Leonid Petrenko. Krasnoyarsk Madonna. Geological essay - Museum of Geology of Central Siberia Bazaikha River water flow by season hydrograph

6. Up the Moscow River The upper reaches of the Moscow River are extremely beautiful. Back in the 16th century. Here, individual estates began to appear, which still preserved ancient monuments, such as the villages of Khoroshevo and Trinity-Lykovo, now included within the borders of the capital. Subsequently, the number of estates and

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

From Magansk along Bazaikha During the winter - only occasionally, and by spring more or less systematically - independent, unorganized crossings along Bazaikha from Magansk to the final stop of the thirty-ninth bus route are made. This transition

Russia, Russia

Description of the river

Average annual water flow - - 5.0 m³/s. The largest tributaries: Namurt, Kaltat, Dolgin, Zhistik and Korbik.

On the bank of the river, at the confluence with the Yenisei, the village of “Bazaikha” was founded in 1640. 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, residents of Krasnoyarsk built their dachas on the banks of the river.

In 1931, near the mouth of the river in the village of Bazaikha, construction of a wood processing plant began, after which the village was included within the boundaries of Krasnoyarsk.

On the left bank of the Bazaikha, next to the Bolgashov Log, in the territory of the Stolby Nature Reserve, a marble quarry operated.

Tourism

The river is suitable for tourist rafting during spring floods. The tourist route of the second category of complexity began from the village of Erlykovka. Kayak competitions were held at the threshold of Abatak.

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Literature

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

Links

Notes

Excerpt characterizing Bazaikha (river)

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 of Shevardin and Borodino given and accepted? Why was the Battle of Borodino fought? It didn’t make the slightest sense for either the French or the Russians. The immediate result was and should have been - for the Russians, that we were closer to the destruction of Moscow (which we feared most of all in the world), and for the French, that they were closer to the destruction of the entire army (which they also feared most of all in the world) . This result was immediately obvious, but meanwhile Napoleon gave and Kutuzov accepted this battle.
If the commanders had been guided by reasonable reasons, it seemed, how clear it should have been for Napoleon that, having gone two thousand miles and accepting a battle with the probable chance of losing a quarter of the army, he was heading for certain death; and it should have seemed just as clear to Kutuzov that by accepting the battle and also risking losing a quarter of the army, he was probably losing Moscow. For Kutuzov, this was mathematically clear, just as it is clear that if I have less than one checker in checkers and I change, I will probably lose and therefore should not change.
When the enemy 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.

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 (R 3)

Upper Riphean deposits (430-600 million years) are developed in the basins of the Mana and Bazaikha rivers. According to lithological features, three formations are distinguished in the section: Urman, Mansk and Bakhtin. Contacts with older sediments are universally tectonic; the relationships between the retinues within it are consistent.

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 marbleized limestones, and rarely dolomites. The rocks are often sulfidized and collected in small isoclinal folds. Thickness more than 200 m.

The Manskaya Formation (R3mn) is composed of dark gray and black crystalline limestones, platy, sometimes lumpy, with interlayers of siliceous and phyllitic clayey shales (up to 12 m thick), less commonly metasandstones. Thickness over 600 m.

In the Krasnoyarsk region, the rocks of the Urman and Mansk formations 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 Mansk formation in contact with the Stolbovsky massif are marbleized.

The Bakhtin Formation (R3bh) is distributed in the vicinity of the city of Krasnoyarsk to a limited extent in the southern and southwestern parts of the area (in the area of ​​the northern contact of the Stolbovsky massif near the observation deck of the Stolby Nature Reserve above the Bobrovy Log). Here it is developed exclusively in tectonic wedges, and the rocks composing it are hornfelsed under the influence of the Stolbovo intrusion. In adjacent areas, the Bakhtin Formation conformably overlies the Man Formation.

The Bakhtin Formation is composed predominantly of metabasalts. In the lower part of the formation, among the volcanic rocks, there are interlayers of lithoclastic and crystalloclastic tuffs of basic composition, chlorite-sericite schists and black siliceous thin-platy shales, and less commonly - tuff conglomerates.

The rocks of the Bakhtin Formation are characterized by a green, greenish-gray or dark green color, they are often foliated and have intense greenstone alterations. 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, basaltic lava breccias, basaltic andesites and their tuffs with rare interlayers of marbled limestones, dolomites and siliceous shales.

The thickness of the formation reaches 2000 m.

Vendian system (V)

The Tyubil 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 Sobakina River), the rocks of the formation form an extended strip of latitudinal strike and are folded into complex folds.

Artificial outcrop of sandstones of the Tyubil formation near the road near the village of Udachny. Stop Yuzhnaya

Calcite veins in sandstones

Greenish-gray color of sandstone on fresh chips

On the right bank of the Yenisei they participate in the construction of the Bolshesliznevskaya syncline. Some fields are known from the Bazaikha River, on the left bank of which the formation rocks are hornfelsed under the influence of the Stolbovsky massif.

Kaltat fold. The right bank of the Yenisei, not far from the mouth of the Kaltat River

The formation is composed of polymictic, micaceous, calcareous sandstones, siltstones, shales, gravelites 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-breaking ripple marks and traces of raindrops. Sericite is often developed along 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 formation are often significantly foliated. So, in a large artificial outcrop on the right bank of the river. Bazaikha (near its mouth) there are intense disjunctive dislocations of the formation sediments and fracturing in several directions. general power divisions 950 - 1100 m.

The Tyubil Formation is conformably overlain by the Ovsyankovsky Formation. The contacts with the underlying sediments are tectonic.

In the upper part of the formation, small tubular skeletal remains were found. Similar fossils are found from the Vendian. The age of the formation is assumed to be Late Vendian (570-555 million years).

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

The Ovsyankovsky formation is composed of dolomites, dolomitic limestones, calcareous dolomites, dolomite breccias, rarely limestones, and quartzites are found in areas.

Kurumnik near the village of Ovsyanka

Dolomite rocks vary 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 the abundant microphytoliths, especially oncolites and vesicular catagraphs. During weathering, the internal parts of the nodules of microphytoliths are leached, and empty shells are preserved from them, which is why the rock takes on a porous appearance.

In some areas, the rock formations are folded into complex folds and broken through by numerous disjuncts; they are often heavily recrystallized or silicified. The thickness of the formation is estimated at 1000 - 1100 m.

The formation’s contacts 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 conformable occurrence on the Tyubil Formation is established.

Paleozoic erathema (PZ)

Cambrian system (€)

Lower section (€1)

In the vicinity of Krasnoyarsk, the Ungut and Torgashin formations are classified as lower Cambrian.

Ungut suite (€1un). I.P. singled out 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, types of the formation section are identified, for which its local names are adopted.

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 here are exposed in 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 dolomite interlayers in the lower part of the section and a characteristic horizon of oncolite limestones with “floating pebbles” in the middle. Thickness 800 - 920 m. Overlying deposits are present only at one point - along the Karaulnaya River - and are represented by a layer of limestone conglomerates of problematic age (Cambrian?).

Artificial exposure. Ungut Formation, Kaltat type of section. Interbedded limestones and siltstones

Swirling turbidity currents

Dike

The Kaltat type of section of the Ungut Formation is developed along the right bank of the Bazaikha River, where outcrops of its rocks extend from Mount Krasny Kamen eastward at a distance of almost 12 km. Here the formation is composed predominantly of dark limestones, greenish-gray and variegated siltstones, marls and rare dolomites. The rocks are characterized by horizontal layering, smooth bedding planes and abundant terrigenous admixture (Zadorozhnaya, 1974). The apparent thickness of the sediments in the type section opposite the mouth of the Kaltat River is 263 m. The relationships of the formation in the Bazaikha River basin with the underlying sediments are universally tectonic, with the overlying Torgashinsky formation being concordant.

Many organic remains were found in the rocks of the Ungut Formation. In the Karaulinsky type of section this is, first of all, small-shelled fauna, the remains of ancient skeletal organisms (“smallshellyfossils” or SSF). Among them, angustiocraids, chiolites, gastropods, tommotiids, and crustaceans of the Tommotian stage were identified (Sosnovskaya, Shurinova, 2003). The fossils place the age of their host sediments as Early Cambrian (Tommotian).

The Torgashinsky formation (€1tr) was identified by V. Zlatkovsky in 1885. The stratotype is the section of the Torgashinsky ridge formation. Here its deposits, often creating high rocky outcrops (Mount Kommunist, Mount Pioneer, etc.), occupy a significant area and make up both the axial part of the ridge and its slopes. Deposits of the formation are also known on the left side of the Bazaikha River. In contact with the rocks of the Stolbovo intrusion, they were transformed into marble.

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 its good exposure and the presence of numerous organic remains, it was repeatedly visited by geologists who carried out geological surveying and thematic work in this area. The main volume of the formation is composed of gray and light gray massive organogenic limestones. Layered limestones play a subordinate role. In the upper part of the section there are interlayers of dolomite.

Calcite crystal

Calcite

At the base of the section there is a member of unique composition, which has a local name - Bazaikh. It is composed of purple, light pink and gray calcareous gravelites, sandstones, coarse breccias and light pink limestones. Angular fragments of algal limestones are abundant in terrigenous rocks. The cement is carbonate with an abundant admixture of iron hydroxides, which is responsible for the variegated color. Below the mouth of Kaltat, among the variegated sediments, there is a thick layer of dark gray thin-slab limestones and marls with clayey and dolomite layers. In addition, the member contains single algal bioherms that form isolated rocky outcrops in the relief. In general, the rocks of the Bazaikh Member are characterized by coarse cross-bedding, wave ripple marks, abundant erosion surfaces, and poor rounding and sorting of clastic material. Outcrops of the member stretch along the lower part of the southwestern slope of the Torgashinsky ridge, where its variegated rocks are clearly visible on Mount Krasny Kamen. On its northern slope, rock members are known along the Panikovka stream and at the exit of the Cheremukhovsky log to the terrace of the Yenisei River. Its thickness is up to 250 m.

According to N.M. Zadorozhnaya (1974), the limestones of the Torgashinskaya 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 Torgashinskaya Formation is characterized very a large number genera and species of archaeocyaths and other groups of fossil organisms represented by complexes of various horizons of the Atdabanian, Botomian and Toyonian stages of the Lower Cambrian. It lies conformably on the underlying sediments of the Ungut (Kaltat) formation. But in certain areas of the right bank of the Bazaikha River, their contact is complicated by a series of dikes of basic composition. In the field of dike development, layered carbonate rocks are intensively crushed into folds with dip angles on the wings 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 ridge, the formations of the Torgashinsky formation are conformably overlain by the Middle Cambrian Sheshmovsky formation.

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

The limestones of the formation are also known in the area of ​​the Krasnoyarsk reservoir, where high picturesque cliffs form along the sides of Biryusa Bay.

Fold. Rock Red (Creepy), southern slope of the Torgashinsky ridge

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

Middle section (€2)

The department includes carbonate deposits of the Sheshmovskaya Formation.

Shakhmatovskaya 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 ​​study practice, rock formations make up the northern slopes of the Torgashinsky ridge. The formation is represented by gray layered limestones, light dolomites and dolomitized limestones, and red siltstones. The latter are rare in the form of unconsolidated layers with a thickness of no more than 2-3 m. Due to the admixture of manganese, the carbonates of the formation often have a pink color. The thickness of the unit is less than 300 m.

In limestones, trilobites Olenoides convexusLerm., Erbiagranulosa, E.sibiricaLerm., Amgaspis cf.medius N.Tchern., A. sp., Gaphuraspissp., Kooteniellasp., Proasaphiscussp., ProshedinellaerbiensisSiv. and others, as well as algae EpiphytonfruticosumVol., RenalcisgranosusVol.

The relationships of the formation with the underlying Torgashin formation are consonant. The boundary is gradual in nature and is drawn conditionally along a member of limestones containing a reliable trilobite fauna of the lower part of the Middle Cambrian. Younger Devonian sediments occur unconformably or with tectonic contacts. The age of the formation is determined from the finds of trilobites by the Amga Age of the Middle Cambrian.

Ordovician system (O)

Middle-upper sections (O2-3)

Imir Formation (O2-3im). Volcanogenic rocks of the formation, together with subvolcanic formations, are part of the Imir volcanic complex and are widespread within the Kachin-Shumikha depression, which is located in the northwestern frame of the folded system of the Eastern Sayan. This structure extends in the latitudinal direction 50 km 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), 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 volcanogenic rocks of 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, stretching sublatitudinally to the west from Mount Nikolaevskaya (First) Sopka - M.L. Makhlaev and O.Yu. Perfilova (Makhlaev et al., 2007; Perfilova, 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 volcanic rocks of the northern part of the depression and subvolcanic bodies from the Divnogorsk section, isotope dating that was considered quite reliable was obtained, according to which the age of the complex is Middle-Late Ordovician.

Nikolaevskaya (First) Sopka

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

In general, the lower part of the formation section is dominated by moderately alkaline basaltoids, while the upper part is dominated by volcanic rocks of medium and moderately acidic composition (lavas and tuffs of trachytes, trachydacites, trachyrhyodacites). The volcanogenic section is characterized by a high thickness. Based on 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.

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

Nizhneimir subformation (O2-3im1) in the basins of the Gladkaya and Krutaya Kacha and Bol rivers. Minanjul is composed of lava flows and covers of olivine, olivine-augite, augite-plagioclase and plagioclase trachybasalts, trachyandesite-basalts, less commonly trachyandesites with a thickness of 1 - 5 to 30 - 40 m. The rocks of the central parts of the flows are characterized by a high degree of crystallization, microdolerite structure and almost complete absence glassy base. Towards the top and bottom of the flow, the glass content increases. In the marginal parts of the flows, the volcanics have mainly a pilotaxitic structure. The texture of rocks in the roof of streams is usually amygdaloid. There are a few interlayers of litho-, vitro- and crystalloclastic psammitic, psephitic and psammopelitic tuffs, tuffaceous sandstones, tuffaceous siltstones, and volcanomictic sandstones. In the lower part of the formation, interlayers of tuffaceous gravestones and tuffaceous conglomerates are noted, which contain fragments of limestones of the Torgashinsky formation and dolomites, probably of the Ovsyankovsky formation. Cement is basal, basal-pore carbonate pelitic with an admixture of chlorite, clayey-carbonate, carbonate, zeolite 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 commonly 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 et al. on the replacement of essentially basaltoid volcanics by rocks of intermediate and felsic composition. Tuffs of mixed composition often occur here at the base of the upper subformation.

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 commonly trachyrhyolites, as well as their tuffs. The rocks of the upper subformation are mainly colored in various shades of red and brown. Porphyry 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 acidic rocks (trachydacites, trachyrhyodacites), which are absent in the eastern part of the depression. Trachytes, on the contrary, are not typical for this part. The total thickness of the effusive section here is somewhat greater than in the eastern part - no less than 2800 m. Thus, the volcanogenic sequence is characterized by lateral discontinuity, sharp fluctuations in the thickness of individual bodies along the 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 volcanic rocks was determined by the Rb-Sr method - 442 ± 2 million years.

A number of geologists dispute the attribution of the volcanogenic formations of the Kachinsko-Shumikhinsky depression to the Imir formation and propose to distinguish them under the local name Divnogorsk strata with the same age O2-3. (Kruk et al., 2002; Makhlaev et al., 2007,2008; Perfilova, Makhlaev, 2010).

Objects with uranium mineralization of the uranium-molybdenum formation and numerous occurrences of fluorite on both banks of the Krasnoyarsk reservoir are paragenetically associated with the rocks of the Imir Formation. Volcanic rocks (trachytes, trachydacites) meet the requirements of industry in their physical and mechanical properties and have been widely used for filling railway embankments and highways. Some varieties of coarse porphyry volcanogenic rocks of the Imir Formation are quite decorative and can be used as facing stone.

Devonian system (D)

Deposits of the Devonian system are widely developed in Krasnoyarsk and its environs. They form the Rybinsk depression, which extends from the northwestern suburbs of Krasnoyarsk in the eastern and southeastern directions, and are represented by all three departments of the Devonian system.

Lower section (D1)

Karymovskaya formation (D1kr). The Karymovskaya formation begins the section of Devonian deposits of the Rybinsk depression. Its deposits stretch in a strip along the northeastern foot of the Torgashinsky ridge from the village. Torgashino on the southern outskirts of the city of Krasnoyarsk in the direction of the Black Sopka mountain and Petryashino station and further in a south-east direction.

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

Imprints of rhyniophytes

In general, the lower part of the section of the Nizhnekarymovskaya subformation (Assafievskaya formation) is dominated by polymict sandstones of yellow, pinkish-gray and red color, with parallel or directional cross-bedding. At various levels they contain layers and lenses of polymictic gravelstones and conglomerates or layers of green or red siltstones and mudstones. The thickness of the lower part of the subformation section is more than 100 m.

Higher up the section lies a coarse clastic member. Its section is represented by interlayering of small-, medium- and large-pebble (sometimes with an admixture of boulder material) conglomerates. Interlayers and lenses of gravelites and sandstones are occasionally encountered. Polymictic conglomerates; The pebbles are composed of various igneous and sedimentary rocks: syenites, granite porphyries, diorites, gabbroids, volcanic rocks of various compositions, limestones, etc. The total thickness of the Nizhnekarymovskaya subformation (Assafievskaya formation) is at least 400 m.

Deposits of the Nizhnekarymovskaya subformation can be observed in numerous small outcrops along the foot of the Torgashinsky ridge (in the area of ​​​​the villages of Torgashino and Vodnikov).

Higher up, the section of the Karymovskaya subformation increases significantly with volcanogenic formations, sections of which are exposed on the sides of the Berezovka River in the area of ​​Petryashino station. Here, the lava formations of moderately alkaline composition, ranging from basaltoids of high alkalinity to trachyrhyodacites, are irregularly interlayered, often composing pinch-out and lens-shaped bodies. Interlayers of red sandstones and polymictic conglomerates play a subordinate role. 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 basalt

Almond 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 propteridophyte (reniophyte) flora. The largest is the Torgashinskoye location, discovered in the 1930s. and studied in detail by the largest expert on propteridophyte flora A.R. Ananyev, widely known in world literature, which is located in the former quarry “Uval Promarteli”. Protohyeniajanovii, Prototaxitesforfarensis (KidstonetLang.), MinusiaantigmaTschirk., ZosterophyllummyretonianumPenh., DistichophytummucronatumMagdefrau, Sawdoniaornate (Daws) Hueber, Margophytongoldshmidtii (Halle) Zakh., PectinophytonbipectinatumAnan., Ptotobarinophy are identified here tonobrutscheviiAnan., Ienisseiphytonrudnevae (Peresv.) Anan., Drepanophycus spinaeformis Goepp., Platyphyllum fasciculatum Anan., Enigmophyton hoegii Anan., Broeggeria laxa Anan., Relliniia thomsonii (Daws.) Leclerc et Bon., in addition, remains of the racoscorpion Hugmilleria lata (?) Stormer were found. Unfortunately, this location is currently inaccessible for observation, as it was filled in during the construction of the ash sedimentation dam at the Krasnoyarsk Thermal Power Plant-2, despite the fact that it is listed as a protected natural monument.

Middle section (D2)

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

R. Kacha

"Red Yar" on Kach

Drokino hill

At the top of the Drokino hill

The Pavlovsk formation is composed exclusively of sedimentary rocks of terrigenous, partly carbonate composition: sandstones, siltstones, gravelites, conglomerates, marls and limestones. Based on lithological features (mostly the content of carbonate rocks), it is divided into 3 subformations.

Nizhnepavlovsk subformation (D2pv1). The deposits of the lower subformation make up most of the formation section and are represented by sandstones, conglomerates, siltstones, marls with rare lenses of limestones. 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 pack of sandstones, with an admixture of sand and gravel material and small pebbles of volcanic rocks. Carbonates containing interbeds and lenses are present. Above this lies a thick (up to 70 m) pack of conglomerates and sandstones with rare interlayers of sandy marl.

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

Higher up the section, sandy-conglomerate deposits with thin interlayers and lenses of marls again predominate. Small, weakly rounded pebbles are represented by siliceous rocks, syenites and volcanic rocks of basic composition.

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

The Middle Pavlovsk subformation (D2pv2) is a marker sequence and can be traced across a significant part of the Rybinsk depression. The lower boundary is drawn by the appearance in the formation section of limestone layers containing red chalcedony nodules. It is composed mainly of red-brown, less often greenish-gray marls, among which there are layers and lenses of limestone, sandstone 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 sharp, sometimes stepped and cuesta-like forms of relief.

Marking limestone horizon near the village of Kuznetsovo

Marking horizon of clastic limestones (calcarenites) on Pokrovskaya Mountain

3 km southeast of the village of Drokino, on the left bank of the Kachi 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 Srednepavlovskaya subformation is about 120 m.

The Upper Pavlovsk subformation (D2pv3) is close in lithological composition to the Lower Pavlovsk subformation and differs from it in a slightly larger number of limestone layers and the presence of mudstones. The section of the subformation is almost entirely exposed by a trench driven in the north-northeast direction from the chapel (the top of Mount Karaulnaya) for about 650 m. The composition of the sediments is dominated by marls, among which in the form of thin (from 0.2 to 2 m) lenses and interlayers sandstones and small pebble conglomerates occur. The thickness of the sediments of the upper subformation is up to 120 m.

The age of the Pavlovsk Formation is determined to be Middle Devonian based on the findings of flora imprints near the village of Drokino.

Upper Devonian (D3)

The Kunguska Formation (D3kn) is widespread in the Krasnoyarsk region. Its deposits extend to the southeast of the village. Solontsy through the territory of the Sovetsky 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 sediments of the formation were exposed by numerous wells during engineering-geological research at the beginning of the development of the Vzlyotka microdistrict.

The Kunguska formation conformably overlies the Pavlovskaya. Its lower boundary is drawn conventionally by the replacement of the marls of the upper part of the Pavlovsk formation by a unit of gravel-sandstone rocks containing interlayers of grayish-white sandstones. Higher up the section there is interlayering of brick-red, less often green-colored siltstones and marls, often sandy, with interlayers of sandstones, mudstones, gravestones, and limestones.

Interbedded sandstones, gravelites and siltstones
Kungusskaya formation near the village of Solontsy

Red-colored siltstones and gravelstones near the village of Solontsy

Gravelite

Gravelite with calcite crystals

Characteristic of the Kungus Formation are limestone conglomerates called “caviar” limestones. They consist of flat and round pebbles of limestone and marl ranging in diameter from 1 to 5 cm. The cement of limestone conglomerates is limestone-clayey material.

Buried wave-breaking niche

Buried Gully

Devonian takyrs

The upper part of the formation is eroded before the accumulation of overlying Carboniferous sediments. The thickness of the formation in the area of ​​the city of Krasnoyarsk is more than 300 m, in the adjacent parts of the Rybinsk depression it reaches 600 m.

From the lower horizons of the formation, a flora identified as Pseudoborniacf. ursineNath., and Archaeopterissp., Archaeopteriscf. fimbriataNath. etc. In greenish-gray sandstones from the middle part of the Kungus Formation, scales of armored fish, identified as Bothriolepiscf., were discovered. sibiricaObr., remains of armored fish, identified as Osteolepidae, were found in limestone conglomerates. All these finds determine that the formation belongs to the Upper Devonian.

Coal system (C)

Lower section (C1)

The Charga Formation (C1čr) lies with erosion on underlying Upper Devonian sediments. They are common on the right bank of the Yenisei at the eastern outskirts and in the adjacent part of the suburban area of ​​Krasnoyarsk. The best exposed rocks are the lower part of the Charga Formation section, 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 formation is not exposed, but a fragment of the lower part of the formation with a thickness of about 80 m is exposed. Sandstones and siltstones (mostly calcareous), less often gravestones and conglomerates, and sometimes limestones alternate rhythmically in the section. The latter often contain nodules and layers of orange flints. Sharp boundaries between lithological differences are characteristic; Wavy erosion surfaces are common. The thickness of the layers is variable, and there are cases of pinching out along the strike. Directional cross-bedding is widespread. Clastic varieties - calcarenites - are common among limestones. In the lower part of the section red colors predominate; above everything greater distribution acquire green flowers. The proportion of carbonate rocks also increases up the section.

The higher part of the formation section is represented by interlayering of greenish marls, brick-red siltstones and limestone conglomerates. The uppermost part is dominated by limestone conglomerates and limestones with chalcedony inclusions. Among them there are interlayers of calcareous sandstones, siltstones and mudstones. The color is variegated with irregular alternation of greenish-gray and red varieties. Often there is replacement along the strike of limestone conglomerates by greenish-gray sandstones with a large amount of fragments of quartz, chalcedony and cake-like fragments of marl, as well as fine-grained sandstones - siltstones.

The thickness of the formation is more than 450 m.

In the interlayer of green-colored siltstones from the upper part of the formation section, along the Voznesenskoye - Lopatino road, numerous imprints of plants were discovered: AsterocalamitesscrobikulatosSchoth. and HeleniellatheodoriZal., defining the age of the deposits as Early Carboniferous (Tournaisian).

The Krasnogoryevskaya formation (C1kr) is developed in the vicinity of Krasnoyarsk in a narrow sublatitudinal strip, 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, gravelites
Krasnogoryevskaya suite near the village of Voznesenka

Layer of green siltstones and mudstones

The formation is represented by interbedded pinkish-yellow, yellowish-green sandstones with subordinate layers of green siltstones and mudstones. There are layers of acidic 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 sandstones of quartz-feldspathic composition are exposed here. Sandstones are often calcareous and in areas enriched in calcium phosphate. They often contain pellet-shaped fragments of bluish-green mudstones and well-preserved remains of large-trunked lepidodendron flora. Higher up the section they are replaced by greenish coarse-grained quartz-feldspathic sandstones. The upper part of the formation is composed of fine- and medium-grained greenish-gray and greenish-yellow sandstones with interlayers of bluish-green mudstones. The thickness of the Krasnogoryevskaya formation is more than 300 m.

Lepidodendron trunk imprint

Lepidodendron flora imprint

Based on the remains of the lepidodendron flora PorodendroncristatumChachl., PorodendronplicatumChachl., Knorriasp. and others. The age of the formation is determined as Early Carboniferous.

Mesozoic erathema (MZ)

Jurassic system (J)

Jurassic deposits are widespread in the northern and eastern parts of the city of Krasnoyarsk and in the surrounding area. Sediments of this level are represented by continental coal-bearing formation, the most important feature of which is its rhythmic structure. Elementary sedimentation cycles usually begin with sandstones, less often gravelites or conglomerates. Up the section, sandstones give way to siltstones and mudstones. And finally, these cycles are often crowned with layers and layers of brown coal. All Jurassic deposits in the region of the city of Krasnoyarsk belong to the eastern zone of the Chulym-Yenisei depression. Jurassic deposits of the city and its immediate surroundings belong to two sections of this system - lower and middle. The Lower Jurassic is represented by the Makarovskaya and Ilanskaya formations, the Middle Jurassic by the Itatskaya formation, and the overlying deposits are developed at a considerable distance from the city.

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

Lower section (J1)

Makarovskaya 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 lie unconformably on Paleozoic rocks and are represented by conglomerates, sandstones, siltstones, mudstones with several thin layers of brown coal. 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 formation lie yellowish-gray weakly cemented conglomerates with poorly sorted but well-rounded pebbles of siliceous and volcanic rocks, less commonly granites, quartzite-like 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 areal weathering of Corfu. The thickness of the conglomerates is 30 m; their outcrops are also found along the Sukhoi Stream.

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

In the deposits of the Makarovskaya Formation, imprints of plants CladophlebiswhitbiensennueHeer, Elatocladusmanchurica (Lokojame) Labe were found. From them, representative sporopyllen complexes were identified, in which there is pollen of ginkgo, bennetite, conifers, and fern spores, characterizing the age of the formation in the Sinemurian and Pliensbachian stages of the Lower Jurassic.

Ilan Formation (J1il). The sediments of the formation extend in a narrow strip from the eastern outskirts of the city of Krasnoyarsk to the village of Barkhatovo. Here the Ilan Formation lies with erosion on different horizons of the Makarov Formation and on the underlying Paleozoic deposits. Unlike underlying and overlying sediments, it does not contain industrial coal seams. There are only thin (up to 1.6 m) layers of coal-bearing rocks, less often brown coals. The lower boundary of the formation is drawn along the roof of carbonaceous rocks occurring in the upper part of the Makarovskaya Formation, or by the change of predominantly sandy fractions of the Makarovskaya Formation by interbedding 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. Gray-green tones of color are characteristic.

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

Middle section (J2)

Itat Formation (J2it). Formations of the Ilan Formation make up vast areas in the Krasnoyarsk region on the left bank of the Yenisei, within the Zelenaya Roshcha, Severny, Solnechny microdistricts, in the vicinity of KRAZ and the village of Peschanka. Its basal layers, with erosion, lie on various horizons of the Ilan Formation, and in the marginal parts of the Chulym-Yenisei depression - on more ancient deposits. 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, Khudonogovo. It is composed of rhythmically interbedded sandstones, siltstones, mudstones, carbonaceous siltstones and mudstones, with interlayers and lenses of conglomerates and gravelstones, and coal seams.

The formation includes sandstones, siltstones, mudstones, carbonaceous siltstones and mudstones, interlayers and lenses of conglomerates, gravelstones, and coal seams. Based on the cyclical structure of the section, the formation is divided into three subformations, each of which begins with deposits of essentially sandy composition with interlayers and lenses of coarse clastic rocks, and ends with predominantly fine clastic (silty mudstone) rocks with layers and interlayers of brown coal. The deposits of the formation are characterized by representative sporopyllen 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. were found here. Numerous bivalves Unio, Acyrena, remains of fish Psendosurdinia, etc. are known. But this section is of greatest interest due to the presence of the most unique location in Russia of Jurassic insects Their remains were found in the upper part of the section of the Upper Itat subformation in several layers, which extend along strike over a considerable distance. Here are found very numerous and various forms- both aquatic (mayfly larvae, aquatic Temptus beetles, dragonflies, caddisflies, 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, and 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)

Sediments of the Quaternary system are almost universally developed in the vicinity of Krasnoyarsk. Natural deposits of various genetic types are widely represented here: alluvium, proluvium, eluvium, colluvium, colluvium, desertions, defluxions, limnium, polustrium, delupium, as well as man-made formations. Their age ranges from Eopleistocene to Holocene (modern). The basis for the age division of the Quaternary deposits of the region is the chronological sequence of the formation of the Yenisei terrace complex. Therefore, alluvial deposits composing the surfaces of terraces of different ages are most reliably dissected. The age of the terrace alluvium is determined by sporopyllen complexes, bone remains of mammals, and for the youngest - by Paleolithic tools. Sediments of other genetic types are compared with different levels of the terrace complex according to geomorphological characteristics. Those that are superimposed on the surfaces of terraces or associated with relief forms cut into them are considered to be younger.

In total, in the Krasnoyarsk region in the Yenisei valley, nine terraces of different hypsometric levels and, accordingly, age are distinguished. All of them, with the exception of the first one, have their own names. The first terrace is up to 9 m above the modern water line, the second (Ladeyskaya) is up to 15 m, the third (Krasnoyarsk) is up to 25 m, the fourth (Berezovskaya) is up to 35 m, the fifth (Lagernaya) is 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. The valleys of the main tributaries of the Yenisei (rivers Bazaikha, Kachi, Karaulnaya, etc.) are weakly terraced . Only in certain sections of their course are single remnants of terraces found, and a complete terrace complex, similar to the Yenisei one, is not developed anywhere. In vast watershed areas, where there is no possibility of geomorphological comparison with the terrace complex, Quaternary deposits of all genetic types are considered as belonging to an undivided Quaternary system.

The description of Quaternary deposits is given by genetic types.

Alluvial deposits were formed throughout the Eopleistocene to the present. The alluvium of the IX (Badalyk) and VIII (Khudonogovskaya) terraces belongs to the Eopleistocene. In the Krasnoyarsk region, terrace IX is 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 exposed by a quarry. Here, horizontally layered sands and pebbles of polymictic composition, cemented by ferruginous coarse-grained sand, lie on the variegated clays of the weathering crust with erosion. The upper part of the sequence near the village of Badalyk consists of pebble, which contains a lot of weathered rocks cemented by ferruginous clay sand, and gray-brown loam with lenses of sand (Berzon et al., 2001). The total thickness is up to 9 m. The VIII terrace above the floodplain is most pronounced on the left bank, in the area of ​​the State University and the biathlon shooting range on the western outskirts of the city. Here, on the sides of the ravines, one can observe outcrops of brown calcareous sandy loam 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 on terrace VIII is up to 25 m.

The alluvium of the VII (Torgashinskaya) 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 Student Town, and on the right bank it stretches along a significant part of the northern slope of the Torgashinsky ridge 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, west of Akademgorodok. Here, dense loams are revealed, grayish-brown in color, with thin parallel layering (with unbroken interlayers of dark gray color), calcareous; interbedded with sandy loams and overlain by them. The lower parts of the section are not exposed, but along the sides of the ravines 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 from spore-pollen and paleomagnetic analyzes directly on the territory of the city of Krasnoyarsk (Gremyachiy Log).

The alluvial deposits of the VI and V terraces of the Yenisei belong to the middle stage of the Neopleistocene. Terrace VI (Sobakinskaya) is best developed on the left bank of the Yenisei, near the western outskirts of Krasnoyarsk. Here it stretches from the area of ​​the mouth of the Karaulnaya River, through the mouth of the Sobakina River near the village of Udachny to the Peshcherny ravine at the western outskirts of Akademgorodok. The lower parts of the Sobasky alluvium section are exposed by a small quarry located on the surface of the terrace opposite the governor’s residence “Sosny”. Here, predominantly fine-clastic pebbles are developed, which include volcanic and siliceous rocks, vein quartz; There are poorly rounded fragments of Vendian sandstones that make up the base 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 on terrace VI is up to 10 m. Terrace V (Lagernaya) is widely represented on the left bank, from the mouth of the Kachi to the Aluminum Plant. To a depth of 1.5-2 m, the terrace is composed of loess-like loams. Below you can see sandy loam, fine- and medium-grained sand with rare pebbles. Pebbles are observed at the base. The thickness of the alluvium of terrace IV reaches 35 m. The lower part of the alluvial strata is dated to the second Middle Neopleistocene interglacial based on finds of remains of mammoth fauna and a sporopyllen complex (Berzon et al., 2001)

Alluvium of the upper Neopleistocene is represented by sediments of the IV (Berezovskaya), III (Krasnoyarsk) and II (Ladeyskaya) terraces of the Yenisei. The third terrace, 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 blown sand. The thickness of the sediments is 20 m. The lower alluvium with the remains of a woolly rhinoceros and a mammoth corresponds to the glacial period in the composition of the sporopyllen complex and the characteristics of the sediments. The tops of the section contain the southern taiga SPC with an admixture of broad-leaved trees, corresponding to the interglacial period. 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. From it, a radiocarbon dating of 20900±300 years was obtained (Berzon et al., 2001). Terrace II is widespread on the right bank. The entire area along Krasnoyarsky Rabochiy Avenue is confined to its surface. The alluvium of the terrace is represented by pebbles, layered sandy loams with layers of greenish clay, and gray loams. Thickness 14 - 20 m.

The deposits of the first above-floodplain terrace of the Yenisei have a borderline Late Neopleistocene-Holocene age. They are represented by sandy loam with layers of clay and silt, sand, and pebbles. The thickness of the deposits is up to 9 m.

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

Lacustrine-alluvial deposits compared with level VIII terraces of the Yenisei (Eopleistocene), form a plain along the left bank of the river. Kacha, being the facies of the periglacial basin in the river valley. 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).

Lake sediments (limnium) accumulate in modern ponds, many of which are located in the suburban area of ​​Krasnoyarsk. They are represented by sapropel 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 (polustrium) are developed locally in highly moist areas in the floodplains of streams and small rivers. Their observation is possible only when digging small pits in late autumn, when the swamps begin to freeze. The sediments are represented by clay-organogenic sediments of a dark gray color, with a large amount of undecomposed plant material. The age of the swamp deposits identified in the vicinity of Krasnoyarsk is Holocene.

Eluvium is a product of the destruction of bedrock that occurs at the site of formation. It covers gentle 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 the turf layer. Power - up to the first tens of centimeters. The age is determined in the range from Eopleistocene and even late Neogene to modern.

Proluvium is the deposits of temporary water flows. It composes numerous alluvial cones superimposed at the mouths of dry ravines on the surface of various terraces and the modern floodplain, and also often lines the bottoms of dry ravines. It is composed of unsorted loams and sandy loams, usually brown in color, with crushed stone, 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 in some cases When the alluvium of high terraces is eroded, the alluvium contains well-rounded pebbles. The alluvial cones exhibit coarse irregular layering, expressed in the alternation of layers and lenses of irregular thickness, differing in the proportion of coarse clastic material in the composition. The sections of some alluvial fans contain horizons of buried soils. This indicates breaks in the accumulation of proluvium, during which the formation of the soil cover began, after which the removal of clastic material by temporary flows resumed. Numerous alluvial fans can be observed along the entire highway from the village Dachny on the left bank of the Yenisei (near Akademgorodok) to the village. Udachny (where they are often exposed by roadside excavations), as well as along the foot of the Torgashinsky ridge on the right bank of the Bazaikha River. The proluvium thickness in alluvial cones can reach 10 meters or more.

The age of the proluvium and all slope deposits described below is determined at each site geomorphologically by relationships with terrace surfaces. In general, their accumulation occurred in the range from the Eopleistocene to the Holocene and continues at the present time.

Colluvium - landslide and scree deposits - is represented by rubble and blocks. It is developed mainly on steep and dry slopes of southern exposure, where physical weathering processes predominate and their products cannot be retained by too sparse vegetation cover. Colluvial sediments cover the slopes with a thin cover and form, often together with proluvial 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 throughout the foothills of the high terraces of the Yenisei along the road from Akademgorodok to the village. Udachny, where the base is almost entirely composed of sandstones and siltstones of the Tyubilsky suite, which, when weathered, easily crumble into a patchwork.

Desertsion is an unsorted gravelly material developed on moderately steep slopes (mostly with southern exposure), and slowly sliding under the influence of temperature fluctuations. Typical desert formations can be observed on the southeastern slope of the Nikolaevskaya Sopka mountain, in a roadside excavation, where they overlap the bedrock outcrops of syenite porphyry and microgabbro and are themselves composed of products of their destruction. Desertion power up to 1 - 2 m.

Diluvium is a product of washout by rain and melt water. It is represented in the vicinity of Krasnoyarsk by thin, essentially clayey sediments found in the lower parts of gentle slopes. Under modern conditions, the formation of colluvium 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 colluvium was formed during cold periods in a periglacial environment, with sparse vegetation cover. The processes of colluvium formation and desertion often occur on the same sections of slopes, but in different time and probably under different climates, due to changes in the nature of vegetation

Defluxation is another type of slope deposits, the formation of which is the result of plastic sliding of highly moistened, essentially clayey soils. The composition is loam, often with crushed stone of underlying rocks. It is formed mainly on slopes of northern exposure, as well as on shaded and wet slopes of deeply incised ravines. Here, defluxation deposits also often alternate with colluvial deposits that accumulated in colder eras with sparse vegetation cover. In modern conditions, defluxation processes are most activated after snow melts, when the uppermost layer of soil, highly moistened by melt water, slowly slides along a deeper layer that has not thawed and therefore impedes the underground flow of melt water. Similar phenomena can often be observed in early spring in roadside excavations that cut off moist slopes.

Delapsies - deposits of landslide origin - are developed locally on steep slopes composed of loose unstable soils provided they are recharged with groundwater. These are piles of entire layers or blocks of loose sediment that have moved 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 groundwater levels (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 crushed stone-block deposits of quarry dumps, formations of dams and embankments of various granulometry, and bottom sediments of industrial settling tanks. The latter, in particular, include technogenic silt from the ash settling tank of CHPP-2, located in an abandoned quarry of the Tsemzavod.

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

View from Pokrovskaya Mountain

They are thin sediments of ash-gray color with thin parallel bedding and high contents of heavy metals. As the settling tank fills, they are removed and transported for burial in the nearby Tsvetyushchy Log quarry. A special type of technogenic deposits are accumulations of household, construction and industrial waste at 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 various petrographic compositions, formed in the age range 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 foliated. In the Krasnoyarsk zone, its bodies form two close “belts”: Akshepsky and Sliznevsky. Previously they were united by G.V. Pinus to the “Krasnoyarsk Belt”. The “Sliznevsky belt” is located in the zone of a large deep NE-trending fault up to 10 km wide (from the mouth of the Bazaikha River to the mouth of the Sliznevaya River) and more than 35 km long. Ultrabasic rocks of the complex are exposed in the basin of the Bolshaya and Malaya Sliznevykh rivers, the Sobakina River, on the left bank of the Yenisei River, above the village of Udachny, as well as in the lower reaches of the Bazaikha River (Blue Hill and Mount Vyshku).

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

Serpentinite with sliding mirror (1 side)

Serpentinite with slip mirrors (2nd side)

Small bodies of hypermafic rocks are close to each other, forming chains consisting of two, less often three or four, lens-shaped bodies of linearly elongated protrusions, with a thickness of 100 - 200 m. The largest of them are the Bazaikhsky (5 km2) and Sliznevsky “massifs” (about 12 km2). All protrusions are composed of sheared, less often massive, serpentinites, green and dark green (to black) in color, sometimes containing a few relics of olivine (partially replaced by iddingsite) and rhombic pyroxene (enstatite). Among the accessory minerals, magnetite and chromite predominate. In relatively large bodies of ultramafic rocks, various ultramafic and mafic rocks are observed, which have been subjected to varying degrees of serpentinization processes. Thus, 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%), highly 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, permeated with veins of chrysotile-asbestos and carbonates, is exposed. The serpentinites of the described area were formed due to pyroxenites, peridotites, dunites and other rocks of similar petrographic composition. The complex has not been studied enough, and there are no reliable data to substantiate its age. Its Late Riphean age is assumed conditionally.

Bakhtinsky 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 in size, intense greenstone fine- and medium-grained microgabbro with a gabbroophite structure. The contacts of the dikes are sharp, tearing, and the sills are concordant with the host sediments.

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

Root outcrops 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 volcanic rocks of the cover facies in the Bakhtin Formation and are often feeder channels for these effusives. The Late Riphean age is assumed conditionally.

Middle-Late Ordovician intrusions

Genetically and spatially, they are related to the volcanics of the Imir Formation, and the figurative points of the compositions of both volcanic and intrusive rocks form common differentiation trends on most petrochemical diagrams, which makes it possible to consider them as members of common volcano-plutonic associations. Magmatism of the Ordovician stage is characterized by increased alkalinity, with a 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 - low Rb content and high Sr, Ba, Th, Mo and B contents.

Imir volcanic complex. Vent and subvolcanic formations are an integral part of the Imir basalt-trachyandesite-trachyrhyolite volcanic complex. They form stocks, ethmolites, akmolites, and necks with an area of ​​up to 3 km2 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 village of Udachny, as well as on the spout of the Gladkaya and Krutaya Kacha rivers. filled with eruptive breccias of predominantly basaltoid composition, in which isolated fragments of pink trachytes and microsyenites are found.

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 with a thickness of 0.5 - 0.6 m, traceable over a distance of 500 - 800 m, sometimes more than 1000 m. Usually, subvolcanic intrusions of the complex are quite clearly distinguished in the relief in the form of crests, ridges and isometric peaks .

The intrusion of quartz syenite porphyries (in the area of ​​the First and Second Sopka mountains) is a laccolith, the roof of which is well prepared in modern relief. The intrusion has a zonal structure. In its center, quartz weakly porphyritic syenites are developed. Pink colour with a fine-grained groundmass, and the peripheral zone of the intrusive body is composed of microsyenites and syenite porphyries with a fine-grained groundmass. In terms of petrochemical characteristics, they are close to the corresponding effusive rocks of the Imir Formation.

Geological map of the “Long Griva” ridge (Perfilova, Makhlaev, 2010):

1 - quaternary formations; 2 - Imir volcanic complex, subvolcanic formations: 2 a - porphyry syenite, 2 b - fine-grained weakly porphyritic syenite; 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 - coarse porphyry basalts (first member); 11 - Ungut formation - limestones and dolomites; 12 - Tyubilsky suite, Verkhnetyubilsky subformation - sandy and clayey bituminous limestones; 13 - Tyubilskaya suite, Nizhnetubilskaya subformation - sandstones, rhythmically layered, calcareous siltstones; 14 - Akshepa complex of alpinotype hyperbasites: serpentinites, peridotites, pyroxenites; 15 a - geological boundaries, 15 b - facies boundaries, 15 c - occurrence elements; 16 - 18 - discontinuous violations: 16 - reliable; 17 - suspected; 18 - covered with 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 area of ​​Divnogorsk and Minino station), determined by the U-Pb method, was 447 ± 10 million years.

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 Shumikha 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 the State Geological Maps, 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 areas. 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 are biotite (usually highly decomposed), green aegirine-augite and augite, hornblende. Accessory minerals: magnetite, apatite, zircon, rutile, sphene. Characterized by increased alkalinity of the potassium-sodium type, less often 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-shaped body with an area of ​​about 40 km2. Previously it was considered a subvertical rod. But our analysis of the petrostructural zoning of the intrusion allows us to consider it as a laccolith, gently plunging to the northeast, under the valley of the Bazaikha River, which is confirmed by the latest geophysical data. The intrusion contains formations of two crystallization phases. Almost the entire volume belongs to the main phase, composed of relatively coarse-grained rocks, the composition of which varies smoothly in the range from syenites and quartz syenites to granosyenites. The crystallization phase 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, internal 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 in the modern erosion section are observed in the highest part of the watershed, is composed of granosyenites, which are also distinguished by the smaller grain size of the groundmass (1 - 3 mm). Dark-colored minerals are represented by green augite and hornblende, and less commonly 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, for the most part does not differ in mineral composition from the internal one. But in some areas it contains grains of alkaline dark flowers, replacing the primary hornblende. This is apparently due to the processes of endocontact metasomatism at the boundaries of the intrusion with calcareous rocks, where metasomatic removal of silica is characteristic, resulting in an increase in total alkalinity.

Exocontact changes in the host rocks manifested themselves in their hornification, argillization, marbleization, beresitization, skarning, and sometimes feldspathization over a considerable distance (up to 1.5 km).

The rocks of the Stolbovsky syenite-granosyenite complex belong to the moderately alkaline suborder of the potassium-sodium series (with a predominance of Na).

The Late Ordovician age of the Stolbovo complex is determined both by the breakthrough of comagmatic effusives of the Imir Formation and on the basis of available radioisotope dating: for the Stolbovo massif - U-Pb 449±3 and 451 Ma, K-Ar 469 Ma (Rublev et al., 1995).

In the Stolbovsky massif, occurrences of fluorite and molybdenite have been established. Syenites of the Stolbovskaya intrusion (Mokhovskoe deposit) are widely used as facing stones for external and internal decoration of buildings in the city of Krasnoyarsk, for the manufacture of monuments, road curbs, and stairs.

Syenites of the Stolbovsky complex. Mokhovskoye deposit

Early Devonian intrusions

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

Chernosopkinsky complex (D1čr). Includes rocks of the petrotypical massif of the Black Sopka mountain and numerous dikes of trachydolerites and dolerites among the formations of the Karymov Formation of the Early Devonian. Mount Black Sopka is clearly visible from many areas of Krasnoyarsk, being one of the highest peaks in the vicinity of Krasnoyarsk. Absolute altitude mountains - 691 m. It is located 8 km southeast of the city of Krasnoyarsk in the Berezovsky administrative region, in the area where the northwestern tip of the Eastern Sayan meets the Rybinsk depression

For the first time, the Black Sopka mountain massif was described by Yu.A. Kuznetsov in 1932. He identified 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 Permian-Carboniferous. S.I. shared the same point of view. Makarov (1968). Later, the Early Devonian age of the intrusion was established (Parnachev et al., 2002).

Black Hill is a subvolcanic intrusion well prepared in relief. In shape it is a rod with a diameter of 1.2 - 1.5 km, having a ring structure. Its central part is composed of alkaline olivine dolerites and essexites, and the periphery is composed of tinguaites; moreover, the latter perform a ring fault that arose after the formation of the dolerite intrusion. This is evidenced by the results of monitoring fracture tectonics, the presence of alkaline syenite-porphyry veins in dolerites and near-contact changes in the latter.

Kurums on the slope of the Black Sopka mountain

The stock of alkaline dolerites and essexites is inclined to the north, which is confirmed by the orientation of plagioclase phenocrysts in the porphyry varieties of these rocks. This is also evidenced by the asymmetrical arrangement of alkaline dolerites and essexites relative to the top of the Black Sopka mountain. If in the south their distribution is limited to a horizontal line drawn through 680 m above sea level, then in the north - to a horizontal line drawn through 550 m. Nepheline syenites occurring among the greywacke sandstones of the Tyubil Formation are known only in one exposure - 3.5 km west of Black Sopka mountains.

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

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

Mineral composition of alkaline syenite porphyries 2 phases: porphyry 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 nepheline segregations ( 2 - 3 mm). The groundmass consists of arcuate subparallel microlites of intensely pelitized and limonitized alkali feldspar, between which small xenomorphic grains of aegirine-augite are “sandwiched.” The areas are composed of an aggregate of fresh lath-like albite. Nepheline-containing and feldspathoid-containing syenite porphyries: albite, potassium feldspar, spreusteinized nepheline (or analcime) - up to 10 - 15%, aegirine and arfvedsonite - up to 10 - 15%, zeolites. Nepheline grains are often armored with prismatic grains of alkali amphibole and needle-like tangled fibrous aggregates of aegirine. Accessory minerals: titanomagnetite, fluorapatite, pyrite, pyrrhotite. Sometimes fluorite veins are observed in the rocks of the massif.

Nepheline-feldspathic rocks may be promising as a decorative facing material. The age of the Black Sopka mountain massif is Early Devonian, which is confirmed both by its comagmatism with the trachydolerites of the Karymov Formation of the Early Devonian, and by 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 Early Devonian magmatism of high alkalinity, which manifested itself within the Rybinsk depression, and comagmats of effusive rocks of the Karymov formation.

These dikes are predominantly developed in the southeastern part of the area. Moreover, trachydolerite dikes are often found directly among the formations of the Karymov Formation. Their morphology is varied. Length - from 200 - 250 to 2500 m. The predominant strike is northwestern, less often - northeastern. The dolerites and trachydolerites that make up the dikes are distinguished by their fresh appearance, have a dark gray and black color, and most often have a porphyritic structure with a fine-grained groundmass. The porphyry 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 with finely dispersed magnetite and therefore are characterized by increased magnetism.

5.3.. TECTONICS

In the geological structure of the region of the city of Krasnoyarsk, three structural floors are clearly distinguished. The lower, folded structural floor is composed of formations of the Late Precambrian and Lower-Middle Cambrian. The middle, transitional structural, forming superimposed depressions, is made of volcanogenic and sedimentary rocks of the Middle-Upper Ordovician, Devonian and Lower Carboniferous. Finally, the upper, platform structural level is represented by shallow-lying Mesozoic sediments.

The lower structural level (RF3 - €2) is characterized by complex dislocation of its constituent rocks. Their formation occurred in the conditions of an open oceanic basin and an active continental margin of the Pacific type (the setting of a marginal sea). They are mostly folded 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 alpinotype hypermafic rocks (Akshep complex), metapsammitic-siliceous-carbonaceous-schist with carbonate elements (Urman Formation), metacarbonate with carbon-siliceous elements (Manskaya Formation) and metapicrobasalt-metabasalt-metatrachybasalt (Bakhtin Formation).

In the territory under consideration, the formations of this structural stage are mainly developed in the form of tectonic wedges within the Laletin-Ustbazaikh fault zone. Formations of alpine-type hypermafic formations, in addition, occur along other subvertical faults of northeastern strike, forming lens-shaped protrusions. The relationship of the rocks composing 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 Kuwai series of the Upper Riphean with erosion and angular unconformity, on which the assignment of these formations to different structural stages is based, is established far beyond the boundaries of the territory we are considering.

Tectonic diagram of the surroundings of Krasnoyarsk. Compiled by G.V. Mironyuk based on materials from 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 - Derba anticlinorium (Kuluk block): 2 a - Sliznevskaya brachysyncline; 2 b - Malosliznevskaya syncline; 2 c - Namurt syncline; 2 g - Namurt anticline. II - Rybinsk depression: 3 - Krasnoyarsk monocline; 4 - Balayskaya synclinal zone: 4 a - Zhernovskaya syncline; 4 b - Sorokinskaya anticline.

West Siberian plate: III - Chulym-Yenisei trough. Prienisei depression: 5 a - Areisko-Shilinsky swell; 5 b - Badalyk trough; 5 in - Esaulovskaya trough.

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

Faults and their numbers: P1 - Kansko-Agulsky (Iysko-Kansky); P2 - Batoisky; 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, for the most part, were subjected to 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 the flysch formation (Tyubil Formation).

The formations of this stage make up the bulk of the formations of the lower structural floor in the immediate vicinity of the city of Krasnoyarsk. The sedimentary rocks of the stage over vast areas are crushed into tense linear folds, often overturned, broken by numerous faults of a reverse-thrust nature. As a result, there are numerous cases of repeated summation of the same section fragments. Most typically observed in many areas, the subsidence of the axes of overturned folds and fault planes at medium (30-50°) angles in the WSW direction, which corresponds to thrust movements from SW to NE. Folds and faults of this orientation can be observed southwest of Akademgorodok, along the descent along the Monastyrskaya road, and in the estuarine part of the Kaltat River. The largest folded structure composed of formations of the substage under consideration is the Bolshesliznevskaya syncline located on the right bank of the Yenisei. The axis of this syncline is oriented submeridionally. Its core is made of carbonate rocks of the Ovsyankovsky formation, and its wings are made of terrigenous deposits of the Tyubil formation.

The Torgashinsky structural block, located on the right bank of the Bazaikha River, stands out especially in terms of the occurrence of Cambrian deposits. Stressed linear folds and manifestations of thrust tectonics are not typical here. Here the rocks are collected in a series of gently sloping folds, with dip angles of 25 - 60o. Often these are monoclinally dipping, slightly wavy layers, complicated by flexure-like bends. It can be assumed that during the folding era this block played the role of an autochthon, in relation to which the remaining blocks of the lower structural floor were subject to thrust movements.

The middle structural floor (O2-3 - C1) is represented by sedimentary and volcanogenic formations of the Ordovician and Middle Paleozoic, filling individual depressions with a pronounced structural unconformity superimposed on the complex folded complex of the lower structural floor. The formation of these depressions took place on young continental-type crust 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, partly, geological formations, but corresponding to two different stages of tectonic activation - the Middle-Upper Ordovician and the Devonian-Lower Carboniferous.

Middle-Upper Ordovician substage (O2-3). The formations of this subfloor are represented exclusively by igneous rocks - volcanics of the trachybasalt-trachyte-trachyrhyolite formation (related to the Imir formation or the Divnogorsk strata (O2-3). They form the Kachinsko-Shumikhinskaya 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 section 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. The lava flows and tuff layers that fill the depression are gently plunging (at angles up to 30 - 35°) from the edges depressions in the northern 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 (Stolbovsky complex), developed partly within the Kachin-Shumikha depression itself, partly - in the structures of its folded frame (among the formations of the lower structural floor).

Devonian-Lower Carboniferous substage (D1 - C1). Its rocks formed the Rybinsk depression, which opens from the city of Krasnoyarsk in the eastern and southeastern directions. The Lower Devonian formations of this substage are represented by a combination of molasse and trachybasalt-trachyte-trachyrhyolite formations, together forming the Karymov Formation. The overlying sediments are represented mainly by formations of the continental terrigenous red-colored formation with elements of carbonate, as well as terrigenous-telepyroclastic formation (Krasnogoryevskaya formation of the Lower Carboniferous). In the structure of the substage, several structural stages are distinguished: Lower Devonian (Karymovskaya 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 substage in the area of ​​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 southeastern direction. Within its boundaries there is a stable monoclinal dip of Devonian and Carboniferous sediments in the northeast direction at angles of up to 20°. The Zhernovskaya (Berezovskaya syncline) replaces the Krasnoyarsk monocline in the SE direction. This is a brachyform fold located in the valley of the Berezovka River in the area of ​​Zykovo station and the Petryashino platform. It is composed of rocks of various members of the Karymov Formation. The fold axis is oriented submeridianally; the hinge is gently immersed in the south-south direction. The dip of the layers in the southwestern wing is 15 - 30°, and 30 - 55° in the northeastern wing.

The upper structural floor (J) in the area under consideration is entirely formed by sediments of the Jurassic system. They belong to the coal-bearing limnic formation and form a system of depressions in the Kansk-Achinsk lignite basin, stretching in a sublatitudinal strip along the northern periphery of the Altai-Sayan folded region. The formations of this level lie with sharp structural unconformity on all underlying sediments. In the marginal parts of the depressions, they are sometimes observed to be adjacent to more ancient formations. It is characterized by a very gentle bedding - angles of incidence usually do not exceed 5°. Only in the marginal parts, near faults and in rare flexural bends can they increase to a few tens of degrees.

Jurassic deposits of the region of the city of Krasnoyarsk belong to one of the depressions of the Kansk-Achinsk basin - the Chulym-Yenisei basin. Within its boundaries, on the territory of the city and its environs, there are two flat troughs - Badalykskaya and Esaulovskaya, as well as the meridionally oriented Areisko-Shilinsky shaft, limiting the Badalyk trough from the west.