kulogorsky caves

They are located on the territory of the Pinezhsky district and are the GNP of the geomorphological type of the federal rank. Several caves have been studied here, they were worked out in white gypsum-dolomite deposits of the Lower Permian, which are distinguished by tectonic fracturing. In terms of the variety of types of karst cavities, this territory occupies one of the first places in the country.

Kulogorskaya Troy is the largest cave in the Arkhangelsk region, and in terms of the length of the passages it ranks 3rd in the world among gypsum caves. It has many halls with an area of ​​​​30-50 square meters. m, the vaults of which are decorated with large gypsum crystals. Eleven deep lakes with very cold water have been found. The total length of the passages is 13.5 km. Kulogorskaya-5 belongs to the class of horizontal karst cavities, has 12 halls, underground reservoirs are represented by baths and lakes. The length of the passages is 2,035 m.

6. Lake Xiamgo

In the Plesetsk region, the lake, which is one of the largest periodically disappearing karst reservoirs, is classified as a hydrogeological monument of nature of the federal rank. It is elongated from north to south for 4 km with a width of 2 km. From time to time, water from the lake through ponors in the underlying limestones of the Middle Carboniferous goes into fissure-karst horizons. This happens once every 3-4 years, usually in winter. Within a few hours, the water disappears, and the basin of the lake is covered with ice that has settled to the bottom. After 2-3 weeks the lake is filled with the same water. The fish returns with the water. Such a specific regime of the lake is determined by the presence of large karst cavities in the limestone massif and their hydraulic interconnection with the lake. The preservation of the constancy of the species composition of fish indicates the absence of a connection between the lake and the modern river network.

Komi Republic

1. Vorkuta

In the banks of the river Vorkuta on the outskirts of Vorkuta, in the vicinity of the village. The mine, a stratotype section of deposits of the Rudnitskaya subformation of the Kungurian stage of the lower part of the Permian system is opened. The rocks contain numerous imprints and phytoleims of leaves, generative organs, seeds, and fossilized wood of Early Permian plants. It is offered as a complex GPP of federal rank with a custom protection regime. The section is represented by a layer of interbedded sandstones, siltstones, mudstones, and bituminous coals. It has 10 horizons with remains of marine fauna, as well as horizons where plant remains are found together with freshwater forms. The value of the site is determined by the fact that remains of cordaites and ferns with preserved vegetative and generative organs are observed here in situ burial.

The complex of plant remains is typical for many botanically and stratigraphically important species. The location is under threat of destruction due to the construction of a thermal power plant and the transformation of the territory of the monument into a landfill for household and construction waste. It is necessary to determine the area of ​​the GBP, install security signs and fences. According to I.A. Ignatiev, the location deserves the status of a paleontological reserve.

2. The upper gate of the Bolshaya Synya River

On the territory of the Pechora region, the exclusively picturesque canyon of the river. Big Son. The rocky sides of the canyon are composed of carboniferous limestones and dolomites. Their contact with the underlying Devonian sediments is well recorded, and organogenic Lower Permian limestones are exposed on the right bank.

On both banks of the river, rocks 70-80 m high are piled up, in which various forms of microrelief have been created by weathering, reminiscent of the outlines of people, animals, birds. The carbonate rocks are strongly karstized, there are manifestations of numerous and diverse karst forms - dips, funnels, caves. The river bed is rapids, the current is stormy. The GSP has features of geomorphological and stratigraphic types.

3. Lembeko-Yu (Yarenei section)

On the right bank of the river Kozhim, 40 km above the confluence of the stream. Yarenei-Shor, a section of boundary deposits of the Ordovician and Silurian systems, unique in its exposure and completeness, is being opened. The section is also a stratotype of the Yarenei horizon of the Silurian system and contains a rich complex of organic remains (stromatoporates, corals, gastropods, brachiopods). It was approved as a SPP of national rank by the Decree of the Council of Ministers of the Komi ASSR No. 193 of September 26, 1989.

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It is proposed as a geological monument of nature of the world rank of complex type. The facility is located 156 km from Yekaterinburg.

The deposit as the Mariinsky mine was discovered back in 1833 by the peasant Karelin, but active exploration and development began only in the late 40s. this century. The ore field of the emerald mines is located in the lateral exocontact of the vast, deeply eroded Adui massif of biotite and two-mica granites. The massif is part of a large belt of orogenic granite intrusions associated with the East Ural uplift.

Granites cut through a complex complex of metamorphic and intrusive rocks: Upper Ordovician amphibolites and amphibole schists, Lower Silurian carbonaceous-siliceous schists and ultramafic rocks, followed by serpentinites and talc schists, diorites, quartz diorites and diorite porphyrites of the Middle Carboniferous.

The endocontact and near exocontact zones of the Adui massif include columbite-beryl pegmatites (partially emerald-bearing), and at some distance there are emerald-beryl deposits associated with greisens. They are characterized by host rocks of ultramafic composition, which determined the development of a specific greisen facies - phlogopite mica, the appearance of emeralds and alexandrite colored with chromium borrowed from host rocks.

The ore bodies are represented by beryl-plagioclase veins and vein-metasomatic zones with emeralds. The veins fill discontinuous cracks in rigid blocks of competent rocks (diorites, serpentinites), have a predominantly sublatitudinal strike with a gentle dip.

Their thickness reaches 2-3 m. The main minerals are: oligoclase-andesine, albite, quartz, muscovite, beryl (including in the form of transparent crystals and druze), Be-margarite, fluorite, apatite (crystals up to 5-6 cm), molybdenite sockets. The zonal structure of the veins is characteristic.

Veinlet-metasomatic ore zones have a maximum thickness of 5-10 m and are located in tectonically weakened areas. As a result of intensive crushing and crushing, they acquired a lenticular-block internal structure. Blocks ("nodules") consist mainly of phlogopite mica, including fragments of boudinated veins and veinlets of beryl-plagioclase, beryl-muscovite, and other compositions. It is in the zones that crystals of emerald, chrysoberyl (including alexandrite), and phenakite are concentrated. A single find of bromellite is known.

Additional mineralogical interest to the deposit is given by the intensive development of the post-ore hydrothermal stage, during which there is a partial decomposition and dissolution of beryl and plagioclase and redeposition of beryllium in the form of a complex of secondary minerals. Beautiful brushes, druses, spherulites and individual crystals of bertrandite, bavenite, euclase, occasionally behoite crystallize in cracks and leaching cavities, accompanied by segregations of late fluorite, adularia, biotite, analcime, corundophyllite, sericite, pyrite, chalcopyrite, sphalerite and other minerals.

© OCR - A. V. Belikovich, A. V. Galanin, O. M. Afonina, and I. I. Makarova Published according to the text: Belikovich A.V., Galanin A.V., Afonina O.M., Makarova I.I. Flora of specially protected territories of Chukotka. Vladivostok: BSI FEB RAN, 2006. 260 p.

Regional geological and water monuments of nature

Geological monument of nature "ANYUYSKY"

The monument is located in the eastern part of the Bilibinsky district, the area of ​​the Monni River (the basin of the Bolshoi Anyui River). The area is 10.5 thousand hectares. The monument is an extinct conical trachybasaltic stratovolcano of the Holocene age with a diameter of 480 m and its surroundings, the height of which is 90-120 meters. A fissure lava flow 56 km long is associated with it (Fig. 23). Monument of natural disasters. The last volcanic eruption, according to geological data (Ustiev, 1961), occurred about 500 years ago. The highest point of the volcano crater is 1100 m, the base of the crater is at an altitude of 600 m. Erupted lava flows stretch down the northern slope in a narrow strip, and then spread widely to the west for more than 30 km along the ancient valley. Directly from the south, Mount Vulkannaya adjoins the volcano - the highest elevation in a small massif composed of acidic crystalline rocks.

There is only one work on the vegetation cover of the monument (Petrovsky, Plieva, 1984). The area is distinguished by its forest-tundra character, since the territory of the protected area is located in the contact zone of larch sparse forests penetrating along the valleys of the right tributaries of the river. Big Anyui to the middle part of the Anyui Range, with mountain tundra dominating most of the range. The main types of ecosystems found here are as follows:

summit surfaces of mountains, low ridges and individual hills with patchy and patchy dryad tundras;

stony placers with open vegetation groups and lichen-moss tundras;

southern slopes of mountains with rubbly spotted and continuous dryad-forb tundras;

northern slopes of mountains with shrub and shrub-moss-lichen tundras;

cedar and dwarf thickets along mountain slopes with alder forests along runoff hollows;

slopes of narrow river valleys. Ustiev and its tributaries with larch woodlands;

complexes of herbaceous alder and willow forests around lakes formed as a result of springing by frozen lava flows of surface water runoff;

brook complexes of willow and shrub larch forests along streams and rivers;

floodplain terraces. Ustiev with shrubs, meadows and swamps;

river floodplain Ustiev with chozen, willow and pebble.

Notes: From a botanical point of view, it is most interesting to compare the composition of the flora in lava flows and in areas where there are no igneous rocks. Specific flora is confined to the substrates formed as a result of a volcanic eruption. These are 28 pioneer species of colonization of volcanic lavas and tuffs (13% of the total number of identified species). These are mainly mountain arctic and arctoalpine species, as well as several hypoarcto-mountainous species. In the lower parts of the cone, where significant accumulations of snow form in winter, Delphinium chamissonis, Papaver microcarpum, Saxifraga hyperborea are noted in a noticeable abundance. Hierochloe alpina, Luzula confusa, Saxifraga punctata are very common on lava flows, and Poa glauca, Dicentra peregrina, Ermania parryoides, Artemisia glomerata are constantly found on tuff screes along the slopes of the cone. Other pioneer species: Trisetum spicatum, Poa pseudoabbreviata, Festuca brachyphylla, Luzula confuse, Salix phlebophylla, Silene stenophylla, Minuartia rubella, Thalictrum alpinum, Cardamine bellidifolia, Draba lonchocarpa, Saxifraga funstonii, S. nivalis, Oxytropis czukotica, Diapensia obovata, Androsace ochotensis , Artemisia furcata, Crepis chrysantha, Dryopteris fragrans, Rhodiola atropurpurea. This composition of species can be considered random and due to the introduction of seeds from neighboring plots.

plant communities(Petrovsky, Plieva, 1984):

16% - open vegetation groups on scree slopes of the volcano (Diapensia obovata, Saxifraga funstonii, Androsace ochotensis);

27% - pioneer vegetation of lava flows (Hierochloe alpina, Luzula confusa, Saxifraga punctata);

5% - combinations of rubbly spotted and clump dryad, forb-dryad tundras (Dryas puntata, Carex rupestris, Potentilla uniflora, Minuartia rubella, Salix phlebophylla, Silene stenophylla, Anemone sibirica) on the top surfaces of mountains, low ridges, dry slopes;

1% - combinations of open vegetation groups and lichen-moss tundras (Woodsia ilvensis, Potentilla anachoretica, Potentilla elegans, Carex podocarpa, Lloydia serotina) on rocks and stony slopes;

14% - combinations of shrub-moss-lichen and sedge-forb tundras (Cassiope tetragona, Minuartia macrocarpa, Diapensia obovata, Ledum decumbens, Novosieversia glacialis, Parrya nudicaulis, Saxifraga nelsoniana, Carex lugens, Valeriana capitata, Saussurea tilesii) according to northern slopes and shrub-forb tundra (Vaccinium uliginosum, Empetrum subholarcticum, Arctous alpina, Dianthus repens, Dracocephalum palmatum, Arenaria capillaris) along the southern slopes;

9% - combinations of dwarf cedar thickets, larch subalpine sparse with dwarf elfin forests on mountain slopes and alder thickets with dwarf pine (Pinus pumila, Alnus fruticosa, Betula middendorffii, Lycopodium pungens, Vaccinium vitis-idaea, V. uliginosum subsp. microphyllum, Arctous alpina, Orthilia obtusata, Polygonum tripterocarpum) along damp runoff troughs on slopes;

15% - larch woodlands and sparse forests (Larix cajanderi, Betula exilis, Ledum decumbens, Pyrola grandiflora, Salix saxatilis, Pedicularis labradorica, Calamagrostis neglecta, Arctagrostis arundinacea) along the sides of the narrow valleys of the river protected from the winds. Ustiev and its tributaries;

3% - combinations of herbaceous alder and willow forests (Alnus fruticosa, Salix boganidensis, S. anadyrensis, S. pulchra) around lakes formed as a result of damming of surface water runoff by frozen lava flows;

1% - combinations of wet meadows, sedge and sphagnum bogs (Arctophila fulva, Rubus chamaemorus, Salix fuscescens) in thermokarst ditches and subsidence;

1% - combinations of shrubs, willows and meadows (Spiraea stevenii, Pentaphylloides fruticosa, Rosa acicularis, Carex melanocarpa) on dry areas of floodplain terraces;

3% - combinations of swampy shrubs, sedge and sedge-shrub-sphagnum bogs (Carex rotundata, C. stans, C. appendiculata, Eriophorum polystachion, E. russeolum, Chamaedaphne calyculata, Tofieldia pusilla) along the depressions of the floodplain terraces;

4% - brook complexes of willows and larch shrubs (Salix pulchra, S. krylovii, S. hastata, Ribes triste) along streams and upper reaches of rivers;

1% - floodplain complexes of willows, chozen forests and meadows along riverbed alluviums (Chosenia arbutifolia, Salix alaxensis, S. schwerinii, S. anadyrensis, Pulsatilla dahurica, Chamerion latifolium, Artemisia borealis) on the river. Ustiev.

Biodiversity: in the flora of protected areas there are 218 species of vascular plants (Petrovsky, Plieva, 1984).

Protected species: rare plant species in the territory of the protected area are not observed.

Geological monument of nature "KEKUR"

Plant communities of protected areas(Galanin A.V. Geobotanical descriptions (12) of the area of ​​the village of Apapelgino for 1974. Archive of the BSI FEB RAS, unpublished data):

70% - complexes of tuberous dwarf shrubs, willows, cassiopeia moss-lichen tundras (Betula exilis, Ledum decumbens, Salix pulchra, S. sphenophylla, S. reticulata, S. reptans, Carex lugens, Vaccinium vitis-idaea, Arctous alpina, Empetrum subholarcticum, Eriophorum vaginatum, Senecio atropurpureus, Petasites frigidus, Parrya nudicaulis, Luzula nivalis, Cassiope tetragona);

30% - complexes of tussocky sedge-cotton grass, sedge-shrub tundras (Betula exilis, Ledum decumbens, Salix fuscescens, Polygonum tripterocarpum, Carex lugens, C. stans, Vaccinium vitis-idaea, Eriophorum vaginatum, E. polystachion, Calamagrostis holmii, Arctagrostis latifolia , Valeriana capitata).

Biodiversity: according to expert data, more than 60 species of vascular plants grow on the territory of protected areas (see descriptions).

Geological monument of nature "ELGYGYTGYN LAKE"

Rice. 25. Geological monument of nature "Lake Elgygytgyn". The monument is located in the northern part of the Anadyr region along the border with the Chaun region at an altitude of about 500 m above sea level. sea, coordinates 67°29"32"N. 172 ° 04 "33" W. The area is 350 hectares. The lake basin has a regular rounded shape with a diameter of about 17 km. Its formation occurred in the latest stage geological history Anadyr Plateau, about 3 - 5 million years ago (Bely, 1993). The site itself includes the lake itself as a unique geological object (Fig. 25), the origin of which (meteorite crater or endogenous explosion) is the subject of discussion (Bely, 1982). The fauna of the vicinity of the lake is represented by species of large land mammals typical of Chukotka, including the population of bighorn sheep, listed in the Red Book of Russia (Vaskovskii et al., 1988; Zheleznov, 1994). Of the birds, a number of “Red Book” species have been noted here (Nature of the Lake Depression ..., 1993). The ichthyocenosis of the lake is extremely poor, but is unique in its endemism and relict character (Chereshnev and Skopets, 1993). Three species of charr live in the lake, including two endemic ones. On the shore of the lake there are archaeological sites (sites of ancient people). The maximum depth in the center of the lake is 169 m.

According to the latest research by scientists, the lake is of global importance. The proposed object was included in the order of the Government of the Russian Federation dated 23.04.94. No. 572-r "On the formation of new specially protected areas of the Russian Federation in 1994-2005" under the name of the Elgygytgynsky National Park. The feasibility study was developed by the Research Center "Chukotka" FEB RAS (Belikovich, Galanin, 1994).

The vegetation of the monument has been studied well (Kozhevnikov, 1978, 1985, 1993; Belikovich, 1988, 1989, 1990, 1994; Belikovich, Galanin, 1989, 1992).

Type of ecosystems of protected areas - typical hypoarctic tundras in the zone of southern hypoarctic tundras. The main ecosystems are associated with abiotic differences in the environment:

flat mountain tops and upland terraces with cryogenic relief and windblown clump and spotted tundras;

moderately steep solifluction slopes with sinter hillocks and characteristic banded shrub (most often dryad) tundras;

slightly sloping solifluction terraces, wide runoff hollows on the slopes, with peaty-humus substrate and complexes of meadows and tubercular shrub tundras;

gentle trails of slopes and saddles with close permafrost and marshy sedge and hummocky cottongrass tundras, fragments of moss swamps;

nival ecotopes in places of snowfields in slope bends, ledges of terraces, erosion troughs, floodplain terraces of streams, alluvial fans;

pebbles of the ancient valley of the river. Enmyvaam with sparse herb communities and silty channels;

floodplains of streams with fragments of willows and sparse grass meadows.

Notes: The lake has a cooling effect on the surrounding vegetation, in connection with which the participation of steppe groups and meadows in the vegetation cover is reduced. On the eastern shore of the lake, there is the “Pink Rocks” tract, which is an elongated rock mass composed of andesites interspersed with plagioclase and labradorite. Relic plant species Pulsatilla multifida subsp. nutalliana, Carex supina subsp. spaniocarpa. The only stepoid in the area was also found here - between steep rocks on a steep crumbling rubble area. In addition to the above species, Artemisia kruhseana, Poa glauca, Potentilla stipularis, P. nivea, P. arenosa, Carex rupestris, Antennaria monocephala, Trisetum molle, Dryas punctata, Selaginella sibirica, Saxifraga funstonii, Androsace septentrionalis, Festuca brachyphylla, Polemonium boreale, Myosotis asiatica, Arnica iljinii.

In the region of the lake Elgygytgyn, despite its continental position, has enhanced oceanic signs of vegetation, which proves the ratio of continental and oceanic elements of flora and vegetation (Kozhevnikov, 1979, p. 118). This is confirmed by other observations: finds in the surface layers of soil trunks of large willows, which are currently absent here, geomorphological changes over the past 100 years according to the descriptions of early researchers. The increase in the oceanic climate in the lake area and the corresponding change in the vegetation cover is due to the elevation of the area above sea level.

plant communities(Kozhevnikov, 1993, Belikovich, 1988; area after: Belikovich, Galanin, 1989):

15% - combinations of clump and spotted dryad-lichen, forb-dryad, cobresia tundras (Salix phlebophylla, Pedicularis lanata, Artemisia furcata, Potentilla elegans, Eritrichium aretioides, Minuartia arctica, Potentilla uniflora, Arenaria capillaris, Poa pseudoabbreviata, Cardamine bellidifoserpyllifolia , Kobresia myosuroides, Crepis nana) on horizontal rocky surfaces - flat mountain tops, upland terraces, tuff screes;

20% - combinations of spotted shrubby, dryad-forb, Cassiopeia moss-lichen tundras (Cassiope tetragona, Rhododendron parvifolium, Senecio resedifolus, Ermania parryoides, Silene stenophylla, Dryas octopophylla, Crepis nana, Potentilla elegans, Androsace ochotensis) of gentle and medium steep slopes ;

9% - combinations of meadows and tubercular shrub tundras (Artemisia arctica, Aconitum delphinipholium, Arctagrostis arundinacea, Carex podocarpa, Festuca altaica, Luzula multiflora, Senecio tundricola, Thalictrum alpinum, Veratrum oxysepalum) on slightly inclined solifluction terraces, wide runoff troughs on slopes, areas plumes with a humus substrate;

40% - combinations of sedge-cotton grass-shrub tussock tundra and sedge moss bogs (Eriophorum vaginatum, E. callitrix, E. polystachion, Pedicularis pennellii, P. albolabiata, Carex rotundata, C. lugens, Salix fuscescens, S. reticulata, Senecio atropurpureus , Ledum decuumbens, Andromeda polifolia, Vaccinium uliginosum, V. minus) along gentle trails of slopes, on saddles, upland terraces and the old lacustrine terrace of the lake;

1% - combinations of forb, dryad tundras, including stepoids (Potentilla stipularis, Artemisia kruhseana, Myosotis asiatica, Saxifraga eschscholtzii, Papaver lapponicum, Senecio jacuticus, Woodsia ilvensis, Dianthus repens) of rocky ledges along the sides of valleys and mountain slopes;

9% - combinations of nival cassiopeia-moss, willow and snowy sparse grass tundras (Salix polaris, Cassiope tetragona, Carex tripartita, Phippsia algida, Koenigia islandica, Saxifraga hyperborea, Eritrichium villosum, Primula tschuktschorum, Hierochloe pauciflora) in places of snowfields in slope bends, ledges terraces, erosional hollows, non-floodplain terraces of streams, alluvial cones;

1% - forb meadows (Arctagrostis latifolia, Carex misandra, C. atrofusca, Saxifraga cernua, Ranunculus affinis, Anemone sibirica, Polygonum viviparum, Valeriana capitata) on ground squirrels;

3% - combinations of hairy meadows, clumps of willows, moss sedge, grassy and wet silty sparse grass communities (Androsace ochotensis, Empetrum subholarcticum, Salix tschuktschorum, S. saxatilis, Pleuropogon sabinii, Polemonium boreale, Beckwithia chamissonis, Saussurea tilesii, Lagotis minor, Pedicularis hirsuta ) on the pebbles of the ancient valley of the river. Enmyvaam;

2% - combinations of fragments of willow forests and sparse grass meadows (Salix alaxensis, S. krylovii, Deschampsia borealis, Chamerion latifolium, Equisetum variegatum, Stellaria fischerana, Potentilla hyparctica, Eutrema edwardsii, Cardamine blaisdellii, Trollius membranostylus, Polemonium acutiflorum, Parnassia kotzebuei, Polemonium acutiflorum, Parnassia kotzebuei, Poa) along the floodplains of the streams.

Biodiversity: The flora of the region includes 249 species (Kozhevnikov, 1978; Belikovich, 1990).

Protected species: Over 100 species of the region are rare or found singly. Koeleria asiatica, Carex amblyorhyncha, C. holostoma, Tofieldia pusilla, Saxifraga setigera, Trollius chartosepalus, Corydalis arctica, Astragalus tugarinovii can be considered rare species. Festuca baffinensis, which is extremely sporadically found in Chukotka, is common here - around the lake it grows in places where andesitic tuffs come out, on dry rubble chicken tundra, grows luxuriantly near remnant rocks, on ground squirrels (Yurtsev et al., 1973). Most of the flora of the site is represented by species that took part in transcontinental migrations through Beringia in the Pleistocene. Endemes and species listed in the Red Book of the RSFSR are not registered in the area.

Water monument of nature "ACCHEN"

Rice. 26. Water monument of nature "Lake Achchen". It is located in the southern part of the Providensky district, on the coast of the Gulf of Anadyr, 50 km from the village of Nunlingran (Fig. 26). The area is 9 thousand hectares. The monument is a unique lake - a spawning place for valuable species of fish, including sockeye salmon, chinook salmon, pink salmon, loaches, vendace (by its size, fat content and fatness, the vendace of the lake is a unique form not found in any reservoir of Chukotka and Kolyma). Lake Achchen is a lagoon-type lake. It is a laced sea lagoon, separated from the sea by a sand and pebble bridge, desalinated by numerous small streams and rivers flowing into the lake. The greatest depth of the lake is 27 m.

In the southern part, the sea comes close to the lake. It is separated by a pebble spit 150 m wide at its narrowest point. This spit is low relative to the water level in the lake and the sea, and during the period of maximum water levels in the lake and strong storms on the narrowest section of the pebble spit, sea water surges, overflowing through the spit, fall into the lake . From the south, the lake is connected to the sea by a channel 1 km long.

The protected area is located in the subzone of the northern (typical) hypoarctic tundra. Main ecosystems: mountain slopes with patchy, patchy and full-cover tundras; runoff hollows with complexes of nival tundras and lawns; valleys of streams and small rivers with sparse grass meadows, willow forests, lawns and nival tundras; the lower parts of the slopes of the mountains with trains with tubercular and hummocky sedge-cotton grass tundras; a marine pebbly spit separating a lagoon-type lake from the Gulf of Anadyr, with complexes of halophytic sparse grass meadows and leimus meadows in a wide part.

Plant communities of protected areas(according to preliminary and archival data):

24% - combinations of sparse clump, clump and spotted forb, shrub tundra (Dryas punctata, Salix sphenophylla, Festuca brachyphylla, F. brevissima, Carex misandra, Minuartia biflora, M. arctica, Anemone sibirica, Cardamine bellidifolia, Saxifraga serpyllifolia, S. flagellaris subsp . setigera, Potentilla elegans) on the near-top parts of the slopes;

1% - steppe forb, dryad-forb and fescue-kobresia tundras (Dryas punctata, Festuca altaica, Kobresia simpliciuscula, Carex melanocarpa, Claytonia arctica, Arenaria capillaries, Silene acaulis, S. stenophylla, Erysimum pallasii, Ermania parryoides, Saxifraga funstonii) southern heated convex sections of slopes and terraces;

32% - combinations of whole-cover shrub, dryad, dryad-sedge moss-lichen tundras (Dryas punctata, Salix arctica, S. phlebophylla, Betula exilis, Vaccinium uliginosum, V. vitis-idaea, Arctous alpina, Carex scirpoidea, Luzula tundricola, Thalictrum alpinum , Parrya nudicaulis, Acomastylis glacialis, Arctous erythrocarpa, Oxygraphis glacialis) along the slopes of different exposures;

4% - combinations of nival forb, forb-sedge-moss and willow-moss tundras and lawns (Salix polaris, S. reticulata, S. phlebophylla, S. chamissonis, Carex podocarpa, Oxyria dygina, Koenigia islandica, Ranunculus nivalis, R. pygmaeus , R. sulphureus, Poa malacantha, P. paucispicula, Phippsia algida, Luzula unalashkensis, Dodecatheon frigidum) along erosion ravines, hollows, small streams, under ledges of upland terraces;

2% - combinations of sparse grass meadows, willows, lawns and nival willow tundras (Salix alaxensis, S. glauca, S. pulchra, S. nummularia, Spiraea stevenii, Allium shoenoprasum, Lloydia serotina, Leymus interior, Arctagrostis arundinacea, Festuca altaica, Pleuropogon sabinei , Veratrum oxysepalum, Rumex acetosa subsp. pseudoxyria, Polygonum tripterocarpum, Anemone richardsonii, Rubus arcticus, Lagotis minor) in the valleys of streams and small rivers;

31% - tuberculous shrub-forb moss-lichen tundras (Salix pulchra, S. saxatilis, S. reptans, Betula exilis, Carex lugens, Alopecurus alpinus, Arctagrostis latifolia, Eriophorum vaginatum, Tofieldia coccinea, T. pusilla, Polygonum ellipticum, Clalytonia acutifolia ) lower parts of mountain slopes and trails of slopes;

35% - combinations of tussock shrub-cotton grass-sedge tundras, marshy sedge-moss tundras and sedge bogs (Salix fuscescens, Eriophorum polystachion, E. medium, E. russeolum, E. triste, Pedicularis oederi, P. pennelii, Carex rariflora, C . rotundata, Ranunculus pallasii) along flat areas of terraces and trails of mountain slopes;

2% - combinations of moss forb and shrub tundras (Petasites frigidus, Phippsia algida, Empetrum subholarcticum, Salix rotundifolia, Carex glareosa, Salix ovalifolia, S. glauca, S. alaxensis) along the banks and old lacustrine pebbles;

2% - halophyte sparse grass and shiksha-leimus meadows (Arctopoa eminens, Leymus villosissimus, Empetrum subholarcticum, Deshampsia paramushirensis, Puccinellia phryganodes) on a pebbly spit;

2% - halophytic shiksha-grass-forb marsh tundras (Salix ovalifolia, Calamagrostis deschampsioides, Puccinellia angustata, Silene acaulis, Armeria arctica) in wide parts of the pebble spit.

Biodiversity: about 270 species of vascular plants have been identified in the area.

Protected species: On a lake Locations of a rare species of moss Leptopterigynandrum austro-alpinum are known in Achchen. It is a rocky and tundra moss with a disjunctive range, growing on rather wet surfaces of limestone rocks and on gravelly substrates in mountain tundras. A rare species of large-seeded drema Gastrolychnis macrosperma, club moss Lycopodium clavatum subsp. monostachyon, arctic reed grass Calamagrostis arctica, and Pleuropogon sabinii, rare for the Bering Sea coast (Yurtsev et al., 1975b). Also recorded are Maksimovich's reed Scirpus maximowiczii, found on wet spotted and small sedge tundras of mountain saddles, cobresia Kobresia sibirica, K. simpliciuscula, and the green grasshopper Coeloglossum viride from the fam. Orchids (Yurtsev et al., 1973a).

5 rare species of mosses were found in the protected areas: Encalypta vulgaris, Kiaeria starkei, Leptopterigynandrum austro-alpinum, Racomitrium afoninae, Seligeria polaris.

Water monument of nature "RAUCHUAGYTGYN"

Rice. 27. Water monument of nature "Lake Rauchuagytgyn". It is located in the southern part of the Chaunsky district, in the upper reaches of the Rauchua River, not far from the village of Baranikha (Fig. 27). Area 573 ha. The monument is a unique lake of moraine genesis with its surroundings. The terrain is sharply dissected, rocky. Classical glacial trough valleys, glacial moraine and hydroglacial formations are typical. The lake is located at an altitude of 593 m. The length of the lake is 4.3 km, the width is 1.8 km, the depth is 15-20 m. The lake is flowing. The flow of the Rauchua River is regulated. The lake area is characterized by an inversion of air temperature in winter (an increase in air temperature with altitude). The lake was formed as a result of the damming of the valley by moraine deposits. The confinement of the lake to the junction of the volcanogenic belt with mesozoids gives the area a colorful multi-colored hue. Wild deer, bighorn sheep, brown bear, wolverine, etc. live in the vicinity of the lake. The vegetation of the river basin. Rauchua was studied in detail by A.V. Galanin (1977, 1989, 2005), there are data on floristic finds (Yurtsev et al., 1973a). The protected area belongs to the Western Chukotka district of the Continental Chukotka subprovince of the Arctic floristic region, the subzone of the southern hypoarctic tundra (Yurtsev, 1973). The area is located 70 km southwest of the southern tip of the Chaun Bay and is characterized by a medium-dissected mountainous terrain. Separate mountain ranges exceed 1300 m above sea level and have alpine-type features. Most of the hills are 600–1100 m high with flat tops and strongly terraced slopes. The peaks of neighboring hills are connected with each other by saddles in chains and large massifs, which are interspersed with wide mountain ravines. Numerous streams and rivers usually dry up in the second half of summer.

The slopes of the hills quite sharply turn into extensive loamy plumes. In places where the slope - plume there are leveled areas - subslope terraces, which, despite good drainage, are intensively moistened due to the inflow of groundwater from the slope of the hill. On the plumes there are gravel ridges 2 to 10 m wide and up to 0.6 m high, oriented down the slope, and in some places, usually in the middle and lower parts, there are wide (up to 20–30 m) trough-shaped runoff hollows. Some of the highest peaks have remnants, near which a large amount of coarse clastic material is observed. On the steep slopes of the hills, rubble and stony screes are quite common. The area as a whole is dominated by acid sedimentary and igneous rocks: granitoids, sandstones and shales. Basic rocks are absent here. In the valley of the river flowing out of the lake, floodplain terraces are well expressed, turning into a floodplain with numerous swamps and lakes.

The main types of protected area ecosystems are as follows: peaks, near-top ridges and parts of steep southern slopes and upland terraces with clump and fragmentary gravel tundra; convex sections of mountain slopes of hills of southern exposure with steppe tundras; extensive upland terraces and slopes of northern exposure with whole-cover shrub moss-lichen tundras; slopes and upland terraces at an altitude of 700–900 m a.s.l. seas with patchy forb-shrub moss-lichen tundras; runoff hollows on slope plumes with tussocky sedge-cotton grass tundras in combination with low-growing willows; nival tundras and lawns along streams, places of snowfields, narrow erosive; above-floodplain terraces of the river and fragments of the lakeside terrace with dwarf birch, sedge-moss tundras, polygonal swamps with bulgunnyakhs; old pebbles of vast floodplain terraces of the river. Rauchua with dwarf shrubs, patchy and patchy forb-shrub tundras; floodplain complexes of sparse-grass meadows on pebbles and reed meadows on silted sand deposits in the floodplain of the river. Rauchua in the place where it flows out of the lake.

Notes: Not far from the protected area is the border between the basins of the Kolyma, Anadyr and rivers flowing into the Arctic Ocean. The vegetation cover of the lake area is the southern version of the subzone of the southern hyporactic tundra, which will be replaced by forest tundra literally in a couple of tens of kilometers (Petrovsky, Plieva, 1988, 2000). In this regard, many boreal species have been recorded in the flora of protected areas. These species are found mainly in swamps, willow forests, and partially in floodplain-above-floodplain ecotopes. In floodplains and on floodplain terraces of the river. Rauchua found fragments of reed meadows - full-fledged boreal meadows, located here at the northern limit of their distribution.

Plant communities of protected areas(Galanin, 1977):

19% - combinations of clump and fragmentary forb-dwarf shrub gravelly, clump and spotted forb-lichen and dryad-lichen tundras (Dryas punctata, Salix phlebophylla, S. tschuktschorum, Viccinium vitis-idaea, Crepis chrysantha, Silene stenophylla, Oxytropis czukotica, Artemisia furcata , Arnica frigida, Ermania parryoides, Selaginella sibirica, Polygonum laxmanii, Potentilla uniflora, Festuca brachyphylla, Arctous alpina, Hierochloe alpina, Anemone sibirica) on the tops and near-top parts of steep slopes, screes of southern and southwestern exposure and upland terraces;

3% - combinations of clump and fragmentary forb-dwarf shrub gravelly, forb-lichen steppe tundras (Dracocephalum palmatum, Dianthus repens, Erysimum pallasii, Festuca auriculata, Potentilla nivea, Dryas punctata, Minuartia rubella, Carex rupestris, C. obtusata, C. pediformis, Androsace bungeana, Silene repens, Thymus oxyodonthus, Potentilla arenosa, Draba cinerea) on convex mountain slopes of southern exposure hills;

15% - combinations of forb-shrub and willow moss-lichen tundras (Salix pulchra, S. tschuktschorum Arctagrostis latifolia, Carex lugens, Ledum decumbens, Vaccinium uliginosum, Betula exilis, Eriophorum vaginatum, E. brachyantherum, Gentiana glauca, Senecio frigidus, Pedicularis lapponica , P. oederi) extensive upland terraces and slopes of northern and northeastern exposure;

15% - combinations of spotted forb-shrub moss-lichen and lichen tundras (Betula exilis, Ledum decumbens, Salix sphenophylla, S. phlebophylla, Carex lugens, Pedicularis amoena, Anemone sibirica, Polygonum ellipticum, P. tripterocarpum, Androsace ochotensis, Vacsumcinium uligino, Cassiope tetragona, Poa alpigena, P. malacantha, Deschampsia brevifolia, Pedicularis adamsii, Gentiana algida, Saxifraga nivalis, S. foliolosa, Petasites glacialis, Saussurea tilesii, Oxygraphis glacialis) on slopes and upland terraces at an altitude of 700–900 m a.s.l. seas;

12% - combinations of raw forb-shrub eutrophic, willow-sedge-moss and forb-shrub moss tundras (Salix saxatilis, S. reticulata, Rhododendron parvifolium, Andromeda polipholia, Parrya nudicaulis, Claytonia acutifolia, Polygonum ellipticum, Luzulagotis nivalis, Lagotis minor, Carex lugens, C. misandra, C. algida, C. williamsii, Pedicularis oederi, Thalictrum alpinum, Saxifraga hirculus, S. hieracifolia, Chrysosplenium alternifolium, Melandrium apetalum, Thalictrum minus, Juncus biglumis, Corydalis arctica, Tofieldia coccinea) on subslope terraces and alluvial fans and along inter-ridge depressions of hill slope plumes;

18% - combinations of tussock sedge-cotton grass-shrub, sedge-cotton grass-forb tundra and low-growing willow forests (Eriophorum vaginatum, E. polystachion, E. russeolum, E. medium, Rubus chamaemorus, Carex lugens, C. stans, Calamagrostis holmii, Arctagrostis latifolia, Salix pulchra, S. fuscescens, S. saxatilis, S. krylovii, Betula exilis, Senecio atripurpureus, Ledum decumbens, Saxifraga hieracifolia) along runoff troughs on plumes of mountain slopes;

8% - combinations of nival tundra, lawns, brook forb shrubs and forb-moss shrub tundra (Salix pulchra, S. krylovii, Betula exilis, Ledum decumbens, Rosa acicularis, Saxifraga nelsoniana, S. cernua, Ranunculus grayi, Polygonum tripterocarpum, Veratrum oxysepalum , Polemonium boreale, Gentiana glauca, Anemone richardsonii, Rubus arcticus, Artemisia arctica, Whilhelmsia physodes, Hupperzia selago) along streams, nival niches and narrow erosional ravines (Oxyria digyna, Ranunculus pygmaeus, Carex podocarpa, C. tripartita, Diapensia obovata, Saxifraga oppositifolia, Artemisia arctica, Anemone richardsonii);

1% - xeromesophilic and mesophilic meadows on ground squirrels (Rosa acicularis, Hierochloe alpina, Festuca altaica, Arctagrostis latifolia, Calamagrostis lapponica, Artemisia arctica, Pulsatilla multifida, Drococephalum palmatum, Chamerion angustifolium, Veratrum oxysepalum, Valeriana capitata, Delincarpholia chamissonis) in the lower part of slopes and plumes;

1% - combinations of dwarf birch and sedge-moss tundras (Betula exilis, Salix pulchra, S. fuscescens, Empetrum subholarcticum, Vaccinium uliginosum, V. vitis-idaea, Polygonum tripterocarpum, Valeriana capitata, Petasites frigidus, Carex lugens, C. stans, Eriophorum vaginatum, Poa arctica, Rubus chamaemorus, Saxifraga hirculus, Chamaedaphne calyculata, Senecio atripurpureus) on terraces above the floodplain of small streams and fragments of a lakeside terrace;

4% - combinations of sedge-cotton grass shrub polygonal bogs with bulguniahs (Carex stans, Eriophorum polystachyon, E. russeolum, E. medium, Salix fuscescens, S. myrtilloides, Saxifraga cernua, Comarum palustre, Andromeda polifolia, Ledum decumbens, Oxycoccus microcarpus, Vaccinium uliginosum, Rubus chamaemorus, Hierochloe pauciflora, Carex chordorrhiza, C. rariflora, C. rotundata, Smilacina trifolia, Drosera rotundifolia, Pinguicula villosa) on the floodplain terrace of the river. Rauchua and lakeside terraces;

2% - dwarf shrub blueberry tundra on convex areas and patchy and patchy forb-shrub tundra on old pebbles (Vaccinium uliginosum, Betula exilis, Salix pulchra, Pentaphylloides fruticosa, Empetrum subholarcticum, Pulsatilla multifida, Luzula sibirica, Antennaria villifera) (Festuca altaica acicularis, Arnica iljinii, Hedysarum hedysaroides, Festuca brachyphylla, Salix phlebophylla, Crepis chrysantha, Androsace ochotensis, Silene repens, Thymus oxyodonthus, Potentilla nivea, P. stipularis) of the extensive floodplain terraces of the river. Rauchua;

2% - floodplain complexes of sparse grass meadows on pebbles and reed grass meadows on silty sand drifts (Calamagrostis purpurea, Festuca rubra, F. cryophila, Chamerion latifolium, Artemisia borealis, A. tilesii, Tanacetum boreale, Potentilla stipularis, Rumex graminifolius, Stellaria fischeriana, Leymus interior, Galium verum, Allium schoenoprasum, Helictotrichon dahuricum, Alopecurus glaucus) and fragments of floodplain willows (Salix krylovii, S. hastata, S. lanata, S. pulchra, S. alaxensis, Pentaphyloides fruticosa, Galium boreale, Equisetum arvense) p. Rauchua in the place where it flows out of the lake.

Biodiversity: About 320 species have been recorded in the region (Yurtsev et al., 1973a; Galanin, 1977).

Protected species: Many rare boreal species are found in the area, for example, the foxtail equal to Alopecurus aequalis, the Siberian juniper Juniperus sibirica, the adnexal sedge Carex appendiculata and the nosed C. rostrata (Yurtsev et al., 1973). In eutrophic bogs, there is a boreal relic of the three-leaved smilacina Smilacina trifolia, on old pebbles of the Dahurian oatmeal Helictotrichon dahuricum, and in the gravel tundra on mountain tops, the grapevines Botrychium lunaria, B. boreale grow extremely rarely. The yellow wormwood Artemisia flava, a rare species found only in the east of Chukotka, was found here (Yurtsev et al., 1973a). Other rare species include Carex holostoma and C. irrigua sedges.