Where was the mine on the Bazikha River. Excursion to the area of the river Bazaikha. When is the best time to fly. Chip flights

28.10.2019

Along the river Bazaikhe

Due to the specifics of the Eastern region, we will first consider it as a whole, and then lay the most interesting trails along it. And we will begin our acquaintance with the Torgashinsky Range and the Bazaikha River, with the tributaries of the Berezovka River, originating in the Torgashinsky Range. The Bazaikha River begins in the Mansky district of the region near the village of Novoalekseevka. It flows in a general direction to the northwest, winding strongly between the mountains that form the sides of its valley. River loops of this type are called meanders in geography, after the Meandros River in Asia Minor (now the Great Menderes River in Turkey), which is characteristic of such bends. Bazaikh meanders have been preserved since ancient times, when there was almost a plain here. Gradually, over millions of years, the whole area was slowly rising, and the river had time to wash out its bed in it, preserving the flat bends. Meanders of Bazaikha, as well as Esaulovka and Many, are their good sights.

From the village of Erlykovka on the road Maganskoye - Beret to the pioneer camp "Swallow", which is already within the boundaries of Krasnoyarsk, there are no settlements along the river. Only a few cordon houses of the Stolby reserve stand within the protected area. From the mouth of the Bolshoi Inzhul to Kaltat, the northern border of the Stolbov passes along Bazaikha, and along the entire course of this section, Bazaikha enters the protected zone of the reserve. The strip - Bazaikha from Erlykovka to the mouth, and nearby the Bazaikha forests covering the Torgashinsky Range and the mountains near Magansk - stretched for fifty to sixty kilometers, reaching a width of ten to fifteen kilometers. The northern border of this strip is Krasnoyarsk, the eastern one is the railway. Mountains rise along the axial line of the strip, and many peaks have marks of more than six hundred meters above sea level, and the highest mountain in this area - Chernaya Sopka, or Karatag, reaches almost seven hundred meters. To match her and her southern neighbor - Mount Kamala.

The mountains are covered mainly with coniferous forests, in some places there are birches along old clearings, along streams - spruce and fir forests. The Torgashinsky Range and the Bazaikha River (its meadows and floodplain areas) have a remarkable flora: here there are plants that are not typical for this taiga zone, plants that seem to have come from a higher mountain zone: edelweiss, mountain poppies, Kuril tea, watersheds, some orchids and lilies. And there are plants characteristic of the West Siberian Plain - spring adonis, evening flowers and others, there are plants of the steppes, especially along the southern, sun-drenched slopes of the Torgashinsky Range above Bazaikha. Of course, you can not tear these plants left here from other geological eras. Such plants are called relict.

The forester's house on Bazaikha near the glade of rallies

For the first acquaintance with the Bazaikhsko-Torgashinsky site, we will go by boat along the Bazaikhe River during the spring flood of waters, we will try to discern the Bazaikhsky bends and the Bazaikhsky urmans. We could make the same trip on foot in August-September, when Bazaikha becomes shallow and here and there you can ford along it, bypassing the river clamps.

From the Maganskaya platform we will get by bus to the small village of Erlykovka and from there we will set sail on a comfortable tourist boat. It can be PSN-6, PSN-10, kayak, small raft. If we go along the river, without mooring to the shore, go by self-rafting, then the whole journey will take us twelve to fourteen hours.

Bazaiha at Near Camels

At Yerlykovka, a bridge crosses Bazaikha. Here is the road to Manu, to the village of Beret. This is the bridge we start from. On the left bank of the river lies a fairly large meadow. Below the bridge, the river becomes narrow, the sides of the valley rise above the river by two hundred - two hundred and fifty meters. After a kilometer and a half - a sharp left turn - one of the famous Bazaikha bends begins. The river goes around the hill, flows as if in the opposite direction and again turn - right. Soon after the turn on the right, a gentle log with mowing meadows appears. Here, at a time when wood was flowing along Bazaikha, there was a dam that helped deliver wood to its destination. This log on the right is called Gentle (and also - Duryndin log, or Ilkin key). You can come here from Magansk in a little over an hour. Most often from here, from the mouth of this log, Bazakhi travels begin.

There are paths along the banks of Bazaikha, and in the summer we will still use them. There are trails, as a rule, even on both banks of the river - the remains of the trails of timber rafters. The trails go not only near the water, they sometimes climb the coastal steeps.

Shortly after the Gentle log on the right we will see high banks with rocks along their tops - these are Far Camels, and immediately after turning to the right on the left bank a log is again visible - the Veseliy stream. From it to the mouth of the Big Inzhul, from where the Stolby reserve begins and where the first cordon of the reserve stands, the river flows straight, giving space to narrow meadows on the left.

It must be said that in the straight sections of the river valley, Bazaikha is quite radiant, therefore, when rafting on a boat, there is a danger of jumping out from behind a turn right onto a tree that has fallen into the water. So you have to go by boat according to the rules of an unfamiliar river: sticking to the short bank in the loops of the river, crossing the current on the riffles to the short bank. This reduces the speed of the alloy, but increases safety. River loops begin again from Inzhul, the mountains near the river seem to become smaller, recede to the sides, but the forests still surround the river. When you swim quietly alone, not in a group, you often see a waterfowl, water-loving birds: ducks, waders, kingfisher, and in summer, an eagle-fisherman - an osprey.

Sometimes there is such a clean, park-like section of the forest along the shore that you want to get off the boat and take a walk along it. Left turn, right turn, left again - a small straight section, and we come to the Yakhontova glade, to the mouth of the Yakhontov log.

If you wander through the forest in the mountains near the Yakhontov log, you can find an old road, in the rut of which pine trees have grown in half the girth of the arms, half a hundred to a hundred years old such a tree. It turns out that there used to be some kind of economic life here: mowing, forest preparation, fishing, tar was driven, tar. When it was? Who will tell now?

Behind the Yakhontova Polyana, a long bend of the river begins, at the base of the loop the river is divided by a very narrow mountain spur, crowned at the top with bizarre rocks - the remnants of the summit denudation. These are Near Camels, there is a path to them from the city. The townspeople used to often go to the Camels to relax, swim, fish, admire the rocks. As a rule, they went from overnight - from Friday to Sunday evening.

Bazaikha below Erlykovka

Several trails leave from Yakhontova Polyana: along the Yakhontovoy Log to Magansk, along the Dry Log to the Petryashino stop and to Zykovo, past the high mountains of Kamala and Chernaya Sopka. And again, an interesting fact - once there, along the eastern slopes of Kamala and Chernaya Sopka, bypassing the river valleys, there was a wheeled road to the city, from which only old traces remained.

And the third path - it crosses the river loop in a narrow place, goes to another slope of the spur and goes along the Uchasvenny log to the Sredny log, to the northern slopes of the Torgashinsky ridge, to the village of Kuznetsovo, to Krasnoyarsk Cheryomushki.

A strange feeling almost always overtakes me in these places on Bazaikh. I know that not far from here, behind these mountains, our city of millions of people is noisy, and here - like centuries ago - primitive silence, only the river rustles, the birds sing. The southern slopes of the right bank are filled with the sun, and it is warm from them, like from a stove. It smells of fir, the kingfisher catches fish, orange flames blaze on the frying lawn, along the hidden watercourse a strip of blue mountain catchments blooms, aliens from the high Sayan.

The hourly log has several surviving names, among them are Uskovin, Krestovy, Khairyuzovy, as if reflecting some toponymic layers of time in these places of tourist loneliness. However, on May weekends, in early June, whole fleets of Krasnoyarsk water tourists pass here, up to a hundred tourists in two days, up to five thousand a month. In winter and closer to spring, there are only occasionally chains of skiers from Magansk to Krasnoyarsk, or even only two or three people. How quiet it is in winter!

Behind the Uchasenny Log, on the left, near the Medvezhka River, there is a cordon of the Stolby Reserve. And on the right, a rare river terrace on Bazaikha with unexpected light forest - old fellings, after which for some reason the forest did not want to grow. This terrace is called Veranda. Behind it, mountains again rise above the river, cut by rare ravines-logs - Malaya Vaila and below - Big Vaila. Dry slopes, overgrown with dry-loving steppe grasses, bluish in appearance, are also a foreign inclusion in the flora of the taiga.

On the left is the mountain-taiga massif of the highest mountain in the vicinity of Krasnoyarsk - Abatak, the top of which goes into the sky at a mark of eight hundred meters. It is located in protected areas with a strict regime, where the path is closed for tourists.

At the end of the straight stretch, which began from the mouth of Bolshaya Vaila, the river enters the technically most difficult section of the rafting - the Abatak threshold near the rocky pressure of the right bank. This is a typical rapid on a river, with stones in the channel, with a clamp on a turn, with a large shaft along the core of the current, while some of the empty shafts carry a capsizing moment. The length of the nut is about two hundred meters, of which the most dangerous are seventy to one hundred meters. Inspection before passing can be done both on the left and on the right bank of the river, while the right bank is rocky and high, and the left one is gentle and low. With some skill in passing such rapids-shiver, with knowledge of your boat and its driving characteristics, with a well-trained crew, the threshold is nothing dangerous.

Bazaikh "Alps"

In previous years, Krasnoyarsk water tourists held their first season kayak competitions on whitewater here. The camp was usually located on the right bank below the threshold on the terrace of the river.

At the head of the rapid, the river enters a narrowness, making a turn to the left almost at a right angle, and at the end of the rapid, it again changes the direction of the flow - to the right. After the threshold - a direct current to the Davydov log, from which a small stream flows. The river is quite calm, but shallow, at low water there is a knee-deep ford.

And again, a tear downstream on the banks of Bazaikha is a dense dark coniferous forest, and on the right is the dry slopes of the Torgashinsky Range of southern orientation, plant communities on them are also characteristic not of the taiga, but of the steppes of Khakassia. In early spring - coltsfoot, in summer - thyme, veronica, carnations. Behind the cape, its left tributary, the Namurt River, flows into Bazaikha. Behind Namurt, the Bazaikha valley expands somewhat, wide meadows appear with spruce groves on them, galleries along the river - willow, alder, bird cherry thickets in a narrow strip along the water. Here, in the widening of the Bazakhi valley, there are even oxbow lakes.

The river in the section from Namurt to Synzhul makes many meander loops, which look especially beautiful from the steep right bank.

Below the mouth of the Namurt, in the Bazaikhi valley, there is a beautiful, memorable rocky remnant with a grotto facing the river. And on the right you can see the Barn Log with mighty alluvial fans overgrown with grass, pine and rare birches.

At the mouth of the Synzhul, at the cordon of the reserve, clearly visible from the river, Bazaikha again enters the narrowness, its banks converge again, but it still winds, although its current here is free, fast, unhindered.

To the left, dark coniferous forests are again on the slopes of the mountains, and to the right ... On the right, we come to an interesting section of the river, to weathered ancient rocks, which, like statues, stand above the slopes of the valley. Look at them from the river. You should definitely go there on foot and see it all up close.

We come to the mouth of a small stream that flows in from the right, having washed out for thousands of years a huge log, branched in its top part. Both the brook and the log are called Bolgash, there is another name - "the log of the village of the Marble Quarry." Before the war and after it, not far from here, on the left bank of Bazaikha, within the boundaries of the present reserve, marble tiles and marble chips were mined for construction needs. The quarry was closed only because of the substandard qualities of marble, and not at all because it was in the reserve. The settlement where the workers of the marble quarry lived was located in the Bolgash log. When the quarry finished its work, the village also died out. However, some residents did not leave their homes, and the houses of the village are still standing.

At the mouth of the Bolgash, the first bridge across the Bazaikha, on low-lying sports courts in not very large water, passes under the left bank of the river.

Here, to the mouth of the Bolgash, there are many trails from the Torgashinsky Range, here is the node of the tourist network of weekend hikes along the Torgashinsky site. This is discussed ahead.

From the mouth of the Bolgash again a straight and clean section. Here the river valley expands somewhat, on the left and on the right there are narrow terraces with meadows, birches, shrubs: bird cherry, viburnum, willows; pine is also found in separate specimens. Ahead is one of the Pillars of the reserve - Kovrizhki. The pillar is real, manhole, but rarely visited, although it is located near the road itself.

From Kovrizhek the river turns to the right, leaving behind a large beautiful meadow with groves of birches, individual pines, with meadow flowers. This is a glade of rallies and competitions of Krasnoyarsk tourists. Gatherings of tourists of the RSFSR are also held here. Almost every year Bazaikha hosts the first slalom kayaking competition of the season.

On the left bank of the river opposite the glade of rallies - a wall of rocks, between the rocks and the river - the road to the village of Bolgash, to the cordon on the river Synzhul. There was a heavy concrete bridge at the end of the rally clearing. A few years ago it was demolished by an ice drift, and concrete blocks are still in the water. They are a source of danger for small craft. Behind the broken bridge is a shiverka, a shallow place, immediately behind it is a new bridge, high and safe, and next to the bridge on the right bank is the forester's house. There is an unnamed log near the forester's house in the massif of the Torgashinsky Range, and in it the path, on a low saddle, diverging into three sides: to the left steeply upwards - to the road along the high Bazaikha spur of the Torgashinsky Range, the path goes straight on a gentle ascent to the non-torque road to the pass in the Torgashinsky Range at the top of the Blooming log, and the third path descends from the saddle along a small log into the valley of the Bolgash stream and goes there above the houses of the village. These trails will be useful for hiking along the Torgashinsky Range.

Below the bridge begins the territory occupied by pioneer camps. They are located on the left bank, and on the right - a high slope of the ridge with steep ravines. Below the left tributary of the Bazaikha - the Kaltat River - rocky outcrops - limestones - are visible along the ridge. Kaltat flows from the Stolbov Highlands, its network of streams permeates all the Stolbs: Aesthetic and Wild regions, Kaltats stones.

From the mouth of the Kaltat to the Bazaikha there is a fast swaying current. A terrace begins on the right, on it is the pioneer camp "Grenada" of the Krasmash plant, and in front of the camp there is a bridge. Tourist boats pass easily under the bridge. It happens that the bridge is destroyed by spring waters. In general, where there are bridges on a small river, there are surprises. There is again a bridge behind the pioneer camp, but this is already a stable road bridge, and for rafting it does not present any difficulties in any water.

Below the bridge, the river in its course cuts through river floodplains, on which willows, birches, viburnum, turf, shrub layer grow densely. And after a kilometer from the bridge, it again approaches the root bank. On the right, a red rock rises above the river - Cape Goat. At Cape Goat and below it, coastal booms have been preserved, a dam near the coast, the current beats into it. Immediately below this section, there is a right turn and behind it is a bridge. The bridge stands low above the water and is impassable in high water. For kayaks and PSN. The current here is very strong, and the danger of falling under the bridge is very great.

From this bridge to the mouth of the river five or six kilometers. The river here, as it were, becomes smaller, becomes, as it were, less watery, dries up. Here, within the city, within the boundaries of summer cottages, the river is very cluttered.

In the narrowness, at the rocks of the right bank, along the middle water, you can finish the journey along Bazaikha. On high water, the rafting can be continued to the Krasnoyarsk Divnogorsk auto bridge.

We passed along one of the borders of the Bazaikha travel region. It takes two days for such a trip, and if you don’t rush and stop in some places for an hour and a half, then it’s better to leave on Friday.

Brook Bolgash

Bazaikha, Mana, Mansky and Bazaikha coasts, rocks are extremely interesting. They are located at the junction of physical and geographical countries, at the junction of different geographical formations. Everything is mixed up here: rocks, plant communities, the world of birds and even the weather. Bazaikha, its valley, its logs are good for spring-winter ski trips. In the wind-sheltered valley of Bazaikhi, on some days of the end of winter it is so warm that we used to ski across it without shirts, as in a ski resort.

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According to Bazaikha On the scale of tourist complexity, the Bazaikha river is half a point more difficult than the Mana from Bereti to the mouth. On Bazaikha there is a threshold, perhaps of the second or third category of difficulty, depending on the water level in the river. This circumstance complicates the campaign along Bazaikha. In the chapter

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Nearest hotels (hotels, hostels, apartments, guest houses)

View all hotels in the area on the map

Shown above are the five nearest hotels. Among them there are both ordinary hotels and hotels with several stars, as well as cheap accommodation - hostels, apartments and guest houses. These are usually private mini-hotels of economy class. The hostel is a modern hostel. An apartment is a private apartment with daily rent, and a guest house is a large private house, where the owners themselves usually live and rent rooms for guests. You can rent a guest house with an all-inclusive service, a sauna and other attributes of a good rest. Check with the owners here.

Usually hotels are located closer to the city center, including inexpensive ones, near the metro or train station. But if this is a resort area, then the best mini-hotels, on the contrary, are located away from the center - on the coast of the sea or river.

Nearest airports

When is the best time to fly. Chip flights.

You can choose one of the nearest airports and buy a plane ticket without leaving your seat. The search for the cheapest flights takes place online and you are shown the best deals, including direct flights. As a rule, these are electronic tickets for a promotion or discount from many airlines. Having chosen a suitable date and price, click on it and you will be taken to the official website of the company, where you can book and buy the necessary ticket.

Nearest bus stations, railway stations, bus stops.

Name	Type of	Transport	Distance	Schedule
Maganskaya	stopping point	train	12 km.	Schedule
Berezovka	stopping point	train	12 km.	Schedule
Lugovaya	stopping point	train	13 km.	Schedule
Shushun	stopping point	train	14 km.	Schedule
Camas	stopping point	train	14 km.

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From Wikipedia, the free encyclopedia

K: Rivers in alphabetical order K: Water bodies in alphabetical order K: Rivers up to 500 km in length K: River card: fill in: Coordinates of the source of the river over a hundred km Bazaikha (river) Bazaikha (river) K: River card: correct: The height of the source

Description of the river

Average annual water consumption - - 5.0 m³/s. The largest tributaries are Namurt, Kaltat, Dolgin, Zhistyk and Korbik.

On the bank of the river, at the confluence with the Yenisei, in 1640 the village "Bazaikha" was founded. The village was adjacent to a high mountain ledge, which was called Gorodishche, or Mount Divan. In the 17th century, on the flat top of Mount Divan, there was a Tatar fortress, which the Russians called "Snake Settlement".

In the 19th century, the inhabitants of Krasnoyarsk built their dachas on the banks of the river.

In 1931, in the area of the river mouth in the village of Bazaikha, the construction of a woodworking plant began, after which the village was included in the boundaries of Krasnoyarsk.

On the left bank of the Bazaikha, near the Bolgashov log, on the territory of the Stolby reserve, a marble quarry worked.

Tourism

The river is suitable for tourist rafting during the spring flood. The tourist route of the second category of complexity started from the village of Erlykovka. At the threshold of Abatak, competitions of kayakers were held.

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Literature

Velichko M.F. Small trips around the big city. - Krasnoyarsk: Prince. publishing house, 1989. ISBN 5-7479-0148-6

Notes

Bazaikha

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Characteristic

Length

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Water consumption

Source

- Location

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- Height

- Coordinates

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mouth

- Location

- Height

- Coordinates

/ / 55.97944; 92.78306(Bazaikha, mouth)Coordinates :

river slope

water system

Russia

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Country

Russia 22x20px Russia

Region

Area

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Water Register of Russia

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Pool code

GI code

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Volume GI

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Description of the river

Average annual water consumption - - 5.0 m³/s. The largest tributaries are Namurt, Kaltat, Dolgin, Zhistyk and Korbik.

In the 19th century, the inhabitants of Krasnoyarsk built their dachas on the banks of the river.

In 1931, in the area of the river mouth in the village of Bazaikha, the construction of a woodworking plant began, after which the village was included in the boundaries of Krasnoyarsk.

On the left bank of the Bazaikha, near the Bolgashov log, on the territory of the Stolby reserve, a marble quarry worked.

Tourism

Write a review on the article "Bazaikha (river)"

Literature

Velichko M.F. Small trips around the big city. - Krasnoyarsk: Prince. publishing house, 1989. ISBN 5-7479-0148-6

Notes



tributaries (from 100 km)	Big Yenisei Small Yenisei Elegest Khemchik Us Kantegir Oya Abakan Tuba Syda Kill Sisim Derbin Mana Bazaikha· Kacha · Yesaulovka · Kan · Buzim · Shilka · Yagodkina · Angara · Kem · Big Pit · Kiya · Buggy-eyed · Cleanroom · Yew · Kas · Galaktionykha · Sym · Vorogovka · Dubches · Podkamennaya Tunguska · Bolshaya Varlamovka · Bakhta · Sarchikha · Upper Imbak ·
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An excerpt characterizing Bazaikha (river)

“But why didn’t I need to “cleanse” anything? I was surprised. - Anna is still a child, she does not have too much worldly "dirt", does she?
– She will have to absorb too much into herself, comprehend the whole infinity ... And you will never return there. You don't need to forget anything "old" Isidora... I'm sorry.
“So I will never see my daughter again…?” I asked in a whisper.
- You'll see. I will help you. And now do you want to say goodbye to the Magi, Isidora? This is your only opportunity, don't miss it.
Well, of course, I wanted to see them, the Lords of this Wise World! My father told me so much about them, and I myself dreamed for so long! Only I could not imagine then how sad our meeting would be for me ...
Sever raised his palms and the rock, shimmering, disappeared. We found ourselves in a very high, round hall, which at the same time seemed either a forest, or a meadow, or a fairy-tale castle, or simply “nothing” ... No matter how hard I tried, I could not see its walls, nor what was happening around. The air flickered and shimmered with thousands of brilliant "drops" similar to human tears... Having overcome the excitement, I breathed in... The "rainy" air was amazingly fresh, clean and light! From it, spilling life-giving force, the thinnest living threads of "golden" heat ran all over the body. The feeling was wonderful!
“Come in, Isidora, the Fathers are waiting for you,” Severus whispered.
I stepped further - the quivering air “parted” ... The Magi stood right in front of me ...
- I came to say goodbye, prophetic. Peace be with you…” I said softly, not knowing how I should greet them.
Never in my life have I felt such a complete, all-encompassing, Great POWER!.. They did not move, but it seemed that the whole hall was swaying with warm waves of some kind of unprecedented power for me... It was real LIFE!!! I didn't know what other words to call it. I was shocked!.. I wanted to embrace it with myself!.. Absorb it into myself... Or just fall to my knees!.. Feelings overwhelmed me with a stunning avalanche, hot tears flowed down my cheeks...
- Hello, Isidora. one of them sounded warm. – We pity you. You are the daughter of the Magus, you will share his path... The Force will not leave you. Go with FAITH, my dear...
My soul aspired to them with the cry of a dying bird!.. My wounded heart rushed to them, breaking against an evil fate... But I knew that it was too late - they slinged me... and pitied me. Never before have I "heard" how deep the meaning of these marvelous words is. And now the joy of their marvelous, new sounding surged, filling me, not letting me breathe from the feelings that overwhelmed my wounded soul...
In these words there lived both a quiet, bright sadness, and a sharp pain of loss, the beauty of the life that I had to live, and a huge wave of Love, coming from somewhere far away and, merging with the Earth, flooding my soul and body ... Life swept by in a whirlwind , catching every "edge" of my nature, leaving no cell that would not be touched by the warmth of love. I was afraid that I would not be able to leave ... And, probably because of the same fear, I immediately woke up from a wonderful “farewell”, seeing next to me amazing people in their inner strength and beauty. Around me stood tall old men and young men dressed in dazzling white robes that looked like long tunics. Some of them were girdled with red, and for two it was a patterned wide "belt" embroidered with gold and silver.

In the area of the city of Krasnoyarsk, sedimentary rocks are widely developed - stratified formations of diverse composition and genesis and a wide age range - from Riphean to Quaternary.

Upper Riphean erathema (R3)

Upper Riphean deposits (430-600 Ma) are developed in the basins of the Mana and Bazaikha rivers. According to lithological features, three formations are distinguished in the section: Urmanskaya, Manskaya, and Bakhtinskaya. Contacts with older deposits are everywhere tectonic; the relationship between the retinues in its composition is consonant.

The Urman Formation (R3ur) is composed of grayish-green, dark gray quartz-chlorite-sericite, epidote-chlorite, actinolite, carbonaceous-siliceous, siliceous, chlorite-quartz-calcareous and other shales, metasandstones with interlayers of marmorized limestones, rarely dolomites. The rocks are often sulfidized and collected in small isoclinal folds. Thickness over 200 m.

The Manskaya suite (R3mn) is composed of dark gray and black crystalline limestones, platy, sometimes lumpy, with interlayers of siliceous and phyllite-like clay shales (up to 12 m thick), less often metasandstones. Thickness over 600 m.

In the Krasnoyarsk region, the rocks of the Urman and Manskaya suites are developed to a limited extent, in small tectonic wedges in the area of the lower reaches of the river. Bazaikha. The limestones of the Manskaya suite in contact with the Stolbovsky massif are marbled.

The Bakhtin Formation (R3bh) is distributed in the vicinity of the city of Krasnoyarsk limitedly in the southern and southwestern parts of the area (in the region of the northern contact of the Stolbovsky massif near the observation deck of the Stolby nature reserve above the Bobrov Log). Here it is developed exclusively in tectonic wedges, and the rocks composing it are hornfelsed under the influence of the Stolbovskaya intrusion. In adjacent territories, the Bakhtin Formation conformably overlies the Manskaya Formation.

The Bakhtinskaya Formation is composed mainly of metabasalts. In the lower part of the suite, among the effusive rocks, there are interbeds of lithoclastic and crystal-clastic tuffs of the basic composition, chlorite-sericite shales and black siliceous thin-platy shales, less often - tuff-conglomerates.

The rocks of the Bakhtinskaya Formation are characterized by green, greenish-gray or dark green color, they are often sheared and greenstone changes are intensely manifested in them. Primary igneous minerals are usually almost completely replaced by epidote, chlorite, sericite, and carbonates. In the stratotype area opposite the village of Bakhta and on the right bank of the Mana River, the formation is represented in the lower part by basalts, lava breccias of basalts, andesite-basalts and their tuffs with rare interlayers of marmorized limestones, dolomites and siliceous shales.

The thickness of the suite reaches 2000 m.

Vendian system (V)

The Tyubilskaya Formation (Vtb) is widespread in the area. Its deposits are mapped both on the right and left sides of the Yenisei River. On the left bank of the Yenisei River (in the vicinity of the village of Udachny and below the mouth of the Sobakin River), the rocks of the suite form an extended latitudinal band and are folded into complex folds.

Artificial outcrop of sandstones of the Tyubilskaya suite near the road near the village of Udachny. Stop South

Calcite veinlets in sandstones

Greenish-gray color of sandstone on a fresh chip

On the right bank of the Yenisei, they are involved in the construction of the Bolshesliznevskaya syncline. Separate fields are known along the Bazaikha River, on the left bank of which the rocks of the suite are hornfelsed under the influence of the Stolbovsky massif.

Kalta fold. Right bank of the Yenisei, not far from the mouth of the Kaltat River

The suite is composed of polymictic, micaceous, calcareous sandstones, siltstones, shales, gravelstones, and black limestones. The color of terrigenous rocks is dark gray, dirty green, or greenish brown. The texture is massive or layered. The bedding is parallel and wavy. There are wave-cut signs of ripples and traces of raindrops. Sericite is often developed along the bedding planes. Limestones are dark gray, layered, bituminous, often clayey. In general, the formation is characterized by a finely rhythmic structure of the flysch type.

Boudinage structure

The rocks of the suite are often substantially sheared. So, in a large artificial outcrop on the right bank of the river. Bazaikha (near its mouth) there are intense disjunctive dislocations of the suite deposits and fracturing in several directions. The total thickness of the unit is 950 - 1100 m.

The Tyubilskaya Formation is conformably overlain by the Ovsyankovskaya Formation. The contacts with the underlying deposits are tectonic.

Small skeletal remains of a tubular shape were found in the upper part of the suite. Similar fossils are found with the Vendian. The age of the formation is assumed to be Late Vendian (570-555 Ma).

Ovsyankovskaya Formation (Vov). The rocks of the retinue create a vast field in the vicinity of the villages of Ovsyanka and Sliznevo. They are common in the area of the village of Borovoe, as well as in the interfluve of the Bolshaya Sliznevaya River - the Roeva Stream, where they form the nuclear part of the Bolshesliznevskaya syncline.

The Ovsyankovskaya Formation is composed of dolomites, dolomitic limestones, calcareous dolomites, dolomitic breccias, rarely limestones, quartzites are found in some areas.

Kurumnik near Ovsyanka village

Dolomitic rocks are diverse in color and texture. All shades of gray are observed (from light gray to dark gray), sometimes the rocks are yellowish. The textures are massive and layered. A notable feature of the dolomites are abundant microphytoliths, especially oncolites and blistered catagraphies. During weathering, the internal parts of the nodules of microphytoliths are leached, and empty shells are preserved from them, due to which the rock acquires a porous appearance.

The formations are folded into complex folds and cut through by numerous disjunctives in parts of the rock; they are often strongly recrystallized or silicified. The thickness of the suite is estimated at 1000 - 1100 m.

The contacts of the formation with the underlying sediments are mainly tectonic, however, in the interfluve of the Bolshaya Sliznevaya River and the Roeva Creek in the core part of the Bolshesliznevskaya syncline, its consistent occurrence on the Tyubilskaya Formation is established.

Paleozoic erathema (PZ)

Cambrian system (€)

Lower section (€1)

In the vicinity of Krasnoyarsk, the Ungut and Torgashinsky formations are attributed to the lower Cambrian.

Ungut Formation (€1un). Selected by I.P. Zhuiko and V.V. Bezzubtsev in 1959. The stratotype is located near the village of Bolshoi Ungut.

Due to the fact that the composition of individual parts of the Ungut Formation is different and its variability along strike is noted, the types of the section of the formation are distinguished, for which its local names are accepted.

The Karaulinsky type of section is represented by carbonate deposits developed along the Karaulnaya River, as well as above and below its mouth along the left side of the Yenisei River. In addition to natural outcrops, the rocks of the formation are exposed here by a quarry located on the left side of the Karaulnaya River near its confluence with the Yenisei River. This type of section has a uniform limestone composition, with interlayers of dolomites in the lower part of the section and a characteristic horizon of oncolithic limestones with “floating pebbles” in the middle. Thickness is 800 - 920 m. Overlying deposits are present only at one point - along the Karaulnaya River - and are represented by a sequence of limestone conglomerates of problematic age (Cambrian?).

artificial exposure. Ungut Formation, Kaltat type of section. Alternating limestones and siltstones

Mud flow swirls

Dike

The Kaltat type of the section of the Ungut Formation is developed along the right bank of the Bazaikha River, where outcrops of its rocks extend from Krasny Kamen Mountain in an easterly direction for almost 12 km. Here, the suite is predominantly composed of dark limestones, greenish-gray and variegated siltstones, marls, and rare dolomites. The rocks are characterized by horizontal layering, even layering planes, and abundant terrigenous admixture (Zadorozhnaya, 1974). The apparent thickness of the deposits in the type section opposite the mouth of the Kaltat River is 263 m.

Many organic remains have been found in the rocks of the Ungut Formation. In the Karaulinsky type of section, this is, first of all, small-shell fauna, the remains of the most ancient skeletal organisms (“smallshellyfossils” or SSF). Among them, angustiocreids, chiolites, gastropods, tommothiids, and crustaceans of the Tommotian stage were identified (Sosnovskaya and Shurinova, 2003). The fossils determine the age of the deposits containing them as Early Cambrian (Tommoth Age).

The Torgashinsky Formation (€1tr) was identified by V. Zlatkovsky in 1885. The stratotype is a section of the Torgashinsky Ridge Formation. Here, its deposits, often creating high rocky ledges (Mount Kommunist, Mount Pioneer, etc.), occupy a significant area and compose both the axial part of the ridge and its slopes. The deposits of the suite are also known from the left side of the Bazaikha River. In contact with the rocks of the Stolbovskaya intrusion, they were turned into marbles.

The best section of the formation is located on the right bank of the Bazaikha River, opposite the mouth of the Kaltat River. Due to the good exposure and the presence of numerous organic remains, it was repeatedly visited by geologists who carried out geological survey and thematic work in this area. The main volume of the suite is composed of gray and light gray massive organogenic limestones. Layered limestones play a subordinate role. The upper part of the section contains layers of dolomites.

Calcite crystal

Calcite

At the base of the section, a member of a peculiar composition is distinguished, which has a local name - Bazakh. It is composed of lilac, light pink and gray calcareous gravelstones, sandstones, coarse clastic breccias and light pink limestones. In terrigenous rocks, angular fragments of algal limestones are abundant. The cement is carbonate with an abundant admixture of iron hydroxides, which is the reason for the variegated color. Below the Kaltat mouth, among the variegated deposits, there is a thick layer of dark gray thin-platy limestones and marls with clay and dolomite layers. In addition, the member contains solitary algal bioherms that form isolated rocky outcrops in the relief. In general, the rocks of the Bazakh Member are characterized by coarse cross bedding, signs of wave ripples, abundant erosion surfaces, poor roundness, and sorting of detrital material. The outcrops of the member stretch along the lower part of the southwestern slope of the Torgashinsky Range, where its variegated rocks are clearly visible on Mount Red Stone. On its northern slope, member rocks are known from the Panikovka brook and at the exit of the Cheremukhovsky ravine to the terrace of the Yenisei River. Its thickness is up to 250 m.

According to N.M. Zadorozhnoy (1974), the limestones of the Torgashinsky Formation form a complex organogenic structure, which can be considered as a reef complex consisting of smaller elementary organogenic structures (bioherms and biostromes) and accompanying breccia and layered limestones.

The Torgashinsky Formation is characterized by a very large number of genera and species of archaeocyaths and other groups of fossil organisms, represented by complexes of various horizons of the Atdaban, Botom, and Toyon stages of the Lower Cambrian. It lies conformably on the underlying deposits of the Ungut (Kaltat) suite. However, in some areas of the right bank of the Bazaikha River, their contact is complicated by a series of basic dikes. In the field of dike development, layered carbonate rocks are intensively folded into folds with dip angles on the limbs from 30° to 85°. Above the dikes, the occurrence of rocks is calm, with dip angles of no more than 10°. On the northern slopes of the Torgashinsky Range, the formations of the Torgashinsky Formation are conformably overlapped by the Chessovskaya Formation of the Middle Cambrian.

The total thickness of the suite reaches 900 - 1000 m.

Limestones of the suite are also known in the area of the Krasnoyarsk reservoir, where high picturesque cliffs are created along the sides of the Biryusa Bay.

Fold. Rock Ryzhaya (Creepy), the southern slope of the Torgashinsky Range

The carbonate composition of the formation and the fracturing developed in its deposits contribute to the manifestation of karst processes, including the formation of karst caves. The remnant karst relief with grottoes and arches is developed on the right slope of the Bazaikha River opposite the marble quarry. Funnels are found in the watershed part of the Torgashinsky Range. Eight caves are known here, the largest of which are Torgashinsky (length 3 km, depth 165 m) and Ledyanaya (length 720 m, depth 32 m).

Middle section (€2)

The department includes carbonate deposits of the Chessovskaya Formation.

The Shakhmatov Formation (€2sh) was identified by V.I. Popov and L.V. Yakonyuk in 1961. The stratotype is located in the upper reaches of the Bazaikha River near the village of Shakhmatovo (outside the site area).

In the area of educational practice, the rocks of the suite compose the northern slopes of the Torgashinsky Range. The suite is represented by gray layered limestones, light-colored dolomites and dolomitic limestones, red-colored siltstones. The latter are rare in the form of unseasoned interbeds no thicker than 2-3 m. Due to the admixture of manganese, the carbonates of the suite often have a pink color. Unit thickness less than 300 m.

Trilobites Olenoides convexusLerm., Erbiagranulosa, E.sibiricaLerm., Amgaspis cf.medius N.Tchern., A. sp., Gaphuraspissp., Kooteniellasp., Proasaphiscussp., ProshedinellaerbiensisSiv. and others, as well as algae Epiphytonfruticosum Vol., Renalcisgranosus Vol.

The relationship of the retinue with the underlying Torgashinsky retinue is consonant. The boundary has a gradual character and is conventionally drawn along a limestone unit containing a reliable fauna of trilobites from the lower part of the Middle Cambrian. The younger Devonian deposits are unconformable or with tectonic contacts. The age of the suite is determined from the finds of trilobites by the Amga Age of the Middle Cambrian.

Ordovician system (O)

Middle-upper divisions (O2-3)

Imir Formation (O2-3im). The volcanic rocks of the suite, together with subvolcanic formations, are part of the Imir volcanic complex and are widespread within the Kachinsko-Shumikhinskaya depression, which is located in the northwestern frame of the Eastern Sayan fold system. This structure stretches in the latitudinal direction for 50 km to the west of the outskirts of the city of Krasnoyarsk and has a width of up to 30 km along the meridian. In the western part of the depression (near the city of Divnogorsk), the volcanogenic rocks of the Imir Formation were studied in detail by V.M. Gavrichenkov and A.P. Kosorukov. In the northern part of the territory, within sheet O-46-XXXIII, sections of volcanic rocks of the Ordovician age were first described by E.I. Berzon and V.E. Barseghyan (Berzon et al., 2001). And in the eastern part of the depression, on the slopes of the Dolgaya Griva ridge, sublatitudinally stretching to the west from Mount Nikolaevskaya (First) Sopka - M.L. Makhlaev and O.Yu. Perfilova (Makhlaev et al., 2007; Perfilova and Makhlaev, 2010). In terms of petrographic composition and structural-tectonic position, the volcanic complex of the Kachinsko-Shumikhinskaya depression for many decades was compared with the Byskara series of the Minusinsk trough and belonged to the Early or Early-Middle Devonian. But subsequently, based on the effusive rocks of the northern part of the depression and subvolcanic bodies from the Divnogorsk section, isotope dates recognized as sufficiently reliable were obtained, according to which the age of the complex is Middle-Late Ordovician.

Nikolaevskaya (First) Sopka

The rocks of the suite with a sharp structural unconformity overlie the older complexly dislocated Vendian-Early Cambrian formations and are unconformably overlain by the red-colored deposits of the Middle Devonian.

In general, moderately alkaline basaltoids predominate in the lower part of the section of the formation, while moderately and moderately acidic effusives (lavas and tuffs of trachytes, trachydacites, and trachyrhyodacites) dominate in the upper part. The large thickness of the volcanogenic section is characteristic. Only one continuous section along the Yenisei River near the city of Divnogorsk, studied in detail by V.M. Gavrichenkov and A.P. Kosorukov, it is at least 2800 m.

There are two subformations: the Lower Imir trachybasalt-basaltic andesite and the Upper Imir trachyandesite-trachyte-trachydacite.

Nizhneimir subformation (O2-3im1) in the basins of the rivers Smooth and Krutaya Kacha, Bol. Minanzhul is composed of lava flows and covers of olivine, olivine-augite, augite-plagioclase and plagioclase trachybasalts, trachyandesite basalts, less often trachyandesites with a thickness of 1–5 to 30–40 m. glassy base. The glass content increases towards the top and bottom of the flow. In the marginal parts of the flows, the volcanic rocks are mainly of the pilotaxitic structure. At the top of the streams, the rock texture is usually almond-stone. A few interlayers of litho-, vitro- and crystal-clastic psammite, psephytic and psammopelitic tuffs, tuff sandstones, tuff siltstones, volcanomictic sandstones are observed. In the lower part of the suite, there are interlayers of tuff-gravelites and tuff-conglomerates, which include fragments of limestones of the Torgashinsky Formation and dolomites, probably of the Ovsyankovskaya Formation. The cement is basal, basal-porous carbonate pelitic with an admixture of chlorite, clayey-carbonate, carbonate, zeolitic and clayey-ferruginous.

The total thickness of the subformation is from 350 to 1000 m.

The Upper Imir subformation (O2-3im2) is composed of lava flows and covers of trachytes, trachydacites, trachyrhyodacites, less often trachyrhyolites, andesites and trachybasalts, as well as their tuffs and tuff lavas. The boundary between the lower and upper subformations is drawn by E.I. Berzon and others on the replacement of essentially basaltoid volcanic rocks by rocks of intermediate and acidic composition. Often, tuffs of mixed composition occur at the base of the upper subformation.

The composition of the upper subformation in the northern part of the depression in the basins of the Karaulnaya and Gladkaya Kacha rivers is dominated by lava flows (10–110 m thick) of trachytes, trachydacites, trachyrhyodacites, less often trachyrhyolites, as well as their tuffs. The rocks of the upper subformation are mainly colored in various shades of red and brown. Porphyritic varieties predominate. The thickness of the subformation is up to 1800 m.

In the area of the city of Divnogorsk, a significant proportion of the volume of the upper subformation is composed of moderately alkaline felsic rocks (trachydacites, trachyrhyodacites), which are absent in the eastern part of the depression. Trachytes for this part, on the contrary, are not typical. The total thickness of the effusive section here is somewhat greater than in the eastern part - at least 2800 m. Thus, the volcanic sequence is characterized by lateral irregularity, sharp fluctuations in the thickness of individual bodies along strike.

The absolute age of trachytes according to Rb-Sr isochron dating was 447+6 Ma, and K-Ar - 464+11, 452+11 and 467+11 Ma. Previously, the age of these effusives was determined by the Rb-Sr method - 442 ± 2 Ma.

A number of geologists dispute the attribution of the volcanogenic formations of the Kachinsko-Shumikhinskaya depression to the Imirskaya suite and propose to distinguish them under the local name of the Divnogorskaya sequence with the same age of O2-3. (Kruk et al., 2002; Makhlaev et al., 2007, 2008; Perfilova and Makhlaev, 2010).

Objects with uranium mineralization of the uranium-molybdenum formation and numerous manifestations of fluorite along both banks of the Krasnoyarsk reservoir are paragenetically associated with the rocks of the Imir Formation. Volcanic rocks (trachytes, trachydacites) in terms of their physical and mechanical properties meet the requirements of the industry and were widely used for backfilling railway embankments and highways. Some varieties of large-porphyritic volcanic rocks of the Imir Formation are quite decorative and can be used as a facing stone.

Devonian (D)

Deposits of the Devonian system are widely developed on the territory of Krasnoyarsk and its environs. They fill the Rybinsk depression, stretching from the northwestern suburbs of Krasnoyarsk in the east and southeast direction, and are represented by all three divisions of the Devonian system.

Lower section (D1)

Karymov Formation (D1kr). The Karymov Formation begins the section of the Devonian deposits of the Rybinsk depression. Its deposits stretch as a strip along the northeastern foot of the Torgashinsky Range from the village. Torgashino on the southern outskirts of the city of Krasnoyarsk in the direction of Mount Chernaya Sopka and Petryashino station and further in the SE direction.

The lower part of the section has a terrigenous composition and is either distinguished as the Nizhnekarymovskaya subformation (D1kr1) or is considered as an independent suite - Assafievskaya (D1as). Its deposits with structural unconformity lie on a deeply eroded surface of carbonate deposits of the Lower-Middle Cambrian. This boundary and the basal horizon of the Assafiev Formation developed above were exposed in the eastern wall of the Uval Promarteli quarry opposite the Krasnoyarsk CHPP-2. Here, an erosion surface developed on the limestones of the Torgashinsky Formation with deep (up to 0.8 m) pockets was exposed, above which variegated terrigenous deposits occur. "Pockets" in limestones are filled with weakly cemented non-layered gray-green siltstones. Above, the section of the basal horizon is consistently built up by fine-medium-grained sandstones with parallel and oblique bedding. Sandstones of sandy-yellow and burgundy color are interbedded. Numerous imprints of propteridophyte (rhiniophyte) flora are found in yellow sandstones. The thickness of the sandstones is about 1.5 m. Poorly sorted gravel-conglomerates with sandy cement and gravel-pebble rounded fragments of underlying rocks, at least 2 m thick, conformably overlie. Several years ago, this outcrop was destroyed during construction work.

Rhinophyte prints

In general, in the lower part of the section of the Nizhnekarymovskaya subformation (Assafievskaya suite), polymictic sandstones of yellow, pinkish-gray and red color, with parallel or directed oblique bedding, predominate. At different levels, they contain interlayers and lenses of polymictic gravelstones and conglomerates or interlayers of green or red-colored siltstones and mudstones. The thickness of the lower part of the section of the subformation is more than 100 m.

A coarse-grained member occurs higher along the section. Its section is represented by intercalation of small-, medium-, and large-pebble (sometimes with an admixture of boulder material) conglomerates. Interlayers and lenses of gravelstones and sandstones are occasionally encountered. Polymictic conglomerates; pebbles are composed of various igneous and sedimentary rocks: syenites, granite-porphyries, diorites, gabbroids, effusives of various compositions, limestones, etc. The total thickness of the Nizhnekarymovskaya subformation (Assafievskaya formation) is at least 400 m.

The deposits of the Nizhnekarymovskaya subformation can be observed in numerous small outcrops along the foot of the Torgashinsky Range (near the settlements of Torgashino and Vodnikov).

Higher up, the section of the Karymov subformation is built up by substantially volcanic formations, the sections of which are exposed in the banks of the Berezovka River in the area of Petryashino Station. Here, intercalated irregularly, often composing wedge-shaped and lenticular bodies, mainly lava formations of a moderately alkaline composition, ranging from basaltoids of increased alkalinity to trachyrhyodacites. A subordinate role is played by interlayers of red sandstones and polymictic conglomerates. The total thickness of the volcanogenic part of the section in the vicinity of Petryashino station is at least 100 m.

Artificial outcrop of the Karymov Formation. Mount Ostraya near the Petryashino platform
Fragments of amygdaloidal basalts in red sandstones and conglomerates

Almond stone basalt

Agglomerate from volcanic bombs

Volcanic bomb

More precisely, the age of the terrigenous deposits of the Karymov Formation is determined as Lower Devonian based on numerous remains of the propteridophyte (rheniophyte) flora. The largest is the Torgashinsky locality, discovered in the 1930s. and studied in detail by the largest expert on the propteridophyte flora A. R. Ananiev, widely known in the world literature, which is located in the former quarry "Uval Promarteli". Здесь определены Protohyeniajanovii, Prototaxitesforfarensis (KidstonetLang.), MinusiaantigmaTschirk., ZosterophyllummyretonianumPenh., DistichophytummucronatumMagdefrau, Sawdoniaornate (Daws) Hueber, Margophytongoldshmidtii (Halle) Zakh., PectinophytonbipectinatumAnan., PtotobarinophytonobrutscheviiAnan., Ienisseiphytonrudnevae (Peresv.) Anan., Drepanophycus spinaeformis Goepp., Platyphyllum fasciculatum Anan., Enigmophyton hoegii Anan., Broeggeria laxa Anan., Relliniia thomsonii (Daws.) Leclerc et Bon. Unfortunately, at present this location is not accessible for observation, as it was filled up during the construction of the dam of the ash-sump of the Krasnoyarsk CHPP-2, despite the fact that it is listed as a protected natural monument.

Middle section (D2)

The Pavlovskaya suite (D2pv) rests with erosion and angular unconformity on the rocks of the Lower Devonian Karymovskaya suite. Its deposits stretch as a strip from the northwestern outskirts of the city of Krasnoyarsk, through the central part of the city to its southeastern suburbs (Zykovo station area) and beyond. The deposits of the Pavlovskaya Formation are best exposed along the Kacha River, especially along the southern slope of the Pokrovskaya Mountain. It is on the cliffs, composed of red-colored rocks of this suite (“red ravines”), that the city of Krasnoyarsk got its name.

R. Kacha

"Krasny Yar" on Kacha

Drokinskaya Sopka

At the top of the Drokinsky hill

The Pavlovskaya suite is composed exclusively of sedimentary rocks of terrigenous, partly carbonate composition: sandstones, siltstones, gravelstones, conglomerates, marls and limestones. According to lithological features (to the greatest extent in terms of the content of carbonate rocks), it is subdivided into 3 subformations.

Lower Pavlovsk Subformation (D2pv1). The sediments of the lower subformation make up most of the section of the suite and are represented by sandstones, conglomerates, siltstones, and marls with rare limestone lenses. These rocks are exposed near the villages of Drokino, Lukino, Kuznetsovo and in the eastern part of the city of Krasnoyarsk. At its base lies a member of sandstones, with an admixture of sandy-gravel material and small pebbles of volcanic rocks. There are interlayers and lenses of carbonates. Above lies a thick (up to 70 m) member of conglomerates and sandstones with rare interlayers of sandy marl.

The middle part of the lower subformation is composed of often interbedded marls and sandstones. Marl greenish-pink and pinkish-gray fine-grained, red and pinkish-gray sandy, sometimes red-burgundy strong with small mica flakes. Fine-grained greenish-pink sandstones with interlayers of gritty sandstones and burgundy-red dense slightly sandy marls.

Higher up the section, sandy-conglomerate sediments with thin interlayers and marl lenses again predominate. Small weakly rounded pebbles are represented by siliceous rocks, syenites and basic effusives.

The total thickness of the Lower Pavlovsk subformation is 350 - 400 m.

The Middle Pavlovian subformation (D2pv2) is a marker sequence and can be traced in a significant part of the Rybinsk depression. The lower boundary is drawn by the appearance in the section of the formation of limestone layers containing nodules of red chalcedony. It is composed mainly of red-brown, rarely greenish-gray marls, among which lie layers and lenses of limestones, sandstones and individual lenses of conglomerates. This subformation is the most saturated with carbonate rocks. Interlayers of limestone, occurring among rocks less resistant to weathering, form pronounced, sometimes stepped and cuesto-like relief forms.

Marking limestone horizon near the village of Kuznetsovo

Marking horizon of detrital limestones (calcarenites) on Pokrovskaya Gora

3 km southeast of the village of Drokino, on the left bank of the Kacha River, among the yellow sandstones, there is a thin (0.3 m) layer of fine-grained sandstone with imprints of plants OrestoviabazhenoviiLar., SporitesdevonicusGar., SporitessibiricusGar., ProtocephalopterispraecoxAnan., Psilophytoncf. dawsoniiAndrewsetal. and etc.

The thickness of the Middle Pavlovsk Subformation is about 120 m.

The Upper Pavlovsk Subformation (D2pv3) is similar in lithological composition to the Lower Pavlovian Subformation and differs from it in a slightly larger number of limestone layers and the presence of mudstones. The section of the subformation was almost entirely exposed by a trench cut in the north-northeast direction from the chapel (the top of Mount Karaulnaya) for about 650 m. sandstones and small-pebble conglomerates occur. The thickness of the deposits of the upper subformation is up to 120 m.

The age of the Pavlovskaya suite is determined as Middle Devonian based on the finds of flora prints near the village of Drokino.

Upper Devonian (D3)

The Kungus Formation (D3kn) is widespread in the area of the city of Krasnoyarsk. Its deposits extend to the southeast from the settlement. Salt licks through the territory of the Soviet district of the city to the village of Lopatino. The rocks of the Kungus Formation are generally unstable to weathering and are poorly exposed. Their exits can be observed in the basement of the terrace on the left bank of the Yenisei below the Medical Academy. In addition, the deposits of the suite were uncovered by numerous wells in the process of engineering and geological research at the beginning of the development of the Vzlyotka microdistrict.

The Kungus Formation conformably overlies the Pavlovskaya Formation. Its lower boundary is conventionally drawn by the replacement of marls of the upper part of the Pavlovskaya suite by a member of gravel-sandstone rocks containing interlayers of grayish-white sandstones. Higher in the section, there is an interbedding of brick-red, less often green-colored siltstones and marls, often sandy, with interlayers of sandstones, mudstones, gravelstones, limestones.

Interbedded sandstones, gravelstones and siltstones
Kungusskaya suite near the village of Solontsy

Red-colored siltstones and gravelstones near the village of Solontsy

gravelite

Gravelite with calcite crystals

Characteristic of the Kungusskaya suite are limestone conglomerates called "caviar" limestones. They consist of flat and round pebbles of limestone and marl ranging in size from 1 to 5 cm in diameter. The cement of limestone conglomerates is limestone-argillaceous material.

Buried wave-cutting niche

buried ravine

Devonian takyrs

The upper part of the suite is eroded prior to accumulation of overlying Carboniferous deposits. The thickness of the formation near the city of Krasnoyarsk is more than 300 m, in the adjacent parts of the Rybinsk depression it reaches 600 m.

The flora identified as Pseudoborniacf. was collected from the lower horizons of the formation. ursineNath., and Archaeopterissp., Archaeopteriscf. fimbriata Nath. and others. Scales of armored fish identified as Bothriolepiscf. sibiricaObr., remains of armored fish identified as Osteolepidae were found in limestone conglomerates. All these finds determine that the suite belongs to the Upper Devonian.

Carboniferous system (C)

Lower section (C1)

The Charga Formation (C1čr) rests with erosion on the underlying deposits of the Upper Devonian. They are distributed on the right bank of the Yenisei near the eastern outskirts and in the adjacent part of the suburban area of Krasnoyarsk. The rocks of the lower part of the section of the Charginsky Formation are best exposed, observed along the right bank of the Berezovka River near the Sukhoi platform and along the road between the village of Voznesenskoye and the village of Lopatino. In the section near the Sukhoi platform, the base of the suite was not exposed, but a fragment of the lower part of the suite about 80 m thick was exposed. In the section, sandstones and siltstones (mainly calcareous), less often gravelstones and conglomerates, and sometimes limestones rhythmically alternate. The latter often contain nodules and interlayers of orange cherts. Characterized by sharp boundaries between lithological differences; wavy erosion surfaces are not uncommon. The thickness of the layers is variable, there are cases of their wedging out along the strike. Directional cross bedding is widespread. Among the limestones, clastic varieties are common - calcarenites. In the lower part of the section, red-colored colors predominate; higher up, green-colored ones are becoming more widespread. The share of carbonate rocks also increases up the section.

The higher part of the formation section is represented by intercalation of greenish marls, brick-red siltstones, and limestone conglomerates. The uppermost part is dominated by limestone conglomerates and limestones with inclusions of chalcedony. Interlayers of calcareous sandstones, siltstones, and mudstones are noted among them. The coloration is variegated with an irregular alternation of greenish-gray and red-colored differences. Limestone conglomerates along the strike are often replaced by greenish-gray sandstones with a large number of fragments of quartz, chalcedony and lozenge fragments of marl, as well as fine-grained sandstones - siltstones.

The thickness of the suite is over 450 m.

In a layer of green-colored siltstones from the upper part of the suite section, along the Voznesenskoye-Lopatino road, numerous plant imprints were found: AsterocalamitesscrobikulatosSchoth. and HeleniellatheodoriZal., which determine the age of the deposits as Early Carboniferous (Tournaisian).

The Krasnogoryevskaya Formation (C1kr) is developed in the vicinity of Krasnoyarsk as a narrow sublatitudinal band traced from the area of the village of Berezovka to the village of Voznesenskoye. It conformably builds up the section of the underlying Charga Formation and, with deep erosion and angular unconformity, is overlain by Lower Jurassic deposits, and therefore its section in the area is incomplete.

Variegated interbedded siltstones, sandstones, gravelstones
Krasnogoryevskaya suite near the village of Voznesenka

Layer of green siltstones and mudstones

The suite is represented by interbedded pinkish-yellow, yellowish-green sandstones with subordinate layers of green siltstones and mudstones. There are interbeds of felsic ash tuffs, tuffites, and tuff sandstones. The most representative fragment of the lower part of the formation section is exposed by a roadside quarry near the southeastern outskirts of the village of Voznesenskoye, along the road to the village of Lopatino. Pink, yellowish often micaceous fine- and medium-grained quartz-feldspar sandstones are exposed here. The sandstones are often calcareous, sometimes enriched in calcium phosphate. They often contain flat-shaped fragments of bluish-green mudstones and well-preserved remains of large-stemmed lepidodendron flora. Higher in the section, they are replaced by greenish coarse-grained quartz-feldspar sandstones. The upper part of the formation is composed of fine- and medium-grained greenish-gray and greenish-yellow sandstones intercalated with bluish-green mudstones. The thickness of the Krasnogoryevskaya suite is more than 300 m.

Lepidodendron trunk imprint

Lepidodendron flora imprint

According to the remains of the lepidodendron flora PorodendroncristatumChachl., PorodendronplicatumChachl., Knorriasp. and others. The age of the suite is determined as Early Carboniferous.

Mesozoic erathema (MZ)

Jurassic system (J)

Jurassic deposits are common in the northern and eastern parts of the city of Krasnoyarsk and in the surrounding environs. The sediments of this level are represented by a continental coal-bearing formation, the most important feature of which is its rhythmic structure. Elementary cycles of sedimentation usually begin with sandstones, less often with gravelstones or conglomerates. Up the section, sandstones give way to siltstones and mudstones. And, finally, these cycles are often crowned with layers and interlayers of brown coal. All Jurassic deposits of the area of the city of Krasnoyarsk belong to the eastern zone of the Chulym-Yenisei depression. The Jurassic deposits of the city and its immediate environs belong to two divisions of this system - the lower and the middle. The Lower Jurassic is represented by the Makarov and Ilan Formations, the middle Jurassic by the Itat Formation, and the overlying deposits are already developed at a considerable distance from the city.

In the Jurassic deposits of the region of the city of Krasnoyarsk, facies variability is manifested. In the direction from east to west, the number of elementary cycles and, accordingly, the coal seams and layers usually crowning them increases.

Lower section (J1)

Makarov Formation (J1mk). Deposits of the Makarov Formation are distributed along the right bank of the Yenisei on the eastern outskirts of the city of Krasnoyarsk. They unconformably overlie Paleozoic rocks and are represented by conglomerates, sandstones, siltstones, mudstones with several thin brown coal seams. The most complete section of the formation is observed in coastal outcrops along the right bank of the Yenisei River, below the northern end of Tatyshev Island.

At the base of the suite lie yellowish-gray weakly cemented conglomerates with poorly sorted but well-rounded pebbles of siliceous and volcanic rocks, less often granites, quartzitic sandstones, metamorphic schists, and gneisses. There are pebbles of kaolinized rocks, which is associated with the processes of redeposition of formations formed at the end of the Triassic - the beginning of the Jurassic of the areal Korf weathering. The thickness of the conglomerates is 30 m; their outcrops are also found along the Sukhoi creek.

Higher in the section, conglomerates through a member of yellow and gray-green medium-fine-grained sandstones with interlayers of gravelstones are gradually replaced by rhythmic interbedding of predominantly gray-green fine-grained sandstones, siltstones and mudstones with interlayers of brown coal. In the uppermost part of the section, greenish-gray mudstones with interlayers of fine-grained sandstones and three layers of brown coal up to 1 m thick predominate. The total thickness of the Makarovskaya suite deposits in the Krasnoyarsk region is about 100 m, in the western regions of the region it increases to 200 or more meters.

Imprints of plants CladophlebiswhitbiensetennueHeer, Elatocladusmanchurica (Lokojame) Labe were found in the deposits of the Makarovskaya Formation. Representative spore-and-pollen complexes were identified from them, in which there is pollen of Ginkgoales, Bennetites, conifers, spores of ferns, characterizing the age of the formation in the Sinemurian and Pliensbachian stages of the Lower Jurassic.

Ilan Formation (J1il). The deposits of the suite stretch in a narrow strip from the eastern outskirts of the city of Krasnoyarsk to the village of Barkhatovo. Here, the Ilan Formation occurs with erosion on different horizons of the Makarov Formation and on the underlying Paleozoic deposits. Unlike the underlying and overlying deposits, it does not contain industrial coal seams. There are only thin (up to 1.6 m) interlayers of coal-bearing rocks, less often brown coals. The lower boundary of the suite is drawn along the top of the carbonaceous rocks occurring in the upper part of the Makarovskaya suite, or along the change of predominantly sandy fractions of the Makarovskaya suite by intercalation of siltstones, mudstones and sandstones. The Ilan Formation is composed of siltstones, sandstones and mudstones, with interlayers and lenses of carbonaceous mudstones, less often brown coals. Characterized by gray-green tones of color.

The deposits of the Ilan Formation are characterized by spore-pollen complexes of the Toarcian stage of the Lower Jurassic. Its total thickness is up to 180 m.

Middle section (J2)

Itat Formation (J2it). The formations of the Ilan Formation compose vast areas in the Krasnoyarsk region on the left bank of the Yenisei, within the microdistricts of Zelenaya Roshcha, Severny, Solnechny, in the vicinity of KRAZ and the village of Peschanka. Its basal layers lie with erosion on various horizons of the Ilan Formation, and in the marginal parts of the Chulym-Yenisei depression - on older deposits. The rocks of the Itat Formation can be observed in the coastal outcrops of the Yenisei below the city of Krasnoyarsk, in the area of the villages of Korkino, Kubekovo, and Khudonogovo. It is composed of rhythmically interbedded sandstones, siltstones, mudstones, carbonaceous siltstones and mudstones, with interlayers and lenses of conglomerates and gravelstones, coal seams.

The suite includes sandstones, siltstones, mudstones, carbonaceous siltstones and mudstones, interlayers and lenses of conglomerates, gravelstones, coal seams. Based on the cyclic structure of the section, the suite is subdivided into three subformations, each of which begins with deposits of an essentially sandy composition with interlayers and lenses of coarse clastic rocks, and ends with predominantly fine clastic (silty argillite) rocks with seams and interlayers of brown coal. The deposits of the suite are characterized by representative spore-and-pollen complexes of the Middle Jurassic (Lower Itat Subformation - Aalenian Stage, Middle Itat Subformation - Bajocian Stage, Upper Itat Subformation - Bathonian Stage).

The Upper Itat subformation is characterized by a rich complex of flora and fauna. The chain of outcrops where organic remains were found stretches from the village of Kubekovo for 7 km and ends below the village of Khudonogovo. Remains of gymnosperms Ginkgo, Bajtra, Phoenicopsis, Czekenowckia, ferns Coniopteris, Cladophlebis, arthrophytes Equisetites, etc. are found here. insects. Their remains were found in the upper part of the section of the Upper Itat subformation in several layers, which are maintained along the strike for a considerable extent. Very numerous and diverse forms have been found here - both aquatic (larvae of mayflies, water beetles Temptus, dragonflies, caddis flies, stoneflies, lacewings) and terrestrial (hemipterans, cockroaches, beetles).

The thickness of the Lower Itat Subformation is up to 150 m, the Middle Itat Subformation is up to 250 m, the Upper Itat Subformation is up to 200 m. The total thickness of the Itat Formation is up to 600 m.

Cenozoic erathema (KZ)

Quaternary system (Q)

Deposits of the Quaternary system are used in the vicinity of Krasnoyarsk almost everywhere. Natural deposits of various genetic types are widely represented here: alluvium, proluvium, eluvium, colluvium, deluvium, desertion, defluction, limnia, polestry, delipsium, as well as technogenic formations. Their age ranges from Eopleistocene to Holocene (modern). The basis of the age division of the Quaternary deposits of the region is the chronological sequence of the formation of the terrace complex of the Yenisei. Therefore, alluvial deposits that make up the surfaces of terraces of different ages are most reliably dissected. The age of terraced alluvium was determined from spore-pollen complexes, bone remains of mammals, and, for the youngest, from Paleolithic tools. Deposits of other genetic types are compared with different levels of the terrace complex according to geomorphological features. Those that are superimposed on the surfaces of the terraces or confined to the landforms cut into them are considered as younger ones.

In total, in the region of Krasnoyarsk in the Yenisei valley, nine terraces of different hypsometric levels and, accordingly, age are distinguished. All of them, with the exception of the first, have their own names. The first terrace - up to 9 m above the modern water line, the second (Ladeyskaya) - up to 15 m, the third (Krasnoyarskaya) - up to 25 m, the fourth (Berezovskaya) - up to 35 m, the fifth (Lagernaya) - up to 60 m, the sixth (Sobakinskaya ) - up to 80 m, the seventh (Torgashinskaya) - up to 110 m, the eighth (Khudonogovskaya) - up to 140 m, the ninth (Badalykskaya) - up to 220 m. . Only in some sections of their course are single remnants of terraces found, and a complete terrace complex, similar to the Yenisei, is nowhere developed. In the vast watershed spaces, where there is no possibility of geomorphological comparison with the terrace complex, Quaternary deposits of all genetic types are considered as belonging to the undivided Quaternary system.

Quaternary deposits are described by genetic types.

Alluvial deposits formed throughout the Eopleistocene to the present. Alluvium of the IX (Badalykskaya) and VIII (Khudonogovskaya) terraces belongs to the Eopleistocene. In the region of Krasnoyarsk IX, a terrace has been preserved on the left side of the Yenisei valley near the village of Badalyk, on the right - on Mount Sosnovy Mys, where the lower part of the alluvium is uncovered by a quarry. Here, on the variegated clays of the weathering crust, horizontally layered sands, polymictic pebbles, cemented with ferruginous coarse-grained sand, occur with erosion. The upper part of the sequence near the village of Badalyk consists of pebbles, which includes many weathered rocks cemented with ferruginous kaolinized sand, and gray-brown loam with sand lenses (Berzon et al., 2001). The total thickness is up to 9 m. Terrace VIII above the floodplain is most pronounced on the left bank, in the area of the State University and the biathlon shooting range near the western outskirts of the city. Here, in the sides of the dens, one can observe outcrops of brown calcareous sandy loams corresponding to the upper part of the section. The lower parts of the alluvium VIII section were observed by E.I. Berzon et al. (2001) in the upper part of the Pokrovka microdistrict, where they are represented by ocher-brown sand with pebbles of siliceous rocks, sandstone, granite, as well as sandy loam and loam. The total thickness of alluvium in terrace VIII is up to 25 m.

Alluvium of the VII (Torgashinsky) terrace, 80-110 m high, belongs to the lower link and the lowest part of the middle links of the Neopleistocene. This terrace is one of the most pronounced terraces of the Yenisei in the Krasnoyarsk region. On its surface, on the left bank, there are Akademgorodok and Studenchesky Gorodok, and on the right bank, it stretches along a significant part of the northern slope of the Torgashinsky Range from the Bazaikha River to the area of the village of Torgashino (Tsemzavod). The upper parts of the terrace section are well exposed in roadside excavations near the pond in the area of the subsidiary farm of the Yenisei sanatorium, to the west of Akademgorodok. Here, dense loams are revealed, grayish-brown in color, with thin parallel layering (with unseasoned interlayers of dark gray color), calcareous; interbedded with sandy loams and overlapped by them. The lower parts of the section are not exposed, but along the sides of the logs cut into the terrace, there are numerous well-rounded small pebbles of various compositions, apparently washed out from the terrace alluvium. The total thickness of the Torgashinsky alluvium is up to 40 m. The age is determined by the findings of the fauna of mammoth, woolly rhinoceros, bison, mollusks, data of spore-pollen and paleomagnetic analyzes directly on the territory of the city of Krasnoyarsk (Gremyachiy Log).

Alluvial deposits of the VI and V terraces of the Yenisei belong to the middle link of the Neopleistocene. VI (Sobakinskaya) terrace is best developed on the left bank of the Yenisei, near the western outskirts of Krasnoyarsk. Here it stretches from the region of the mouth of the Karaulnaya River, through the estuary part of the Sobakin River near the village of Udachny to the Cave ravine near the western outskirts of Akademgorodok. The lower parts of the section of the Sobkin alluvium were exposed by a small quarry located on the surface of the terrace opposite the Sosny governor's residence. Predominantly small-clastic pebbles are developed here, which include volcanic and siliceous rocks, vein quartz; there are poorly rounded fragments of Vendian sandstones that form the basement of the terrace. The overlying part of the alluvium section is exposed by pits and is composed of light loams and sandy loams, often calcareous. The total thickness of alluvium in terrace VI is up to 10 m. Terrace V (Lagernaya) is widely represented on the left bank, from the mouth of the Kacha to the Aluminum Plant. To a depth of 1.5-2 m, the terrace is composed of loess-like loams. Sandy loam, fine-, medium-grained sands with rare pebbles can be traced below. Pebbles are observed at the base. The thickness of the alluvium of terrace IV reaches 35 m. The lower part of the alluvial sequence is dated to the second Middle Neopleistocene interglacial based on the findings of remains of the mammoth fauna and the spore-pollen complex (Berzon et al., 2001)

Upper Neopleistocene alluvium is represented by sediments IV (Berezovskaya), III (Krasnoyarskaya), and II (Ladeiskaya) terraces of the Yenisei. Terrace III, on which the center of the city of Krasnoyarsk is located, enjoys the greatest development. The terrace is accumulative, composed of pebbles with lenses of sand. In some places, the pebbles are covered with loess-like loams and mounds of winnowed sands. The thickness of the sediments is 20 m. The bottoms of alluvium with the remains of the woolly rhinoceros and the mammoth, according to the composition of the spore and pollen complex and the characteristics of the sediments, correspond to the glacial period. The tops of the section contain the southern taiga SPK with an admixture of broad-leaved trees corresponding to the interglacial. The lower cultural layer of the Upper Paleolithic site "Afontova Gora II" near the railway bridge is confined to the cover formations of the terrace. A radiocarbon dating of 20900±300 years was obtained from it (Berzon et al., 2001). Terrace II is widespread on the right bank. The entire area along Krasnoyarsky Rabochiy Avenue is confined to its surface. Terrace alluvium is represented by pebbles, layered sandy loams with interlayers of greenish clay, and gray loams. Thickness 14 - 20 m.

Late Pleistocene-Holocene marginal age has deposits of the first floodplain terrace of the Yenisei. They are represented by sandy loams with interlayers of clays and silts, sands, and pebbles. The thickness of deposits is up to 9 m.

Modern alluvium is represented by channel and floodplain deposits of the Yenisei and its tributaries - Bazaikha, Berezovka, Kacha, Karaulnaya, etc. Its composition is mostly pebbly or sandy, with lenses of sediments of silty-clayey composition. In areas with a rapid current, there are boulder deposits, observed, in particular, in the mouth part of the Kaltat stream and some sections of the river. Bazaihi.

Lacustrine-alluvial deposits, comparable with level VIII of the Yenisei terrace (Eopleistocene), compose the plain along the left bank of the river. Kacha, being facies of the periglacial basin in the valley of the river. Yenisei. They are represented by brown, gray, greenish-gray clays with silt, at the base of which there are sandy loams, clayey sands with gravel. Thickness 5-15 m (Berzon et al., 2001).

Lacustrine sediments (limnium) accumulate in modern ponds, a large number of which are located in the suburban area of Krasnoyarsk. They are represented by sapropelic silts with thin horizontal layering and an admixture of sandy material. They can be observed during dry seasons when the water level in the ponds is low. Holocene age.

Swamp deposits (polustria) are developed locally in highly humid areas in the floodplains of streams and small rivers. Their observation is possible only when driving small pits in late autumn, when the swamps begin to freeze. Sediments are represented by clay-organogenic deposits of dark gray color, with a large amount of undecomposed plant material. The bog deposits found in the vicinity of Krasnoyarsk are Holocene in age.

Eluvium is the products of the destruction of bedrocks occurring at the place of formation. It covers gently sloping peaks and watersheds with a thin layer. It is represented by gruss and crushed stone, the composition of which corresponds to the underlying bedrock. It usually lies directly under a layer of turf. Power - up to the first tens of centimeters. Age is determined in the range from the Eopleistocene and even Late Neogene to modern.

Proluvium is a deposit of temporary water flows. It composes numerous alluvial fans superimposed in the mouths of dry dens on the surfaces of various terraces and the modern floodplain, and also often lines the bottoms of dry dens. It is composed of unsorted loams and sandy loams, usually brown in color, with rubble, sometimes with blocks. Clastic material is always represented by rocks developed higher up the slope. In areas where the eroded substrate is represented by carbonate rocks, the deposits are calcareous and have a whitish color. In some cases, when the alluvium of high terraces is eroded, well-rounded pebbles are present in the proluvium. In alluvial fans, coarse irregular layering is manifested, expressed in the alternation of layers and lenses that are not consistent in thickness, differing in the proportion of coarse clastic material in the composition. In the section of some alluvial fans, there are horizons of buried soils. This indicates interruptions in the accumulation of proluvium, during which the formation of the soil cover began, after which the removal of detrital material by temporary flows resumed. Numerous alluvial fans can be observed along the entire road from the village. Dachny on the left bank of the Yenisei (near Akademgorodok) to the village. Udachny (where they are often exposed by roadside cuts), as well as along the foot of the Torgashinsky Range along the right bank of the Bazaikha River. Proluvium thicknesses in alluvial fans can reach 10 meters or more.

The age of the proluvium and all the slope deposits described below is determined geomorphologically in each area according to the relationship with the terraced surfaces. In general, their accumulation proceeded in the range from the Eopleistocene to the Holocene and continues at the present time.

Colluvium - landslide and talus deposits - is represented by crushed stone and blocks. It is developed mainly on the steep and dry slopes of southern exposure, where physical weathering processes predominate and their products cannot be retained by too sparse vegetation cover. Colluvial deposits cover the slopes with a thin cover and form, often together with proluvial alluvial fans, trails along their foot, up to several meters thick. These deposits are most developed where the slopes are composed of unstable, highly fractured bedrock. This can be observed along the entire foot of the high terraces of the Yenisei along the road from Akademgorodok to the village. Udachny, where the basement is almost entirely composed of sandstones and siltstones of the Tyubilskaya suite, which easily crumble into shag when weathered.

Desertium is an unsorted rubble material developed on slopes of medium steepness (mostly southern exposure), and slowly sliding under the influence of temperature fluctuations. Typical desertification formations can be observed on the SE slope of Nikolaevskaya Sopka Mountain, in a roadside excavation, where they overlap the bedrock outcrops of syenite-porphyries and microgabbro and are themselves composed of their destruction products. Desertion power up to 1 - 2 m.

Deluvium is a product of flushing with rain and melt water. It is represented in the vicinity of Krasnoyarsk by thin, essentially clayey sediments occurring in the lower parts of gentle slopes. In modern conditions, the formation of deluvium practically does not occur, since the slopes are almost everywhere covered with a fairly dense layer of turf, which protects it from erosion. The main volume of deluvium was formed during cold epochs in a periglacial setting, with a sparse vegetation cover. The processes of deluvium formation and desertification are often manifested in the same parts of the slopes, but at different times and, probably, in different climates, due to a change in the nature of the vegetation.

Defluxation is another type of slope deposits, the formation of which is the result of plastic landslide of highly moistened, substantially clayey soils. Composition - loam, often with crushed stone of the underlying rocks. It is formed mainly on the slopes of the northern exposure, as well as on the shaded and wet slopes of deeply incised dens. Here, defluction deposits also often alternate with deluvial deposits, which accumulated in colder epochs with a sparse vegetation cover. In modern conditions, defluction processes are most activated after the snow melts, when the topmost layer of soil, highly moistened with melt water, slowly slides over a deeper layer that has not thawed and therefore prevents the underground runoff of melt water. Such phenomena can often be observed in early spring in roadside cuts cutting off wet slopes.

Delapsium - deposits of landslide origin - is developed locally on steep slopes composed of loose unstable soils, provided that they are replenished with groundwater. These are heaps of entire layers or blocks of loose sediment, displaced to the foot of the slope without violating the integrity. Sometimes landslide processes are activated as a result of technogenic intervention, leading to an increase in the level of groundwater (the construction of dams, dams).

Landslide on the western slope of Pokrovskaya Mountain

Technogenic deposits within Krasnoyarsk and its environs are very diverse. Among them are blocky and rubble-blocky deposits of quarry dumps, formations of dams and embankments of various granulometry, bottom sediments of industrial sedimentation tanks. Among the latter, in particular, are the technogenic sludge of the CHPP-2 ash pit, arranged in an abandoned quarry of the Tsemzavod.

The photo shows the Torgashinsky Range, the quarries of CHPP-2 and Tsemzavod.

View from Pokrovskaya mountain

They are thin, ash-gray sediments with thin parallel bedding and high concentrations of heavy metals. As the septic tank fills up, they are removed and taken out for burial in the nearby quarry "Tsveshchy log". A special kind of technogenic deposits are accumulations of household, construction and industrial waste in numerous landfills - both legal and unauthorized. Holocene age.

5.2. INTRUSIVE MAGMATISM

Igneous formations in the vicinity of the city of Krasnoyarsk are represented by rocks of diverse petrographic composition, formed in the age interval from the Late Riphean to the Early Devonian.

Late Riphean intrusions and protrusions

Akshepa complex of alpine-type hypermafic rocks (sRF3a). The complex is dominated by serpentinites, often intensely sheared. In the Krasnoyarsk zone, its bodies form two close "belts": Akshepsky and Sliznevsky. Previously, they were united by G.V. Pinus in the Krasnoyarsk Belt. The “Sliznevsky belt” is located in the zone of a large deep-seated fault with a northeast strike up to 10 km wide (from the mouth of the Bazaikha River to the mouth of the Slizneva River) and a length of more than 35 km. The ultrabasic rocks of the complex are exposed in the basin of the Bolshaya and Malaya Sliznevykh rivers, the Sobakinaya river, on the left bank of the Yenisei River, upstream of the Udachny settlement, and also in the lower reaches of the Bazaikhi River (Golubaya Gorka and Mount Vyshku).

Rock outcrop of serpentinites on the left bank of the Yenisei River. Sliznevskaya protrusion

Serpentinite with slip mirror (1 side)

Serpentinite with gliding mirrors (side 2)

Small bodies of ultramafic rocks are close to each other, forming chains consisting of two, less often three or four lenticular bodies of linearly elongated protrusions, 100–200 m thick. km2). All protrusions are composed of sheared, rarely massive, green and dark green (to black) serpentinites, sometimes containing a few relics of olivine (partially replaced by iddingsite) and rhombic pyroxene (enstatite). Magnetite and chromite predominate among accessory minerals. Relatively large ultramafic bodies contain various ultramafic and basic rocks that have been subjected to serpentinization to one degree or another. So, on the left bank of the Yenisei, below the mouth of the Krutenkaya River and along the Sobakina River, there are intensely cataclased greenish-black pyroxenites of a panidiomorphic structure, consisting of augite, hypersthene (about 15%), strongly sericitized plagioclase (up to 10%), ilmenite and secondary: chlorite , prehnite, antigorite, biotite, brownish hornblende, and carbonates. On the right bank of the Yenisei, opposite Sobakinsky Island, there are outcrops of serpentinized dunites, 1 km above the mouth of the Bykova River, a dark green highly serpentinized olivine rock with diallag relics is exposed, penetrated by veins of chrysotile asbestos and carbonates. The serpentinites of the described region originated from pyroxenites, peridotites, dunites, and other rocks of similar petrographic composition. The complex has not been sufficiently studied, and there are no reliable data on age substantiation. Its Late Riphean age is accepted conditionally.

Bakhtinskiy volcanic complex. Subvolcanic formations (nRF3bh) are represented by sills up to 3.5x0.8 km in size and dikes up to 0.2x0.02 km, intensely greenstone-altered fine- and medium-grained microgabbro with gabbroophitic structure. The contacts of the dikes are sharp, tearing; the contacts of the sills are consistent with the enclosing deposits.

Crushing zone of fine-grained gabbro of the Bakhtin complex.

Root outlets on the right bank of the Bazaikha River, in the alignment of the Mokhovaya stream

Calcite vein in the crushing zone of fine-grained gabbro

In terms of petrochemical and petrographic characteristics, they are identical to the mantle facies volcanic rocks of the Bakhtin Formation and are often supply channels for these effusive rocks. The late Riphean age is accepted conditionally.

Middle-Late Ordovician intrusions

Genetically and spatially, they are related to the Imir Formation volcanic rocks, and the figurative points of the compositions of both volcanic and intrusive rocks form common differentiation trends on most petrochemical diagrams, which allows us to consider them as members of single volcano-plutonic associations. Magmatism of the Ordovician stage is characterized by increased alkalinity, with the predominance of Na over K, and an increased content of volatile components in the initial melts. The comagmatic nature of the rocks of the association is also emphasized by their common geochemical specificity - a low content of Rb and an increased content of Sr, Ba, Th, Mo, and B.

Imirsky volcanic complex. Vents and subvolcanic formations are an integral part of the Imir basalt-trachyandesite-trachyrhyolitic volcanic complex. They form stocks, etmolites, akmoliths, and necks up to 3 km2 in area in the fields of development of volcanogenic formations of the Imir Formation.

The vent formations of the Imir volcanic complex are represented by small (up to 200 m in diameter) necks at the southern foot of the Dolgaya Griva ridge and on the left bank of the Yenisei River, 2.5 km west of the Udachny settlement, as well as on the spit of the Gladkaya and Krutaya Kacha rivers. filled with eruptive breccias of predominantly basaltoid composition, in which single fragments of pink trachytes and microsyenites occur.

Subvolcanic formations are represented by laccolithic intrusions of quartz syenite porphyries and microsyenites in the area of the Dolgaya Griva Ridge and Minino Station, as well as numerous dikes of moderately alkaline fine-grained gabbro and microgabbro, trachybasalts, trachydolerites, and trachyte porphyries. microsyenites, microgranosyenites, comagmatic rocks of the Imir Formation. Basalts, dolerites and trachydolerites are often found in the form of dikes 0.5 - 0.6 m thick, traceable at a distance of 500 - 800 m, sometimes more than 1000 m. Usually, subvolcanic intrusions of the complex are quite well distinguished in the relief in the form of ridges, ridges and isometric peaks .

The intrusion of quartz syenite-porphyries (near the mountains Pervaya and Vtoraya Sopka) is a laccolith, the roof of which is well prepared in the modern relief. The intrusion has a zonal structure. In its center, quartz weakly porphyritic pink syenites with a fine-grained groundmass are developed, and the peripheral zone of the intrusive body is composed of microsyenites and syenite-porphyries with a fine-grained groundmass. By petrochemical characteristics, they are close to the corresponding effusives of the Imir Formation.

Geological map of the Dolgaya Griva Ridge (Perfilova, Makhlaev, 2010):

1 - Quaternary formations; 2 - Imir volcanic complex, subvolcanic formations: 2 a - syenite porphyry, 2 b - fine-grained slightly porphyritic syenites; 3 - microgabbro; 4 - eruptive breccias (vent formations); Imir Formation: 5 - trachytes (sixth member); 6 - aphyric and fine porphyry basalts (fifth member); 7 - trachytes (fourth pack); 8 - trachyte tuffs (third member); 9 - aphyric and fine porphyry basalts (second member); 10 - large-porphyry basalts (first member); 11 - Ungut suite - limestones and dolomites; 12 - Tyubilskaya suite, Upper Tyubilskaya subformation - sandy and clayey bituminous limestones; 13 - Tyubilskaya suite, Nizhnetyubilskaya subformation - sandstones, siltstones rhythmically layered, calcareous; 14 - Akshepa complex of alpine-type ultramafic rocks: serpentinites, peridotites, pyroxenites; 15 a - geological boundaries, 15 b - facies boundaries, 15 c - occurrence elements; 16 - 18 - discontinuous violations: 16 - reliable; 17 - alleged; 18 - overlain by Quaternary deposits

Syenite porphyry. Nikolaevskaya Sopka

Syenite porphyry with manganese hydroxide dendrites

Syenite porphyry with calcite coating and manganese hydroxide dendrites

The age of subvolcanic intrusions (the region of Divnogorsk and Minino station), determined by the U-Pb method, was 447 ± 10 Ma.

The Stolbovsky syenite-granosyenite complex (xO3st) was first identified by Yu.A. Kuznetsov in 1932. Subsequently, this association was more often described in the literature as the Shumikhinsky complex. But, since the latter name was used in the region in relation to several associations of intrusive rocks of different composition and age, when developing the latest serial legends for Gosgeolkart, it was decided, in order to eliminate homonymy and taking into account priority, to return to the name under which the complex was originally described.

The complex is two-phase. The first, main, phase is syenites, quartz syenites and granosyenites, hybrid endocontact monzonites and monzodiorites are of subordinate importance. The second phase consists of small stocks and dikes of moderately alkaline granites, leucogranites, granosyenites, quartz syenites, their porphyritic varieties and aplites. The structures are fine- and medium-grained, often porphyritic. The microstructure is hypidiomorphic-granular, micrographic in places. Composition of syenites: anorthoclase - 75 - 80%, oligoclase (An9-12) - 0 - 10%, quartz - 5 - 10%. In granosyenites and moderately alkaline granites, the quartz content increases to 15–30%. Dark-colored minerals - biotite (usually highly decomposed), green aegirine-augite and augite, hornblende. Accessory minerals: magnetite, apatite, zircon, rutile, sphene. Characterized by increased alkalinity of potassium-sodium, rarely sodium type, high concentrations of REE, Th - up to 30 g/t.

The petrotype of the complex is the Stolbovsky massif. In the modern erosional section, it is an oval body with an area of about 40 km2. Previously, it was considered a sub-vertical stock. But our analysis of the petrostructural zonality of the intrusion allows us to consider it as a laccolith, gently dipping to the northeast, under the Bazaikha river valley, which is also confirmed by the latest geophysical data. The formation of two phases of crystallization is distinguished in the composition of the intrusion. Almost the entire volume belongs to the main phase, composed of relatively coarse-grained rocks, the composition of which smoothly varies from syenites and quartz syenites to granosyenites. The phase of crystallization of the residual melt is represented by thin (a few centimeters, rarely up to 10 - 15 cm) veins of quartz microsyenites - moderately alkaline leucogranites. The body, composed of rocks of the main phase, has a zonal structure. The large, inner part of the intrusion is composed of biotite-hornblende quartz syenites, porphyritic, with a medium-grained (up to 5 mm in size) groundmass. The apical zone, the rocks of which are observed in the modern erosional section in the highest part of the watershed, is composed of granosyenites, which also differ in the smaller grain size of the groundmass (1–3 mm). Dark-colored minerals are represented by green augite and hornblende, rarely decomposed biotite. Accessory minerals include magnetite, apatite, zircon, sphene, and rutile. Fluorite and sulfides (pyrite, chalcopyrite and molybdenite) are sometimes noted. The marginal zone, confined to the lateral contacts of the massif, in terms of mineral composition, for the most part, does not differ from the inner one. But in some areas, grains of alkaline dark flowers are noted in it, replacing the primary hornblende. This, apparently, is associated with the processes of endocontact metasomatism at the boundaries of the intrusion with calcareous rocks, where metasomatic removal of silica is typical, resulting in an increase in total alkalinity.

Exocontact changes in the host rocks were manifested in their hornification, argillization, marmorization, beresitization, skarnization, and sometimes feldsparization at a considerable (up to 1.5 km) distance.

The rocks of the Stolbovka syenite-granosyenite complex belong to the moderately alkaline suborder of the potassium-sodium series (predominantly Na).

The Late Ordovician age of the Stolbovka complex is determined both from the outburst of comagmatic effusives of the Imir Formation and from the available radioisotope dates: for the Stolbovsky massif, U-Pb 449±3 and 451 Ma, K-Ar 469 Ma (Rublev et al., 1995).

Manifestations of fluorite and molybdenite have been established in the Stolbovsky massif. Syenites of the Stolbovskaya intrusion (Mokhovskoye deposit) are widely used as a facing stone for exterior and interior decoration of buildings in the city of Krasnoyarsk, for the manufacture of monuments, road curbs, stairs.

Syenites of the Stolbovsky complex. Mokhovskoye field

Early Devonian intrusions

Early Devonian intrusions are very diverse in composition and far from being fully studied. Dikes of diverse composition - from dolerites to granosyenite-porphyries and rhyolites are widely distributed among the deposits of the Lower and Middle Paleozoic.

Chernosopka complex (D1čr). It includes rocks of the petrotypical massif of Mount Chernaya Sopka and numerous dikes of trachydolerites and dolerites among the formations of the Karymov Formation of the Early Devonian. Mount Black Sopka is perfectly visible from many regions of Krasnoyarsk, being one of the highest peaks in the vicinity of Krasnoyarsk. The absolute height of the mountain is 691 m. It is located 8 km southeast of the city of Krasnoyarsk in the Berezovsky administrative region, in the junction of the northwestern tip of the Eastern Sayan with the Rybinsk depression

The Black Sopka massif was first described by Yu.A. Kuznetsov in 1932. He singled out the genetic series of its constituent rocks from trachydolerites to tinguaites, considering them to be differentiates of a single magma chamber and identifying them with those developed in the Kuzbass region, whose age is considered to be Permo-Carboniferous. The same point of view was shared by S.I. Makarov (1968). Later, the Early Devonian age of the intrusion was established (Parnachev et al., 2002).

Chernaya Sopka is a well-prepared subvolcanic intrusion in relief. In shape, this is a stock with a diameter of 1.2 - 1.5 km, having an annular structure. Its central part is composed of alkaline olivine dolerites and essexites, and the periphery is composed of tinguaites; moreover, the latter perform an annular fault that arose after the formation of the dolerite intrusion. This is evidenced by the results of observation of fissure tectonics, the presence of veins of alkaline syenite-porphyries in dolerites, and near-contact changes in the latter.

Kurums on the slope of Mount Chernaya Sopka

The stock of alkaline dolerites and essexites is inclined to the north, which is confirmed by the orientation of plagioclase phenocrysts in the porphyritic varieties of these rocks. This is also evidenced by the asymmetric location of alkaline dolerites and essexites relative to the top of Mount Chernaya Sopka. If in the south their distribution is limited by a horizontal line drawn through 680 m above sea level, then in the north - by a horizontal line drawn through 550 m. mountains Black Sopka.

Structures of alkaline dolerites and essexites are porphyritic, fine-, fine-, and medium-grained. The microstructure of the ground mass is gabbro-ophitic. The textures are massive, and in the marginal parts of the intrusion they are trachytoid, subparallel to the contacts. The composition of alkaline dolerites: plagioclase (andesine-labrador) - 58 - 66%; pyroxene - 11 - 15%; olivine (hortonolite f = 0.6 - 0.66) - 4 - 10%; analcime - 8 - 13%, biotite (red-brown, f = 0.4 - 0.5) - 1 - 4%; sometimes in the interstitium, individual grains of microperthite (anortoclase) are observed.

The color of tinguaites is greenish-gray, reddish-brown, pinkish-gray, they are characterized by platy separation. The structure is porphyritic, phenocrysts are represented by long-prismatic crystals of albite-oligoclase and nepheline. The microstructures are hypidiomorphic-granular and ocelar (eye), due to the formation of a "protective jacket" around nepheline grains from small needle-like crystals of aegirine and arfvedsonite.

The mineral composition of alkaline syenite porphyry 2 phases: porphyritic phenocrysts (up to 30%) up to 6 - 8 mm in size are represented by tabular phenocrysts of K-Na feldspar, less often - dark green aegirine-augite (3 - 4 mm) and isometric segregations of nepheline ( 2 - 3 mm). The groundmass consists of arcuate subparallel microlites of intensely pelitized and limonitized alkali feldspar, between which small xenomorphic aegirine-augite grains are “squeezed”. The sites are composed of an aggregate of fresh lamellar albite. Nepheline-containing and feldspathoid-containing syenite porphyries: albite, K-feldspar, spreusteinized nepheline (or analcime) - up to 10 - 15%, aegirine and arfvedsonite - up to 10 - 15%, zeolites. Often, nepheline grains are armored by prismatic grains of alkaline amphibole and needle-like tangled fibrous aggregates of aegirine. Accessory minerals: titanomagnetite, fluorapatite, pyrite, pyrrhotite. Fluorite veinlets are sometimes observed in the rocks of the massif.

Nepheline-feldspar rocks can be promising as a decorative facing material. The age of the Black Sopka massif is Early Devonian, which is confirmed both by its comagmaticity to trachydolerites of the Early Devonian Karymov Formation, and by the determination of the radioisotope age of rocks by the Ar-Ar method - 402 - 406 million years.

Dikes of basic composition (dolerites, trachydolerites), also attributed to the Chernosopkinsky complex, apparently, are derivatives of the Early Devonian magmatism of increased alkalinity, which manifested itself within the Rybinsk depression, and comagmates of effusive rocks of the Karymov Formation.

These dikes are predominantly developed in the southeastern part of the area. Moreover, dikes of trachydolerites are often found directly among the formations of the Karymov Formation. Their morphology is varied. Length - from 200 - 250 to 2500 m. The prevailing strike is northwestern, less often - northeast. The dolerites and trachydolerites that make up the dikes are fresh in appearance, dark gray and black in color, and most often have a porphyritic structure with a fine-grained groundmass. The porphyritic phenocrysts are dominated by basic plagioclase (labradorite), olivine, and clinopyroxene. The groundmass contains basic plagioclases, pyroxenes, olivine, and sometimes biotite, magnetite, and apatite. Often, the rocks of the complex are enriched in finely dispersed magnetite and, therefore, are characterized by increased magnetite.

5.3.. TECTONICS

In the composition of the geological structure of the region of the city of Krasnoyarsk, three structural floors are clearly distinguished. The lower, folded structural stage is composed of Late Precambrian and Lower-Middle Cambrian formations. The middle, transitional structural, forming superimposed depressions, is filled with volcanic and sedimentary rocks of the Middle-Upper Ordovician, Devonian and Lower Carboniferous. Finally, the upper, platform structural stage is represented by gently dipping Mesozoic deposits.

The lower structural stage (RF3 - €2) is characterized by a complex dislocation of its constituent rocks. They were formed under conditions of an open oceanic basin and an active continental margin of the Pacific type (marginal sea environment). For the most part, they are crumpled into tense folds, mostly linear, and broken by numerous faults. The floor consists of two structural stages - Upper Riphean and Vendian-Middle Cambrian.

The Upper Riphean structural stage is represented by formations of alpine-type ultrabasites (Akshepa complex), metapsammitic-siliceous-carbonaceous-schist with elements of carbonate (Urmanskaya suite), metacarbonate with elements of carbonaceous-siliceous (Manskaya suite) and metapicrobasalt-metabasalt-metatrachybasalt (Bakhtinskaya suite).

On the territory under consideration, the formations of this structural stage are mainly developed in the form of tectonic wedges within the Laletinsko-Ustbazaikhskaya fault zone. The formations of the alpine-type hyperbasite formation, in addition, are found along other subvertical faults of the northeast strike, forming lenticular protrusions. The relationship of the rocks that make up this structural stage with the formations of the Vendian-Middle Cambrian structural stage in the vicinity of the city of Krasnoyarsk is exclusively tectonic. The occurrence of Vendian deposits on the rocks of the Upper Riphean Kuvai Series with erosion and angular unconformity, on which the assignment of these formations to different structural stages is based, is established far beyond the territory under consideration.

Tectonic scheme of the environs of the city of Krasnoyarsk. Compiled by G.V. Mironyuk based on the materials of E.I. Berzona et al. (2001) and L.K. Kachevsky et al. (2009):

Altai-Sayan folded region: I - Krasnoyarsk uplift: 1 - Kachinsko-Listvenskaya volcanogenic depression: 1 a - Malolistvenskaya syncline; 1 b - Karaulninskaya syncline; 1 c - Shchebzavodskaya syncline; 1 g - Kachinsky horst. 2 - Derbinsky anticlinorium (Kuluk block): 2 a - Sliznevskaya brachysyncline; 2 b - Malosliznevskaya syncline; 2c - Namurt syncline; 2 d - Namurt anticline. II - Rybinsk depression: 3 - Krasnoyarsk monocline; 4 - Balai synclinal zone: 4 a - Zhernovskaya synclinal; 4 b - Sorokinskaya anticline.

West Siberian plate: III - Chulym-Yenisei trough. Yenisei depression: 5 a - Areysko-Shilinskiy swell; 5 b - Badalyk trough; 5 in - Esaulovskaya trough.

Intrusive and protrusive massifs: M1 - Listvensky; M2 - Shumikhinsky; M3 - Kulyuk; M4 - Stolbovsky; M5 - Abataksky; M6 - Sliznevsky. Carbonate massifs: K1 - Torgashinsky reef.

Faults and their numbers: P1 - Kansk-Agulsky (Iysko-Kansky); P2 - Batoysky; P3 - Krolsky; P4 - Sliznevsky; P5 - Sosnovsky

As a specific feature of the rocks of the Upper Riphean structural stage, it should be noted that they, in their main part, underwent weak regional metamorphism, the level of which corresponds to the very bottom of the greenschist facies,

The Vendian-Middle Cambrian structural stage is composed exclusively of sedimentary rocks, the accumulation of which is generally characteristic of the environments of marginal seas. Carbonate formations predominate here (limestone-dolomite, silty-limestone, limestone reef); there are also deposits of a flysch formation (Tyubilskaya suite).

The formations of this stage compose the main volume of formations of the lower structural stage in the immediate vicinity of the city of Krasnoyarsk. Sedimentary rocks of the stage are crumpled over vast areas into tense linear folds, often overturned, broken by numerous discontinuous faults of a reverse-thrust character. As a result, there are numerous cases of repeated summation of the same section fragments. Most typically observed in many areas is the subsidence of the axes of overturned folds and fault faults at medium (30-50°) angles in the WSW direction, which corresponds to thrust movements from the SW to the NE. Folds and discontinuities of such orientation can be observed southwest of Akademgorodok, along the descent along the Monastyrskaya road, and in the mouth part of the Kaltat river. The largest folded structure, composed of formations of the considered substage, is the Bolshesliznevskaya syncline located on the right bank of the Yenisei. The axis of this syncline is oriented submeridional. Its core is filled with carbonate rocks of the Ovsyankovskaya suite, and its wings - with terrigenous deposits of the Tyubilskaya suite.

The Torgashinsky structural block, located on the right bank of the Bazaikha River, stands out especially in terms of the nature of the occurrence of the Cambrian deposits. Tense linear folds and manifestations of thrust tectonics are not typical here. Here the rocks are collected in a series of gently undulating folds, with dip angles of 25 - 60o. Often these are monoclinally dipping weakly undulating layers, complicated by flexural bends. It can be assumed that this block in the epoch of folding played the role of an autochthon, in relation to which the other blocks of the lower structural stage were subjected to thrust displacements.

The middle structural stage (O2-3 - C1) is represented by sedimentary and volcanogenic formations of the Ordovician and Middle Paleozoic, filling separate depressions, with a pronounced structural unconformity superimposed on the complexly deformed folded complex of the lower structural stage. The formation of these depressions proceeded on a young crust of the continental type in the setting of the rear part of the active continental margin. Within its framework, two substages can be distinguished, characterized by the similarity of tectonic structures and, in part, geological formations, but corresponding to two different stages of tectonic activation - Middle Upper Ordovician and Devonian-Lower Carboniferous.

Middle-Upper Ordovician substage (O2-3). The formations of this sub-stage are represented exclusively by igneous rocks - volcanic rocks of the trachybasalt-trachyte-trachyrhyolite formation (attributed to the Imir suite or to the Divnogorsk sequence (O2-3). They fill the Kachinsko-Shumikhinsky volcano-tectonic depression, located mainly on the left bank of the Yenisei west of the city of Krasnoyarsk. This a gentle depression, in the modern cut, stretching for about 50 km in the latitudinal direction (from the city of Krasnoyarsk to the city of Divnogorsk and to the west), up to 30 km wide Lava flows and interlayers of tuffs that fulfill the depression gently (at angles up to 30 - 35 °) submerge from the edges depressions in a northerly direction, where they are unconformably overlain by younger deposits (Devonian or Jurassic).The same stage of tectonic development is associated with the formation of large laccolith-like intrusions of the syenite-granosyenite formation (Stolbovka complex), developed partly within the Kachinsko-Shumikhinsky depression itself, partly - in the structures of its fold this frame (among the formations of the lower structural floor).

Devonian-Lower Carboniferous substage (D1 - C1). Its rocks fill the Rybinsk depression, which opens from the city of Krasnoyarsk to the east and southeast. The Lower Devonian formations of this substage are represented by a combination of molasse and trachybasalt-trachyte-trachyrhyolite formations, which together form the Karymov Formation. The overlying deposits are predominantly represented by formations of a continental terrigenous red formation with elements of a carbonate, as well as a terrigenous-telepyroclastic formation (the Krasnogoryevskaya suite of the Lower Carboniferous). Several structural stages are distinguished in the structure of the substage: Lower Devonian (Karymov Formation), Middle Upper Devonian (Pavlovskaya and Kungusskaya Formations), and Lower Carboniferous (Charginskaya and Krasnogoryevskaya Formations). The boundaries between the structural stages are well-defined erosion surfaces, which are also associated with angular unconformities.

The main structural elements of this sublevel near the city of Krasnoyarsk are the Krasnoyarsk monocline and the Zhernovskaya syncline. The Krasnoyarsk monocline extends from the northwestern suburbs of the city in a southeasterly direction. Within its limits, there is a steady monoclinal dip of Devonian and Carboniferous deposits in the northeast direction at angles up to 20°. Zhernovskaya (Berezovskaya syncline) replaces the Krasnoyarsk monocline in the SE direction. This is a brachyform fold located in the Berezovka river valley near the Zykovo station and the Petryashino platform. It is composed of rocks of various units of the Karymov Formation. The axis of the fold is oriented submeridian; the hinge is gently immersed in the south direction. The dip of the seams in the southwestern flank is 15 - 30°, and 30 - 55° - in the northeast.

The upper structural stage (J) in the area under consideration is entirely formed by deposits of the Jurassic system. They belong to the coal-bearing limnic formation and fill the system of depressions of the Kansko-Achinsk brown coal basin, stretching as a sublatitudinal strip along the northern periphery of the Altai-Sayan folded region. The formations of this stage lie with a sharp structural unconformity on all underlying deposits. In the marginal parts of the depressions, their adjoining to more ancient formations is sometimes observed. A very gentle occurrence is characteristic - the angles of incidence usually do not exceed 5 °. Only in the marginal parts, near faults, and in rare flexural kinks, they can increase to a few tens of degrees.

The Jurassic deposits of the region of the city of Krasnoyarsk belong to one of the depressions of the Kansk-Achinsk basin - the Chulym-Yenisei. Within its boundaries, on the territory of the city and its environs, two gentle troughs are distinguished - Badalykskaya and Esaulovskaya, as well as the meridionally oriented Areysko-Shili swell, which limits the Badalykskaya trough from the west.

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An excerpt characterizing Bazaikha (river)

Arriving home, Pierre gave an order to his coachman Yevstafyevich, who knew everything, who knew everything, known throughout Moscow, that he was going to Mozhaisk at night to the army and that his riding horses were sent there. All this could not be done on the same day, and therefore, according to Yevstafyevich's idea, Pierre had to postpone his departure until another day in order to give time for the set-ups to leave for the road.
On the 24th it cleared up after bad weather, and on that day after dinner Pierre left Moscow. At night, changing horses in Perkhushkovo, Pierre learned that there had been a big battle that evening. It was said that here, in Perkhushkovo, the ground trembled from the shots. To Pierre's questions about who won, no one could give him an answer. (It was a battle on the 24th at Shevardin.) At dawn, Pierre drove up to Mozhaisk.
All the houses of Mozhaisk were occupied by the troops, and at the inn, where Pierre was met by his coachman and coachman, there was no room in the upper rooms: everything was full of officers.
In Mozhaisk and beyond Mozhaisk, troops stood and marched everywhere. Cossacks, foot soldiers, mounted soldiers, wagons, boxes, cannons could be seen from all sides. Pierre was in a hurry to move forward as soon as possible, and the farther he drove away from Moscow and the deeper he plunged into this sea of \u200b\u200btroops, the more he was seized by the anxiety of anxiety and a new joyful feeling he had not yet experienced. It was a feeling similar to the one he experienced in the Sloboda Palace during the arrival of the sovereign - a feeling of the need to do something and sacrifice something. He now experienced a pleasant feeling of consciousness that everything that makes up the happiness of people, the conveniences of life, wealth, even life itself, is nonsense, which is pleasant to cast aside in comparison with something ... With what, Pierre could not give himself an account, and indeed he tried to make clear to himself for whom and for what he finds a special charm to sacrifice everything. He was not interested in what he wanted to sacrifice for, but the very sacrifice constituted for him a new joyful feeling.

On the 24th there was a battle at the Shevardinsky redoubt, on the 25th not a single shot was fired from either side, on the 26th the Battle of Borodino took place.
Why and how were the battles at Shevardin and Borodino given and accepted? Why was the Battle of Borodino given? Neither for the French nor for the Russians it made the slightest sense. The immediate result was and should have been - for the Russians, that we approached the death of Moscow (which we feared most in the world), and for the French, that they approached the death of the entire army (which they also feared most of all in the world) . This result was obvious at the same time, but meanwhile Napoleon gave, and Kutuzov accepted this battle.
If the commanders were guided by reasonable reasons, it seemed, as it should have been clear to Napoleon, that, having gone two thousand miles and accepted the battle with the probable accident of losing a quarter of the army, he was going to certain death; and it should have seemed just as clear to Kutuzov that, accepting the battle and also risking losing a quarter of the army, he was probably losing Moscow. For Kutuzov it was mathematically clear, as it is clear that if I have less than one checker in checkers and I will change, I will probably lose and therefore should not change.
When the opponent has sixteen checkers, and I have fourteen, then I am only one-eighth weaker than him; and when I exchange thirteen checkers, he will be three times stronger than me.

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Nearest bus stations, railway stations, bus stops.

Description of the river

Tourism

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Literature

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Notes

Description of the river

Tourism

Write a review on the article "Bazaikha (river)"

Literature

Links

Notes

An excerpt characterizing Bazaikha (river)

An excerpt characterizing Bazaikha (river)

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