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Course work
in structural geology
Analysis of the geological map and map of the tectonic structure
Introduction
Course project sums up the study of the most important part of the course of structural geology, dedicated to the forms of occurrence rocks and methods of their representation on geological and tectonic maps and sections. It contributes to the development of the ability to freely read geological maps and use the collected material for a comprehensive theoretical analysis.
The main goal of the course work is to consolidate knowledge of structural geology and develop the acquired skills in analyzing a geological map and a map of a tectonic structure. The work also aims to teach how to use geological map data for a number of generalizations.
To analyze geological maps, it is necessary to be able to determine the age sequence of sedimentary, metamorphic and igneous rocks and establish the forms of their occurrence; identify and determine the types of unconformity surfaces, analyze their significance for the geological history of a given territory; identify the most characteristic rock formations and analyze their relationship with the tectonic structure and geological history; taking into account the age, composition and thickness of the distinguished stratigraphic units and their changes along strike, as well as on the basis of an analysis of the tectonic structure, establish the main structural elements of the area and give its tectonic zoning; be able to determine the age of igneous formations, as well as to establish to which tectonic epoch the igneous complexes of the study area belong; be able to describe the tectonic structure and outline the main stages of its formation; analyze the geological history of the area and draw the main conclusions about the patterns and relationships of the most important geological events, drawing on the knowledge gained from the courses of historical and structural geology.
When solving the questions posed, a number of methods are used: analysis geological boundaries on the map, historical-geological and paleotectonic methods, bedding sequence analysis, breaks and unconformities analysis method, facies study method, thickness study method, formational analysis and other methods.
When performing this course work, the northern part of the educational geological map No. 23, scale 1: 50000, 1984, was used.
1. Relief and river network
1.1 Relief
Two types of relief are distinguished in the studied territory - mid-mountain and low-mountain. The lowest elevations are 640 m, the highest are 1400 m. The maximum elevation is 760 m.
Low-mountain relief prevails, it occupies about 65 - 70% of the area of the region. The maximum elevation here is 360 m.
Alpine relief occupies 30-35% of the area of the entire territory, the maximum elevation is 400 m.
The relief is confined to outcrops of Neogene, Paleogene, Cretaceous and Jura rocks.
1.2 River network
The entire studied territory is occupied by the basin of the Belaya River, formed by two large tributaries that merge in the southwest of the region. The river is represented by the main channel and many tributaries. The direction of the river flow is to the northeast, the channel is slightly meandering.
The left tributaries have a flow direction to the south, the right - mainly to the north.
Of the large tributaries, one can also note the mountain stream Plishka and the Mutny stream, located in the eastern and northeastern parts of the region.
River floodplain width Belaya varies from 1 km to 100 m, and the floodplain area increases in the direction of the current, i.e. to the northeast. The floodplain in the Mutnoy creek valley is up to 1.5 km wide. The height of the terraces is up to 40 m. The floodplain and terraces are composed of alluvial pebbles and sands
1.3 Stratigraphy
The study area includes rocks of the Jurassic, Cretaceous, Paleogene and Neogene systems. The Jurassic, Cretaceous and Paleogene systems are composed of sedimentary strata, the Neogene system is represented by volcanic-sedimentary rocks.
Jurassic system.
The deposits of the Jurassic system are distributed over a small area in the western and northwestern parts of the study area.
Deposits of the Middle and Upper Jurassic are known.
Middle department.
The rocks of the middle section of the Jurassic system were distributed only in the so-called tectonic wedges, formed by large faults and located in the north-west of the territory.
The sequence is composed of red clays with the presence of limestone marls, has a thickness of more than 270 m.
Upper department.
Represented by deposits of the Tithonian stage.
Tithonian stage.
Deposits of the Tithonian stage of the Upper Jurassic are known within tectonic wedges, are more widespread than the rocks of the Middle Jurassic and are represented by red limestones. On the underlying rocks, the deposits of the Tithonian stage occur according to. The thickness of the entire thickness is 300 m.
Chalk system.
In the study area, the Cretaceous system is represented by two divisions - upper and lower. The deposits of this system are distributed in the northwest and southwest of the territory.
Lower section.
Represented by the Polyana Formation.
Polyanskaya suite.
The deposits of the Polyanskaya suite are not widely distributed, they are observed only in the north-west of the territory, mainly in the area of the settlement of Yuryevka and are represented by sandstones. The thickness of the thickness is more than 600 m.
The sequence rests on the underlying rocks unconformably; contact with the underlying Jurassic rocks is traced along a deep fault.
Upper department.
Represented by the Lyut retinue.
Lyut Formation
The deposits of the Lyutskaya suite stretch from the northwest to the southeast of the territory, crossing the river. Belaya near the settlement Yuryevka; a small outcrop of rocks is also observed in the southwest.
The sequence is composed of sandstones and rhythmically alternating marls and clays, its thickness is 280 m. On the underlying rocks of the Polyana suite, the Upper Cretaceous rocks occur in accordance with the Jurassic deposits, the contact is traced along the fault.
Paleogene system.
In the study area, the Paleogene system is represented by all three divisions. The rocks of this system are quite widespread; they are observed in the west and south-west of the region.
Lower section.
The deposits of the Lower Paleogene are most widely developed and are known mainly in the southwest of the territory. They are represented by rhythmically alternating siltstones and blue, red and green clays. The thickness of the entire stratum is 320 m.
Middle and upper divisions.
The undivided middle and upper sections are represented by the Lumshor Formation. The upper section is represented by the Petrovsky Formation.
Lumshor suite.
The deposits of the Lumshor Formation are quite widespread and stretch from west to south of the territory. They are represented by a rhythmic alternation of siltstones, mudstones and marls. The thickness of the sequence is 500 m. The contact with the underlying deposits of the Lower Paleogene is consistent.
Petrovsky retinue.
The deposits of the Petrovsky Formation stretch from the west to the south of the territory and are represented by black siliceous marls, mudstones and limestones. The thickness of the layer is 440 m.
Neogene system.
The Neogene system is represented by two divisions - the lower, Miocene, and the upper, Pliocene. Neogene deposits are widespread in the area and are represented by both sedimentary and volcanic-sedimentary rocks.
It is composed of strata of sedimentary rocks distributed in the north, east and southeast of the territory. There are three formations: Dusinskaya, Chernikskaya and Mikhailovskaya.
Dusinsky retinue.
The deposits of the Dusinskaya suite are not widely distributed and stretch along the southern margin of the Miocene deposits from the northwest to the southeast. Detrital rocks - conglomerates, gravelstones and sandstones, with a total thickness of more than 520 m. Contact with the underlying Mesozoic and Paleogene deposits can be traced along a large deep fault.
Chernik suite.
The deposits of the Chernikskaya suite are the most widely developed of all Miocene rocks. They occupy the entire area in the north, east and southeast of the district. Represented by gravelstones, sandstones and clays with interlayers of brown coals. The thickness of the entire stratum is 480 m.
Mikhailovskaya retinue.
The rocks of the Mikhailovskaya Formation are known in the northwest, northeast, and east of the study area. They are represented by conglomerates, sandstones and clays with interlayers of liparitic tuffs with a total thickness of 400 m. The contact with the underlying deposits of the Chernikskaya suite is consistent.
The upper section of the Neogene system is represented in the studied area by volcanic-sedimentary rocks. There are three subdivisions: lower, middle and upper. The lower and middle sections are undivided and are represented by deposits of the Bystrinskaya suite.
Bystrinsky suite.
Deposits of the Bysrinskaya suite are known mainly in the central part of the region. They are represented by a sequence of liparitic ignimbrites with a thickness of more than 700 m, lying with angular unconformity in the Miocene and Mesozoic deposits.
Middle Pliocene. ,
In the Middle Pliocene, sequences of dacitic lavas are known, distributed in small areas in the east and northeast of the territory and having a thickness of 85 m. Andesitic lavas are also known, common in the central and eastern parts of the region. Facies replacements by tuffs and tuff breccias occur in their thickness. The thickness of the strata is 250 m. The nature of the relationship with each other and with the underlying ones is an angular unconformity.
Upper Pliocene.
Deposits of the upper subdivision of the Pliocene are distributed in the east of the territory and stretch from south to north. They are represented by andesite-basalt lavas, the thickness of which is 80 m.
2. Intrusive formations
2.1 Pliocene intrusive formations
Intrusive formations are not widely developed in the study area and are represented by a single intrusive body located in the west of the territory. Its area is 0.75 km2, in plan it has a narrow, 250 m wide, elongated shape. Composed of granite-porphyry.
The size of the intrusive body is small; According to the structural features, it can be attributed to dikes.
The dike is dated to the Pliocene and has a secant contact with the Upper Cretaceous deposits, with the Upper Jurassic - contact along the fault. (Fig.1)
Rice. 1 Pliocene dyke composed of granite-porphyries
Vortex formations.
The rocks of the vent facies in the study area are represented by Middle Pliocene and Lower-Middle Pliocene formations, confined mainly to a large fault.
Vent formations of the Lower-Middle Pliocene.
Known in the south of the territory, in the area of the sources of the stream. Plishka. In total, there are 4 bodies in the area. In plan they have an elongated oval shape, their area is from 1 km2 to 0.7 km2. Composed of liparitic ignibrites, they belong to necks according to their structure.
They cut through the Pliocene deposits of the Bysrinskaya suite and are overlain by the Middle Pliocene strata.
Rice. 2 Vent formations of the Lower-Middle Pliocene.
Vent formations of the Middle Pliocene
4 bodies are known in the north-west of the territory, in the area south of the settlement of Yuryevka and in the north-east of the territory. They have an elongated oval shape.
The area of the smaller of them is 0.3 km2, the rest is about 0.75 km2. They are composed of dacites and, according to the features of their structure, belong to the necks. The bodies located in the center of the area break through the Mesozoic deposits and deposits of the Bysrinskaya suite. One of the bodies is overlain by andesite-basalts of the Middle Pliocene.
Rice. 3 Middle Pliocene vent formations
Rice. 4 Middle Pliocene vent formations
Tectonics.
According to the conditions of occurrence and magmatism in the structure of the region, the middle Alpine geosynclinal and late Alpine orogenic structural stages are distinguished.
Middle Alpine geosynclinal structural stage.
Includes deposits from the Middle Jurassic to the Petrovsky Formation of the Upper Paleogene, crumpled into linear folds. Developed in the southwest of the region.
In the structure of this structural stage, the following formations are distinguished: carbonate-terrigenous, including deposits of the Middle Jurassic (red clays, marls and limestones); formation of red limestones of the Tithonian stage of the Upper Jurassic; the formation of uneven-grained sandstones of the Polyanskaya suite of the Lower Cretaceous; two flysch carbonate-terrigenous formations, the lower of which includes deposits of the Lyutskaya suite of the Lower Cretaceous, and the upper one - of the Petrovsky and Lumshorskaya formations of the Middle and Upper Paleogene (here, members of itmic alternating marls, siltstone clays, mudstones and limestones); flysch terrigenous formation of Lower Paleogene rocks (colorful clays and siltstones).
The rocks that make up the Middle Alpine geosynclinal stage are crumpled into linear folds. The axes of the folds stretch from the west and northwest to the south, crossing the river. Belaya in the area of the settlement Yuryevka and upstream.
According to the shape of the lock, the folds are rounded and comb-shaped, and the locks of the folds of older rocks (Cretaceous) have a comb-like shape. With respect to the axial surface to the horizon, the folds are inclined. The angles of inclination of the wings of the folds from to.
Among the clearly visible folds of the first order, 2 anticlinal and 1 synclinal folds stand out.
Synclinal folds.
The fold is located at the confluence of two tributaries in the Belaya River (Fig. 5), has a length of more than 7 km and a width of more than 2 km.
The wings of the fold are composed of rhythmically alternating carbonate-terrigenous rocks of the Lower and Middle Paleogene, in the core of the fold there is a flysch sequence composed of rhythmically alternating rocks of the Upper Paleogene Petrovsky Formation.
The axis of the fold stretches from west to south. The angles of inclination of the wings, and on the northern wing (the angles change accordingly from west to south) and on the southern wing.
The fold is round in shape of the castle, the hinge plunges in the southeast direction, rises in the northwest, forming a centriclinal closure.
Rice. 5 Synclinal fold
2.2 Anticlinal folds
One of them is located in the northwestern part of the territory, its axis stretches from the northwest to the south and, making a smooth bend, crosses the river. Belaya near the village of Yuryevka. The fold is over 10 km long and slightly over 1 km wide. Its wings are composed of rhythmically alternating carbonate and terrigenous rocks of the Upper Cretaceous Liutskaya suite, in the core - inequigranular sandstones of the Lower Cretaceous Polyanskaya suite.
The northern flank of the fold has a slope, the southern one.
The lock of the fold is ridge-shaped, the hinge either plunges in the direction to the northwest and southeast, forming two periclinal closures, then it rises. (Fig. 6)
Rice. 6 Cretaceous anticlinal fold
The second anticline fold is located in the southwest of the region. It is over 5 km long and up to 1 km wide.
The wings are composed of flysch Middle and Upper Paleogene sequences, in the core there is a rhythmic alternation of clays and siltstones of the Lower Paleogene age. The angles of inclination of the wings: at the southern wing, and at the northern one (the angles change in the northwest direction).
The lock of the fold is rounded; on immersion, the hinge forms a pereklinal closure. (Fig. 7)
Rice. 7 Anticlinal fold composed of Paleogene deposits
Among the folds of the second order, 3 synclinal folds can be distinguished, two of which are confined to the Cretaceous anticline fold, and one - to the Paleogene anticline fold.
There are two anticlinal folds of the second order - one is confined to the Cretaceous anticline fold of the first order, the second - to the Cretaceous deposits, the outcrop of which is observed in the south-west of the region.
2.3 Late Alpine orogenic structural stage
Includes deposits of the Miocene and Pliocene. According to the conditions of formation and features of the structure, it is divided into two sub-levels - upper and lower.
Lower structural subfloor.
Includes Miocene deposits folded into brachyform folds. Developed in the north and northeast of the region.
In the structure of the substage, the following formations are distinguished: the lower molasse, composed of conglomerates, gravelstones and sandstones of the Dusinsky suite of the Miocene; coal-bearing molasse, including deposits of the Chernikskaya suite and the upper molasse, including rocks of the Mikhailovskaya suite.
Tectonic structure of the region:
The rocks of this substage are crumpled into brachyform folds.
The limbs of the synclinal folds are composed of coarse clastic rocks of the Chernik and Dusinsk suites of the Miocene, with rocks of the Mikhailovskaya suite in the core.
The castle is rounded, the slope angles are gentle, from to, and the largest angles are noted near the southern flank of the fold, composed of rocks of the Dusinsky suite.
Upper structural subfloor.
Includes Pliocene deposits that make up a large volcanic edifice.
Liparitic ignimbrites of the Bysrinskaya Formation of the Lower-Middle Pliocene and dacitic lavas of the Middle Pliocene compose the terrestrial porphyry formation. Andesite-basaltic lavas, tuffs and tuff breccias of the Middle and Upper Pliocene make up the andesitic formation.
Tectonic structure of the region:
The volcanic edifice has a synclinal structure.
Lines of primary banding are directed towards the center at gentle angles no more.
Lower-Middle Pliocene deposits of the Bysrinskaya suite (liparitic ignimbrites) are confined to the intrusion of vent formations of the Lower-Middle Pliocene and form covers. They are distributed over a large area in the center of the region and cover all Mesozoic and Miocene deposits.
Dacitic lavas of the middle Pliocene compose two small shield volcanoes - one in the northwest of the territory, the other in the northeast. It is characterized by horizontal and inclined (up to) lines of primary banding.
Andesitic lavas of the middle Pliocene form flows with horizontal and inclined (up to) flow lines.
In smaller areas, andesite-basaltic lavas of the Upper Pliocene are common. They have sloping streamlines and stretch from south to north.
Breakdown violations.
On the territory of the study area, there are discontinuous faults of various types and age.
It is possible to distinguish inclined and vertical faults.
All inclined faults are confined to zones of linear folding. They have a longitudinal strike, a large extent, the angle of inclination of the displacer is about, the displacer itself has an inclination to the northwest.
Faults and reverse faults stand out among the faults.
Near reverse faults, the northwestern block is uplifted and composed of older rocks; near normal faults, the northwestern block is lowered and composed of younger rocks.
The time of formation of oblique faults is after the accumulation of the Upper Paleogene Petrovsky Formation, after linear folding, before the accumulation of the Miocene.
A large vertical normal fault stretches across the entire territory of the region from the northwest to the southeast, separating the orogenic and geosynclinal structural levels, and is overlapped in the southern and central parts by Pliocene volcanic-sedimentary formations. The northeastern block, composed of Miocene rocks, is subsided, while the southwestern block, composed of Jurassic, Cretaceous, and Paleogene deposits, is uplifted. Vertical normal faults are attached to this large fault in places, forming wedges along which Jurassic deposits are raised.
The age of the fault is after the accumulation of the Petrovsky Formation of the Late Paleogene, after linear folding, before the accumulation of Miocene strata. The fault is long-lived and remained tectonically active during the accumulation of Miocene deposits.
The latest faults are confined to the effusive strata of the Pliocene. They are located along the banks of the stream. Plishka, and are represented by vertical faults that form graben-like structures in pairs.
sedimentary mountainous tectonic geological
3. History of the geological development of the area
A geosynclinal trough existed on the territory of the studied area in the Middle Jurassic.
The sediments formed during this period testify to the existence of a marine basin of moderate depth with a remote coastline in this area, as evidenced by the terrigenous material present in the sequence.
In the Late Jurassic, the area of the sea basin increased, the coastline moved further away from the coast, as evidenced by the absence of terrigenous material in the thick limestone member. After that, there was an uplift and the associated regression of the sea.
In the early Cretaceous, the transgression of the sea began. The sea basin was shallow with a close coastline, as evidenced by a thick sequence of inequigranular sandstones formed due to the removal of clastic material from the nearby land.
Further, in the Late Cretaceous, the basin continues to deepen, and throughout both the Late Cretaceous and the entire Paleogene, carbonate and terrigenous rocks are deposited here, the rhythmic alternation of which indicates possible action muddy streams.
After the accumulation of the Petrovsky Formation of the Late Paleogene, the area was uplifted and the sea regressed, after which the accumulated sediments were crushed into linear folds and faults were formed longitudinal and transverse to these folds. The Middle Alpine geosynclinal structural stage was formed. During the subsequent time, this territory remained dry land.
In the north-eastern territory of the region in the Miocene there was a shallow marine basin. The close location of the land led to the accumulation of coarse clastic material here, which formed molasse formations; in the Chernik time, interlayers of coal formed here, which indicates an extremely close location of the land, and during the accumulation of the Mikhailovskaya Formation, a small addition of volcanic material occurred, probably as a result of the activity of a volcano located outside the study area.
After the accumulation of the Mikhailovskaya Formation, uplift occurred, as a result of this, the sea regressed, and the accumulated sediments were crushed into brachiform sweets. The lower substage of the orogenic Late Alpine structural stage was formed.
In the Pliocene, deep processes sharply intensified, which led to the intrusion of Pliocene intrusions along large faults, with which the formation of tectonic wedges is associated, and, after that, to the beginning of the development of active volcanic activity, which continued throughout the Pliocene.
First, in the Lower and Middle Pliocene, magma was emplaced along a large fault, which formed vent formations, and the associated flows of liparite ignimbrites were erupted.
In the Middle Pliocene, the intrusion of magma continued; vent formations and covers composed of dacitic lavas were associated with them.
Later intrusions of magma are associated with flows of andesites and andesite-basalts of the Middle and Upper Pliocene.
The tectonic activity of the region did not end there, several faults were formed, which formed graben-like structures.
Conclusion
The result of the analysis of the geological map was the writing of this term paper. A tectonic scheme and a diagram of the relief and river network were drawn up; sections, a block diagram and a structural-formational column were built.
In conclusion, it is worth mentioning the importance of doing this work, which consolidates all the material received over the previous two semesters.
Among the shortcomings, it should be noted that the deadlines for its implementation are too long. Perhaps they should be reduced to 1.5 months and set clear deadlines, which, of course, will only become an additional incentive for writing a course project as soon as possible.
List of used literature
1. A.E. Mikhailov. Structural Geology and Geological Mapping 2012.
2. Uspensky E.P., edited by Mikhailov A.E. Guidelines for coursework on structural geology and geological mapping 2009.
3. Handbook for laboratory work on structural geology, geomapping and remote sensing methods 2010.
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MOSCOW STATE UNIVERSITY
GEODESY AND CARTOGRAPHY
Department of Geography
Practical work No. 1
ANALYSIS OF PHYSICAL, TECTONIC AND GEOLOGICAL MAP
ZONE(100°-130° E)
I've done the work:
Student FKG KiG II-1b
Pashkin A.A.
Teacher:
Associate Professor of the Department of Geography Ph.D.
Kolesnikov Sergey Fyodorovich
Moscow 2014
Lithosphere and relief of the Earth
physical map
Geological map: Scale 1: 80,000,000
The structure of the earth's crust: Scale 1: 80,000,000
Climate map:
The area under consideration in this laboratory work is limited by the longitudes of 100°-130°E. It contains a section of the Eurasian terrain that includes: Eastern Siberia, the Gobi Desert, the Eastern part of Tibet, the Indochina Peninsula, the Indonesian archipelago and the West of Australia.
Research on the physical map:
This area is located entirely in the Eastern Hemisphere between 100°-130°E. In the northern part: part of the Eurasian continent, in the southern Indian Ocean and Western Australia.
Relief:
It is very diverse, since there are quite mountainous areas here: the Central Siberian Plateau, part of Tibet and a rather flat area in Western Australia.
Geological structure:
It is represented by almost all rocks (mainly sedimentary)
In Eurasia, these are most often rocks of the Archean and Proterozoic groups of the Paleozoic, Jurassic, Triassic, Cretaceous systems of the Mesozoic group. Quaternary (in the south of Eurasia).
Australia: Quaternary, Paleogene-Neogene, Cretaceous, Permian system.
The structure of the earth's crust:
In this area, in the north, there is a boundary between the Eurasian and North American lithospheric plates. To the south, in two directions, there is the border of the Eurasian plate with the Philippine one. In the south is the boundary of the Indo-Australian and Antarctic plates.
In the north, we observe the divergence of lithospheric plates. Then south of the collision of plates. And then the divergence of lithospheric plates: Indo-Australian and Antarctic.
Indo-Australian plate. Almost all of Australia is a platform, most of which is plains. Tectonic activity is very slow, crystalline shields are formed. They are associated with minerals.
Climate: all climatic zones and climatic zones are presented here: from the Arctic to the equatorial zone. The continentality of the climate increases with distance from the sea.
Eurasia is rich in water resources; in the north and in mountainous areas, food is predominantly snow and glacial. In the west of Australia, on the contrary, there is a lack of water resources and a desert area.
The distribution of natural zones is mostly latitudinal and all natural areas from arctic deserts to equatorial forests. I am present in altitudinal zonation (mainly in Tibet).
Introduction
Goals and tasks of the work:
1. Training in the complex analysis of a geological map, the construction of derivative maps and schemes (orohydrographic, tectonic, etc.), profile geological sections;
2. Preparation for the passage of geological practice and training in the preparation of geological reports and graphic documentation;
3. Training in forecasting areas that are promising for the search for minerals. The ability to read and analyze a geological map means the ability to characterize:
1. Topography (relief) of the map area (orohydrographic analysis);
2. The sequence and nature of the bedding of rocks of individual stratigraphic complexes (stratigraphic analysis);
3. Tectonic structure and structural forms of the area (structural and tectonic analysis);
4. Genetic connection between the relief, geological structure and the latest tectonic movements (geomorphological analysis).
The generalization of all the data obtained is the reconstruction of the history of the geological development of the area. The study of the geological situation displayed on the geological map makes it possible to draw a conclusion about the prospects for discovering mineral deposits in the study area, including assessing the prospects for their oil and gas potential. Reading geological maps requires knowledge not only in the course of structural geology and geological mapping, but also in the courses of topography, general and historical geology, petrography, etc. The data of the map on which the study was carried out: map No.
Orohydrography
In orohydrographic terms, the territory is divided into two parts - the southeastern mid-mountain and the northwestern plains. The maximum marks are located in the southeast: 1454m, Knife, and the minimum in the north of the territory: 132.4m in the valley of the river. Irsha.
In the mid-mountain part of the territory, the Vostochny mountain range stands out. Maximum mark: 1367.2m. The length of the ridge is more than 15 km. In the low-mountain part of the study region, two mountain ranges are observed. The first one is located in the south, the Stanovoy ridge, and the second one, located in the east, the Lugovoi ridge.
On this geological map, several watersheds can be distinguished, dissected by rivers located from north to south. In the study region, there is a large number of rivers and temporary streams. The map clearly shows the Belaya River, which flows from the southeast to the southwest. It has many tributaries, such as the Kamenka River, the Smolka River, the Tom River, the Krasnaya River. The river itself has a great sinuosity.
The Bystraya (about 30 km long) and Bogataya (about 20 km long) rivers flow from south to north. There are many tributaries near the Bystraya River, one of which is the Klyuchevaya River. The length of the river exceeds 20 km. Several more rivers are observed on the territory, Kolomak with a tributary of the Merla River and Berestovaya with a tributary of the Ingulets River. All these rivers flow from south to north and are characterized by a significant meandering.
This region is very well developed. The map shows a large number of settlements. Most of the settlements are concentrated on the flat part of the territory: Khutora, Ovrazhki, Yurievka, Kalinovka, Malinovka, Makovka, Luzhki, Zgurovka, Shishaki. A large number of settlements stand out in the low-mountain part of the territory: Sosnitsa, Klyuchi, Tatarkino, Nida, Elkino, Boryspil, Dorohovo, Ternovka, Sharovka, Chernukhi. Two settlements are noted in the middle mountain part: Kamenka and Vyselki.
Thus, we can conclude that the study area is very well developed and favorable for life.
Stratigraphy
The study area is composed of deposits of the Mesozoic and Cenozoic groups.
Mesozoic group (Mz).
Mesozoic deposits include Jurassic and Cretaceous rock systems, widely developed in the southeastern part of the region on mountain ranges. The thickness of sedimentation is 3200 meters.
Jurassic system (J). Jurassic formations are represented in the region under study only by the upper section.
Upper section (J 3). In the study area, division into tiers in this department is not presented. The department is represented by deposits with a thickness of more than 550 meters. The outcrop of rocks to the surface is observed, as a rule, in the cores of anticlinal folds. The accumulated sediments are represented by light gray coarsely bedded limestones with interlayers of gray clays.
Chalk system (K). Cretaceous formations are represented by two sections: lower and upper. The total sedimentation capacity of the Cretaceous system is 2700 meters.
Lower section (K 1). In the studied section, it is represented by the Neocomian, Aptian, and Albian stages.
Neocomian (K 1 nc). Neocomian deposits compose mainly the entire southeastern part of the territory; they are also observed in a small amount in the northeastern part. They lie conformably on the Jurassic deposits. The precipitation capacity is 700 meters. Represented by sediments, rhythmically alternating gray sandstones, yellow marls and calcareous mudstones.
Aptian and Albian stages (K 1 ap+al). These deposits come to the surface in the southeastern and northeastern parts. The bedding of the rocks is consonant. The precipitation capacity is 350 meters. The accumulations are represented by massive light gray sandstones with lenses of mudstones and siltstones.
Upper section (K 2). The upper part of the Cretaceous system is represented by the Cenomanian, Turonian, Senonian and Danish stages.
Cenomanian and Turonian stages (K 2 cm+t). Stage deposits are developed in the southeastern and northwestern parts of the study area. The accumulated sediments lie conformably on older rocks. Sedimentation is represented by rhythmic alternation of gray layered sandstones, limestones and marls. In the lower part - layers of gray mudstones. The thickness of these deposits is 600 meters.
Senonian Stage (K 2 sn). Senonian deposits are developed in the northeastern and southwestern parts of the study region. The sedimentation capacity is 425 meters. The rocks lie according to. The deposits are composed of black mudstones and marls. At the base is a horizon of black siliceous mudstones.
Danish Stage (K 2 d). Deposits of this stage are observed in this region in small areas of the territory, usually in the form of remnants. They are observed in the southwestern and northeastern parts of the region. The rocks lie according to. The accumulated sediments are represented by gray lamellar clays with lenses of sandstones and siltstones. The power of which is about 375 meters.
Cenozoic group (Kz).
Cenozoic deposits include the Paleogene, Neogene and Quaternary systems. These accumulations are widely developed in the northwestern and insignificantly in the southwestern part of the territory. The deposits are located on a flat terrain.
Paleogene system (P). Paleogene formations are represented in the region under study by all divisions, i.e. Paleocene, Eocene and Oligocene. The total capacity is 1400 meters.
Paleocene (P 1). Paleocene deposits are developed mainly in the northeastern part and are confined to the flat relief. The deposits rest on older rocks with stratigraphic unconformity (erosion is observed). Sedimentation has a thickness of 1100 meters. These deposits are divided into two packs of rocks. The first unit consists of pebble and gravel conglomerates with pebbles of crystalline rocks. The second unit contains conglomerates and sandstones with rare interlayers of siltstones and clays.
Eocene (P 2). The deposits of the Eocene department overlie older rocks according to. The accumulated sediments of this section are observed in the northeastern part of the territory. The sediments are composed of gray massive sandstones with interlayers of gray clays. In the lower part there is an interbedding of sandstones and siltstones with plant remains. The precipitation capacity is 850 meters.
Oligocene (P 3). Oligocene deposits occupy an insignificant part of the flat terrain. They are observed only in the northeastern part. The bedding of the rocks is consonant. The deposits are composed of gray layered sandstones, red marls and plastic clays. These sandstones are gas-bearing. Sedimentation capacity 600 meters
Neogene system (N). Deposits of the Neogene system make up a significant part of the plain relief. The total thickness of deposits is more than 900 meters. The system is represented by Miocene and Pliocene divisions.
Miocene (N 1). Miocene deposits are developed in the northeastern part in an insignificant amount. The bedding of the rocks is consonant. The sedimentation capacity is more than 500 meters. The deposits are brown plastic clays with lenses and crystals of salt and gypsum.
Pliocene (N 2). Pliocene deposits compose almost the entire northwestern part. Occurrence of rocks on older ones with stratigraphic unconformity. These deposits are gray-yellow sandy limestones, with white loose sandstones and sands at the base. The thickness of the rocks that make up the deposits is 400 meters.
Quaternary system (Q). Quaternary deposits are represented in the study region by upper Quaternary deposits and modern deposits, which are common in river valleys. These Quaternary deposits are represented by alluvial sandy loams, alluvial sands and pebbles. Quaternary deposits occupy most of the study area and are mainly located on a flat terrain.
Tectonics
The territory under consideration belongs to the folded tectonic type of the structure of the earth's crust. According to the vertical section, 1 structural floor is allocated. All breeds present on the map are crumpled into folds.
The tectonic overthrust has a complex occurrence of the autochthonous and allochthonous parts of the structures, that is, the ancient rocks have moved over the younger leans.
In the southeastern part, there is a large wavy overthrust with rocks moving for many tens of kilometers. The fault plane here is composed of crushed rocks. Cretaceous rocks occur in the allochthonous part. Small strike-slip faults are widespread in the vicinity of the thrust fault. Erosion windows are represented by deposits of the Neocomian stage of the Cretaceous system. They range in size from 1 to 3 km. The occurrence of the folds that make up the erosion windows is overturned and inclined (overturned is 70 0, and oblique from 15 0 to 30 0).
The entire northwestern part has an occurrence of the autochthonous part of the structure. It is composed of younger breeds. These deposits are mainly of the Paleogene system (central part) and the Neogene system. In this part, a substage can be distinguished (the Miocene deposits lie obliquely, about 10 0) in relation to the Pliocene deposits. The remnants are represented by sediments of the Cretaceous system of the upper section, mainly by rocks of the Danish stage. Remains are observed in small numbers. The first is in the northeast and the second is in the southeast. The size of the first is 2 km, the occurrence is inclined 50 0 , and the second is 4 km and the rocks lie at an angle of 70 0 .
The northwestern part has a platform occurrence. Composed of Neogene rocks, the relief is flat. Quaternary rocks occur in river deltas. Mostly synclinal folds are observed here.
A series of linear folds is observed in the region under study. The folds have significant angles of incidence of the wings (mainly from 20 0 to 70 0). There are folds with vertical angle tilt 80 0 -85 0 . Inverted bedrock occurrences are also frequent on the map. In the southeastern part, there are mainly linear folds that were formed during thrusting, during the crushing of rocks, as a result, in the frontal part, there are mainly overturned folds.
Geomorphology and recent structures
The work area is characterized by denudation-erosion relief. Moderately intense uplifts occur here, slightly exceeding the intensity of exogenous processes. In the study area, a mid-mountain relief is formed with developed mature plains, relatively wide wavy interfluves. The region is characterized by a strongly dissected relief. The reverse relief is expressed in the development of mountains along the axes of synclinal folds in the southeastern part of the region. In the northwestern part, most of the direct relief, that is, the valleys correspond to synclinal folds.
In the structure of the region, 3 blocks are distinguished, characterized by intense, moderate and weak uplift. They experience vertical movements of different amplitudes.
The first block is a zone of intense uplift, it is located in the southeast of this area. Its marks do not exceed 1500 meters. In the central part of this area, the second block is distinguished, characterized by a relatively moderate uplift (heights do not exceed 1000 meters). The weak uplift zone is located in the northwest of this area. This block is relatively weak uplifts. The marks of this zone are less than 500 meters. The boundary between the zones of intense and moderate uplift is the gap shown on the map. The ancient gap is active in modern times as well.
Thus, taking into account the stratigraphic column, it can be said that the formation of a relief with uneven destruction of the surface of the earth's crust by exogenous processes occurs in those periods when stable tectonic uplifts are observed and, consequently, continental conditions (land) are established on the territory. The first clear uplift can be traced at the boundary between the Cretaceous system of the upper division and the Paleocene. At the Miocene-Pliocene boundary, a second clear uplift is observed, with which the most active folding is associated, at the same time a thrust was formed. The Cretaceous rocks composing the allochthon began to move towards the Paleogene. As a result of this movement, the rocks were crushed into elongated linear folds; brachymorphic folds were preserved in the northwestern part.
History of geological development
The geological history of the territory depicted on map No. 22 can be traced back to the Upper Jurassic, since the most ancient rocks are coarsely bedded limestones with interlayers of marls of the upper Jurassic system. These sediments belong to deep-sea facies. At this time, uplifts of the earth's crust took place and a sea basin existed.
In the Neocomian, the deep-water basin is replaced by a shallow one, there is an alternation of sandstones and mudstones.
In the Aptian-Albian, sedimentation slows down, the territory develops steadily in a shallow basin, and sandstones with mudstone and siltstone lenses accumulate.
In the Cenomanian-Turonian time, the rate of sedimentation increases, the subsidence of the territory begins, which continued until the Senonian. Both mudstones and limestones, marls and sandstones accumulate here.
The rocks of the Paleocene unconformably lie on the older rocks of the Danish stage, there is a sharp accumulation of sediments, since the thickness reaches 1000-1200 meters. At this time, pebble and gravel conglomerates with pebbles of crystalline rocks accumulate, the territory rises to sea level. Further, up to the Miocene, stable sedimentation, a slow subsidence of the territory can be traced, by the middle of the Miocene, the accumulation of shallow sea facies occurs, plate clays with lenses and crystals of salt and gypsum
The rocks of the Pliocene lie unconformably on the deposits of the Miocene, on the border of the Pliocene and Miocene there is a sharp rise of the territory to sea level, the accumulation of sandstones and sands. This time is characterized by the most active folding. An overthrust is formed, the Cretaceous rocks, advancing on the Paleogene, are crushed into elongated linear folds. In the frontal part of the thrust, as a result of the movement of rocks, overturning of the folds is traced. Now, in the Quaternary, the territory is rising, with the northwestern part rising more slowly than the southeastern. As a result, a mountainous dissected relief is formed in the south, and a flat one in the north. Rivers flow on the plains, Quaternary precipitation accumulates in the river valleys.
Minerals
Mineral resources in this area are gas, as well as sandstones and clays for the production of building materials.
Oil and gas prospects were found only in chalk deposits (according to the data of drilled wells). The Jurassic deposits (red clays) serve as a cover for this deposit. This deposit is confined to an anticline in the north-west of the territory.
The predicted deposits of building minerals are confined to Cretaceous deposits in the southeast of the study area (clays, sandstones).
And it is also possible to mine (Co, Sn, W, ...) in metasomatism zones, most likely The best way the extraction of these minerals is open pit, but I think it is also possible in a mine way.
The scheme of mineral prospects is shown in fig.
Conclusion
geological crust tectonic
In this work, I explored the territory and found that the area under study is divided into two types of relief: low-mountain and flat. I also determined that this territory is divided into three tectonic types of crustal structures: platform, folded and transitional. During the research, the latest faults, synclines and anticlines were identified.
My main task was to assess the prospects for the oil and gas potential of this territory. In the north of this territory, there are prospects for gas exploration in Oligocene deposits.
As a result of this work, I consolidated my knowledge of structural geology, and developed the acquired skills in the analysis of the geological map. And also learned to use geological map data for a number of generalizations.
Used Books
1.A.V.Matsera, L.V.Miloserdova, Yu.V.Samsonov. Course project in structural geology.
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Introduction
Chapter I. ORHYDROGRAPHY
Chapter II. STRATIGRAPHY
Chapter III. TECTONICS
Chapter IV. HISTORY OF GEOLOGICAL DEVELOPMENT
Conclusion
Bibliographic list
INTRODUCTION
The purpose of the course work is to learn how to independently analyze the geological map, which is the basis for the search and exploration of mineral deposits. Ability to observe geological objects and geological processes.
The task for the term paper was issued on 09/06/2007, the deadline for the course work is 12/12/2007.
Course work is carried out on the northern part of the educational geological map No. 13 of the 1971 edition. The scale of the map is 1:200000, solid contour lines are drawn every 80 meters. The area of the study area is 643.8 km2. The author of the map is A.A. Mossakovsky, the editors of the map are M.M. Moskvin and Yu.A. Zaitsev.
When performing the course work, a number of materials developed and published at USTU were used.
The main tasks of the analysis of the geological map are the following:
· determination of the age of igneous formations; · determination of the forms of occurrence of all rocks; · identification and characterization of all folded and discontinuous faults with their detailed description;
· identification of unconformity surfaces in the stratigraphic section and analysis of their significance in the geological history of the area; · identification of characteristic rock formations and analysis of their relationship with the tectonic structure and geological history of the territory; · deciphering the history of the geological development of the area based on the analysis of the geological map, sections and stratigraphic column, as well as the types and age of rock dislocations and the types and forms of occurrence of igneous rocks; · allocation of sites promising for various minerals, including oil and gas. The course work was completed by a second-year student of the group GIS-06 Belykh A.A. Chapter I. ORHYDROGRAPHY geological map stratigraphic section Two types of relief are distinguished on the territory of this region: mountainous relief (western part) and flat (eastern part). The maximum absolute mark - 885 m, is located in the southwest of the studied map. The minimum absolute mark is 580 m, located in the northeast. The relative elevation is 305 m. The relief is dissected by a river network, represented by the Abakan river basin, the Kiya river and its tributaries Chernavka and Syutik. The hydroelectric network of the territory is represented by the basin of the large river Abakan, which occupies the southern, central part of the map. The Abakan River takes its source from Lake Shira. It flows from south to north with a length of about 6 km and a width of about 400 m, and then turns to the southwest with a length of 5.5 km and a width of 400 m to 1 km. The Kiya River has two right tributaries: Chernavka, Syutik. Both tributaries flow to the west. The length of the Chernavka River within the map is 20 km and flows into Lake Shira, located in the southwest in the very left corner of the map under study. The length of the Syutik tributary is 6 km. In the east of the study area, there are two more tributaries of the Abakan River - the Mozhorka and an unnamed tributary that flows through almost the entire eastern part of the territory. The Kiya River and its tributaries have a calm character, as evidenced by the slight slope of the channel. On the territory, almost in the central part, there are two lakes - Lake Linevo and Lake Ingol, the distance between which is 5 km. The area of Lake Linevo is about 1 km2, and Lake Ingol is 240 m2. Near Lake Shira (to the west), Lake Ashpyl is located at a distance of 5 km, the area of which is about 480 m2. There are two settlements in the region. The village of Gorby is located in the eastern part, on the left bank of the Majorka River (a tributary of the Abakan). Shirypovo is located to the north locality Humps at 11.5 km. Gorby and Shirypovo are interconnected by a network of roads. There are no railroad tracks. In the west there is a state farm Krutoyarsky. Chapter II. STRATIGRAPHY IN geological structure The rocks of the Paleozoic and Mesozoic erathems take part in the territory of the map. Paleozoic formations occur monoclinally, almost parallel. The total thickness of the studied section is 12400 m. Paleozoic erathema - PZ Paleozoic deposits on the territory of the map are not ubiquitous and are exposed in the western part of the sheet. The Paleozoic erathema is represented by the Devonian and Carboniferous rock system. Devonian - D The Devonian system was established in the studied territory in the volume of the lower, middle and upper sections. The thickness of the Devonian deposits is 8170 m. Byskar series - D1-2bsk The rocks of the Byskar Series are exposed on the map in the northwestern and southwestern parts of the sheet. Unconformity is overlain by rocks of the Toltakov Formation (angular unconformity). The series is composed: in the upper part - andesitic porphyrites, volcanic breccias and tuffs of the same composition, subordinate horizons, composed of basaltic porphyrites; in the middle part - characteristic packs of red-brown tuffaceous sandstones; in the lower part - quartz porphyry, albitophyre, orthophyre, ignimbrite and felsic tuff. The thickness is 3800 m. Toltakov Formation - D2tl The rocks of the Tol'takovskaya Formation are exposed in the central and southern western half of the sheet on the territory of the map. The rocks are crumpled into a fold. The rocks of the Toltakovskaya Formation are conformably overlain by the rocks of the Saragashskaya Formation and unconformably overlie the rocks of the Byskarskaya Series. The Toltakovskaya Formation is composed of red and purple cross-bedded sandstones, siltstones, and conglomerates. The thickness is 200-400 m. Saragash Formation - D2sp The rocks of the Saragash Formation are exposed on the map in the southwestern, central, and northwestern parts of the western half of the sheet. Consistently they overlap with rocks of the Bey Formation and conformably overlie the rocks of the Toltakovskaya Formation. The Saragash Formation is composed of yellowish-gray, "millstone" sandstones, siltstones, marls, and limestones. The thickness is 150-420 m. Bey Formation - D2bs The rocks of the Bey Formation on the territory of the map are exposed in the southwestern, central, and northwestern parts of the western half of the sheet. Accordingly, they overlap with the rocks of the Frasnian stage of the Oidanovskaya suite and, according to them, overlie the rocks of the Saragash suite. The Bey Formation is composed of limestones with interlayers of gray sandstones, siltstones, mudstones, and marls. The layer thickness is 130-400m. Upper section - D3 The upper section of the Devonian system is identified in full and is represented by the Frasnian and Famennian stages. Oidanovskaya Formation - D3od The rocks of the Oidanovskaya Formation are exposed on the map in the southwestern, central, and northwestern parts of the western half of the sheet. Accordingly, they are overlapped by the rocks of the Kokhai suite and conformably lie on the rocks of the Bey suite. The Oidanovskaya suite is composed of red and purple cross-bedded sandstones and siltstones, less often argelites. The thickness is 150-750 m. Kohai Formation - D3kh The rocks of the Kokhai Formation on the territory of the map are exposed mainly in the central part of the western half of the sheet. Accordingly, they are overlapped by the rocks of the Famennian stage of the Tuba Formation and conformably overlie the rocks of the Oidanovskaya Formation. The Kokhai Formation is composed of red and green mudstones and siltstones with thin layers of gray limestones and sandstones. The thickness is 100-600 m. Tubin Formation - D3tb The rocks of the Tuba Formation on the territory of the map are exposed in the central part of the sheet. Accordingly, they overlap with the rocks of the Bystryanskaya suite of the lower part of the Carboniferous system of the Tournaisian stage and, according to them, overlie the rocks of the Kokhai suite. The Turbinsky Formation is composed of red sandstones, siltstones, and mudstones with interlayers of limestone gravelstones and conglomerates. The thickness is 250-800 m. Carboniferous system The Carboniferous system is distinguished in the volume of the lower section. The thickness of the deposits is 1930 m. Lower section - C1 In the lower part of the Carboniferous system, it is fully distinguished and is represented by the Tournaisian, Visean, and Namurian stages. Bystryanskaya Formation - С1bs The rocks of the Bystryanskaya Formation on the territory of the map are exposed in the southern, central, and northern parts of the western half of the sheet. Consistently they are overlapped by the rocks of the Altai suite and conformably lie on the rocks of the Turbine suite. The Bystryanskaya Formation is composed of yellowish-brown tuff sandstones, tuffites of sandstones and limestones. The thickness is 150-400 m. Altai Formation - С1al The pordes of the Altai Formation on the map are exposed in the southern part of the western half of the sheet. Accordingly, they are overlapped by the rocks of the Nadaltai Formation and conformably lie on the rocks of the Bystryanskaya Formation. The Altai Formation is composed of purple and yellow tuffites, tuff sandstones, sandstones, and limestones. The thickness is 180 m. Nadaltay Formation - С1nal The rocks of the Nadaltai Formation on the territory of the map are exposed in the southern part of the western half of the sheet. They overlap with the rocks of the Samokhvalskaya suite and consistently overlie the rocks of the Altai suite. The Nadaltai Formation is composed of gray tuff sandstones, tuffites, and limestones. Power is 160m. Samokhval Formation - С1sm The rocks of the Samokhval Formation on the territory of the map are exposed in the southern part of the western half of the sheet. They are unconformably overlain by the rocks of the lower coal-bearing suite of the Jurassic system of the lower section and conformably overlie the rocks of the Nadaltai suite. The Samokhvalskaya Formation is composed of green tuff sandstones and tuffites with subordinate layers of gravelstones and limestones. The thickness is 390 m. Mesozoic erathema - MZ Mesozoic deposits on the map are not distributed everywhere and are exposed in the eastern part of the sheet. The Mesozoic erathema is represented by the Jurassic and Cretaceous rock system. Jurassic - I The Jurassic system is highlighted in full the lower, middle and upper sections. The thickness of the deposits is 1700 m. Lower section - I1 Represented by the lower coal-bearing suite. Lower coal-bearing suite - I1 Middle coalless suite - I2 The rocks of the middle coalless suite on the territory of the map are exposed in the eastern part of the map with a northeast to southwest strike. Unconformably overlain by the rocks of the Upper coal-bearing suite and unconformably overlie the rocks of the middle coal-free suite. The middle coalless formation is composed of gray clayey sands, loose sandstones, and siltstones. The thickness is 500 m. Upper coal-bearing suite - I3 The rocks of the upper coal-bearing suite on the territory of the map are exposed in the eastern part of the map with a northeast-southwest strike. They are conformably overlain by the rocks of the Altash Formation of the lower part of the Cretaceous system of the Valanginian Stage and unconformably lie on the rocks of the Middle Coalless Formation. The upper coal-bearing suite is composed of gray clayey sands and sandstones with interlayers of siltstones and clays, in the lower part - interlayers and lenses of brown coals. Power is 500m Cretaceous system - K The Cretaceous system is not fully identified in the lower section. The thickness of the lower section in the Valanginian and Hauterivian stages is 600 m. Altash Formation - K1al The rocks of the Altash Formation on the territory of the map are exposed in the central southeastern part of the map. Accordingly, they are overlapped by the rocks of the Shestakovskaya suite and conformably lie on the rocks of the upper coal-bearing suite. The Altash Formation is composed of red clays, gray siltstones, and marls with interlayers of sands. The thickness is 400 m. Shestakovskaya Formation - K1sch The rocks of the Shestakov Formation on the territory of the map are exposed in the eastern part of the map. Accordingly, they lie on the rocks of the Altash suite. The Shestakovskaya Formation is composed of gray sands with lenses of calcareous sandstones. The thickness is 200 m. Quaternary - Q Quaternary QIV deposits are represented by modern deposits. Alluvial sands and pebbles. Quaternary deposits QIII2 are represented by Upper Quaternary deposits. Alluvial deposits of the second floodplain terrace: sands, pebbles. Chapter III. TECTONICS In tectonic terms, the studied area is located on the territory of a folded area. According to the results of analyzes of the geological map, stratigraphic column, geological section, two structural stages can be distinguished: 1) D1-2bsk - C1sm; 2) I2 - K1sch. As part of the first structural floor, two structural tiers can be distinguished. As part of the second floor, one structural tier with minor disagreements can be distinguished. First floor. lower structural layer. The lower structural stage is composed mainly of volcanic rocks: volcanic breccias, tuffs, and other rocks of volcanic activity. From this we can conclude that during this period there was a maximum explosive stage of volcanic activity. The rocks of this stage come to the surface in the northwestern, central, southwestern, and southeastern parts of the sheet. Separated in the volume of the Byskar series. The rocks of the lower tier are crumpled into sweetness. The first fold is located in the southwest. The apparent width of the fold is about 1 km, and the length is 7 km. Stretching from west to east. The type of fold is anticlinal, according to the ratio of the axes - linear. The core includes rocks of the Byskar series. On the wings of the rocks of the middle and late Devonian system. The fold is asymmetric, because the angles of incidence are different on the wings. The second fold is located in the central part of the sheet in the west. The rocks of the Byskar Series are also folded. The fold is approximately 1 km wide and 3 km long. The type of fold is anticlinal, according to the ratio of the axes - brachymorphic. The composition of the wings includes rocks of the middle and late Devonian system. The fold is asymmetric, because the angles of incidence are different on the wings. The third fold is located in the northwestern part of the sheet in the west. The core of the fold contains rocks of the Byskar series. The apparent width of the fold is about 7 km, and the length is 13 km. The type of fold is anticlinal, according to the ratio of the axes - linear. On the wings are rocks of the middle and late Devonian system. The fold is asymmetric. Upper structural layer. The upper structural stage is composed of terrigenous-carbonate sediments. The stage was formed under continental conditions. The stage is represented in the volume of the Toltakovskaya, Saragashskaya, Beyskaya, Oidanovskaya, Kokhaiskaya, Tubinskaya, Bystryanskaya, Altai, Nadaltayskaya and Samokhvalskaya formations. The deposits that make up this suite, mostly rocks, are exposed in the entire western part. There is volcanic activity in the Carboniferous period, which is represented by tuff sandstones. The rocks of this stage are crumpled into folds. The fourth fold is located in the central western part of the leaf. The fold is anticline. The core contains rocks of the Toltakov Formation, which are brachymorphic in terms of the ratio of the axes. The fold is asymmetric and broken by a fault with a fault. The wings of the fold are rocks of the Middle Devonian system. The fifth fold is located in the northern central part of the leaf. The fold is anticline, brachymorphic in relation to the axes. The core contains rocks of the Tol'takov Formation. On the wings are rocks of the middle and late Devonian system. The fold is asymmetric. The length of the fold is 1 km, the width is 1 km. Second floor. The structural stage is composed mainly of terrigenous sediments. This floor shows two small breaks in sedimentation in the eastern part. The deposits that make up this floor are distributed in the eastern part of the sheet. The rocks of this stage do not form folded structures. Chapter IV. HISTORY OF GEOLOGICAL DEVELOPMENT It is possible to restore the geological development of this territory from the early Devonian. Throughout the Byskar time, the territory was a coastal part of the sea basin. Sedimentation continued to accumulate until the end of the Byskar time, with volcanic-type sediments accumulating. There is volcanic activity here. At the end of the Byskar time, this territory was uplifted to a zone where sedimentation did not occur. Further, the territory experienced negative vibrations of the earth's crust. In Toltakov's time, the territory was a sea basin. At that time, terrigenous sediments accumulated. In the Saragash time of the Middle Devonian, the territory was a marine basin of shallow depth, where terrigenous sediments with marine fauna accumulated. In the Beyan time of the Middle Devonian, the territory also represented a marine basin of shallow depth, where terrigenous-carbonate sediments with the remains of marine fauna accumulated. Then there is a slight subsidence of the bottom of the sea basin. In the Oidanian time, the territory was a sea basin of shallow depth, where terrigenous sediments heated up. In the Kohai time of the Late Devonian, the territory was a marine basin. Terrigenous-carbonate sediments with an abundance of marine fauna accumulated here. In the Tuba time of the Late Devonian, the territory was a sea basin. Sediments of terrigenous-carbonate composition with marine fauna accumulated here. In the Bystryanka time of the Early Carboniferous, the territory was a marine basin of medium depth. Sediments with interlayers of sandstones and limestones with marine fauna accumulated here. In the Altai time of the Early Carboniferous, the territory was a sea basin. Volcanogenic-, terrigenous-carbonaceous sedimentation took place here. Volcanic activation is observed here, as evidenced by the accumulation of volcanic sediments. In the supra-Altai time, the territory began to represent the coastal part of the sea basin with small areas of land. Volcanogenic-carbonate sediments accumulated here. In the Samokhval time, a slight transgression of the sea occurred. The territory began to represent a sea basin of shallow depth. Volcanic sediments with interlayers of gravelstones and limestones with marine fauna accumulated here. Then there is a regression, a big break in sedimentation. Tectonic stability is observed, a continental regime has been established, which existed until the Early Jurassic. In the Early Jurassic, the territory was a low land, where terrigenous sediments with brown coal interlayers accumulated. After the Early Jurassic, there is a slight break in sedimentation in the eastern part. In the Middle Jurassic, the territory was also low land. Terrigenous sediments accumulated here. Further in the eastern part there is a break in sedimentation and the territory was a high land. In the Late Jurassic, the area was low land. Terrigenous sediments with interbeds of brown coal accumulated here. In the Altash time of the Early Cretaceous, the territory was a coastal part of the marine basin. Terrigenous-carbonate sediments with interlayers of sand accumulated here. In the Shestakovian time of the Early Cretaceous, the territory became a sea basin of shallow depth (lagoon). Predominantly sands with lenses of calcareous sandstones accumulated here. CONCLUSION As a result of the course work: we learned identify types of unconformity surfaces, analyze their significance for the geological history of a given territory; As a result of the course work, an analysis of the educational geological map No. 13 was carried out and the following conclusions were made: Two types of relief are distinguished on the territory of this region: mountainous relief (western part) and flat (eastern part). The relief is dissected by a river network, represented by the Abakan river basin, the Kiya river and its tributaries Chernavka and Syutik. As a result, it was found that rocks of the Paleozoic and Mesozoic erathems take part in the geological structure of the studied territory. The Paleozoic is represented by the Devonian, Carboniferous and Jurassic systems. The Mesozoic is represented by the Cretaceous system. In tectonic terms, the studied area is located at the late geosynclinal stage of development. According to the results of analyzes of the geological map, stratigraphic column, geological section, two structural stages can be distinguished: 1) D1-2bsk - C1sm; 2) I2 - K1sch. The rocks of the Paleozoic and Mesozoic erathems take part in the geological structure of the territory of the map. Paleozoic formations occur monoclinally, almost parallel. The total thickness of the studied section is 12400 m. REFERENCES 1. Gavrilov V.P. - General geology and geology of the USSR: Textbook for universities. - M.: Nedra, 2009. - 328 p. Minova N.P., Plyakin A.M. Construction and analysis of geological maps; guidelines- Ukhta, USTU: 2011 Mikhailov A.E. Laboratory works structural geology, geomapping and remote sensing; ed. Bosom , 1988 Mikhailov A.E. Structural geology and geological mapping.; ed. Bosom year 2014 Yubelt R., Schreiter P. Determinant of rocks; ed. World M: -1977