What is a moraine and what types does it exist? Glacial deposits

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1. Formation of moraines

A moraine is an accumulation of coarse material formed during the movement of a glacier, which breaks down rocks and transports them down along its movement. The moraine includes shapeless rock fragments of various sizes from 10-15 meters to sand and clay. Ice accumulation in the mountains and its sliding occurs unevenly. The regime of glacier movement and the formation of moraines depends on the climate - the colder and wetter the climate, the more ice accumulates. In the Semirechye Mountains during the Pleistocene era, over the past 1.8 million years, two major glaciations (ice ages) occurred. The first and largest was of a cover nature - the ice covered the entire ridges. The second glaciation was a cover-valley glaciation - glaciers covered the central regions of the mountains and filled the valleys carved out by the first glaciation. The ice of the second glaciation dropped to a level of 1500 - 1700 meters above sea level. After these two major ice ages, the mountains acquired a familiar appearance - deep gorges and pronounced peaks, often with high sheer walls. During the Pleistocene, there were minor ice ages before, between, and after major ice ages. Almost all moraines of past ice ages were destroyed by the geological activity of subsequent glaciations. Currently, we can see the so-called ancient moraines of the last ice age, which took place between 40,000 - 10,000 years ago, and modern moraines of modern glaciers, which had their maximum volume and length in the 16th and 17th centuries.

Ancient moraines descend to a height of about 2500m, creeping into the main valleys from side gorges. Currently, they are overgrown with bushes and trees, including spruce woodland. Modern moraines are piles of bare stones stretching from glaciers. Ice remains in the depths of these moraines. Ice on the daytime surface appears higher at altitudes from 3000m (Northern Talgar glacier), more often from 3400-3500m. From the 19th century to the present, the climate has warmed, glaciers have retreated, exposing accumulations of stones - modern moraines.

If we turn to history, the word “moraine” was first used to refer to ridges and hills composed of boulders and fine earth and found at the ends of glaciers in the French Alps.

The composition of the main moraines is dominated by the material of deposited moraines, and their surface is a rugged plain with small hills and ridges of various shapes and sizes and with numerous small basins filled with lakes and swamps. The thickness of the main moraines varies widely depending on the volume of material brought by the ice.

The main moraines occupy vast areas in the USA, Canada, the British Isles, Poland, Finland, northern Germany and Russia. The areas around Pontiac (Michigan) and Waterloo (Wisconsin) are characterized by basal moraine landscapes. Thousands of small lakes dot the surface of major moraines in Manitoba and Ontario (Canada), Minnesota (USA), Finland and Poland. Terminal moraines form powerful, wide belts along the edge of the ice sheet. They are represented by ridges or more or less isolated hills up to several tens of meters thick, up to several kilometers wide and, in most cases, many kilometers long. Often the edge of the cover glacier was not smooth, but was divided into fairly clearly separated blades. The position of the glacier edge is reconstructed from the terminal moraines. Probably, during the deposition of these moraines, the edge of the glacier was in an almost motionless (stationary) state for a long time. In this case, not just one ridge was formed, but a whole complex of ridges, hills and basins, which noticeably rises above the surface of the adjacent main moraines. In most cases, the terminal moraines that are part of the complex indicate repeated small movements of the glacier edge.

Ancient moraines form mixtite horizons characteristic of platform covers and are called tillites.

2. Classification of moraines

A moraine refers to both glacial sediments currently being transported by a glacier and sediments that have already been deposited.

Therefore, when classifying moraines, moving and deposited moraines are distinguished.

According to the method of formation, moraines are divided into:

· Basic (bottom) moraines are rock fragments transported within the ice sheet and at its base. After melting and being released from under the ice, bottom moraines form an extensive and fairly even layer of moraine accumulations.

· Lateral moraines.

· Central moraines are formed as a result of the merger of glaciers.

· Terminal moraines - the formation of a transverse mound of debris in the area of ​​maximum glacier spread. They are often a natural cause of the formation of reservoirs of glacial origin.

3. Chemical composition of moraine

Clay moraine soils are polymineral formations. Hydromicas most often predominate in their clay fraction. Along with them, there is a significant amount of quartz, feldspars and other minerals, fine particles of which were formed by mechanical grinding of large fragments during the movement of ice. Water-soluble salts are present in small quantities or completely absent, as well as organic matter. A distinctive feature of clay moraine formations is their high density: usually from 1.80-1.90 to 2.20-2.30 g/cm 3 . The porosity of these soils is low - usually 25-35% (but more often 30% or much lower). Such a high compaction of the clay pounds under consideration is explained primarily by the compacting pressure of the glacier during the formation of morainic strata. The high compaction was largely due to the great heterogeneity of the granulometric composition of the bog pounds.

The high density, naturally, largely determined the low compressibility: in general, the indicators of physical and mechanical properties characterize the moraine as a dense, weakly compressible pound. Compressibility moduli obtained from compression tests in the load range of 0.1--0.3 MPa are in the range from 6 to 10--15 and even 20 MPa. For loads of 0.3--0.4 MPa, their values ​​are usually more than 10 MPa. The porosity coefficient for moraine loams lies in the range of 0.3--0.45, and for moraine sandy loams - 0.4--0.5. The shear resistance of moraine pounds is usually quite high: moraine loams have cohesion C = 0.08...0.19 MPa, internal friction angle cp = 18...42°, moraine sandy loams, respectively, C = 0.08...0.001 MPa And<р = 12...35°.

It should be noted that morainic loams and clays, although they have significant water resistance, still get wet in water and are washed away by water. This ability of sinking pounds sometimes causes deformations of slopes and the bottom of excavations and pits. In engineering-geological practice, moraine clay pounds are in most cases considered reliable foundations for the most critical and heavy structures, due to their dense composition, very low porosity and compressibility.

Among the fluvioglacial (fluvioglacial) clay deposits, the most typical are band clays, widely known in engineering-geological practice. Their formation occurred in periglacial lakes, into which water flowed at varying rates throughout the year. With the rapid flow of water and its abundant flow into the lakes in the summer, layers with a large content of sand (sandy) were deposited, and in the winter, with a slow movement of water and its insignificant flow into the lakes, clay layers were formed. As a result, the formation of peculiar sandy-clayey strata occurred, characterized by clearly defined ribbon layering.

Band clays are characterized by high porosity (up to 60-65%) and high natural humidity. Often natural humidity is higher than the upper limit of plasticity, which means that under natural conditions the described clays are in a latent flow state. The banded structure gives these fluvioglacial deposits a clearly defined anisotropy in relation to a number of properties. In particular, their water permeability, which is generally low in band clays, is significantly higher along the bedding than perpendicular to it.

Thus, in sandy and silty layers, which mainly create the possibility of filtration, along the bedding the filtration coefficient kf = 1 -10 -1, 1 10 -3 m/day, and in clay layers it decreases by approximately two orders of magnitude, i.e. i.e. up to 110 5 m/day. Due to the low water permeability, draining the water-saturated layer of ribbon clays is an extremely difficult engineering task and is not always feasible. Band clays in their natural state can withstand loads of up to 0.3--0.4 MPa without significant deformation, even if their natural moisture content exceeds the upper limit of plasticity. Repeated alternation of loading and unloading within these limits imparted, according to a number of experts, elastic properties to the ribbon clays.

It was also noted that after the natural composition of the rock is disrupted by crushing it, accompanied by the transition of the soil from a latent flowing state to a fluid one, a sharp decrease in strength properties is observed, as well as a decrease in deformation indicators. This indicates the presence of internal bonds between particles in ribbon clays, which impart additional strength to the rock, despite its high natural humidity. This is facilitated by the presence of trivalent elements such as iron and aluminum among the exchangeable cations in ribbon clays.

The shear strength of banded clays depends on the location of the shear surface: if the shear surface is located in sandy layers, then the shear resistance value is much higher than if this surface passes through clay layers. In addition, due to the anisotropy of the rock, this resistance varies with the direction of the shear force relative to the bedding surface.

For example, for water-saturated ribbon clays, the angle of internal friction, determined in the pressure range of 0.1--0.2 MPa parallel to the layering, is equal to 11--13° for clay layers. For dusty ones: 15--19°, for sandy ones - about 24°. With a shift of perpendicular layering, this angle is on average 16°. Cohesion in clay layers is 0.02--0.03 MPa, in silty layers - 0.007--0.017 MPa. When the natural structure is disrupted, the adhesion as such is not fixed.

Thus, band clays are characterized by the presence of clearly defined band layering, high porosity, high natural humidity, fairly high strength with natural composition, the value of which drops sharply when it is disrupted, and a clearly expressed anisotropy of properties.

4. Engineering-geological features of lacustrine clay deposits.

Lake clays and loams have a relatively limited distribution. They are usually thin-layered, less often lenticular-layered. Their distinctive feature is a significant content of organic matter, and, as a rule, the plant remains in them are poorly decomposed, which is most often observed in highly dispersed clays. Any clay minerals can be found in lacustrine clay rocks; halloysite and hydromicas play a predominant role. Autogenous non-clay minerals include limonite and other iron oxides, pyrite, marcasite, carbonates, and sometimes minerals consisting of aluminum oxides.

According to the conditions of their formation, lacustrine sediments very much depend on the general characteristics of the reservoir (lake), its nutrition, the presence of inflowing rivers carrying various terrigenous material, on the hydrological parameters of the lake and watercourses flowing into it, the nature, composition and conditions of occurrence of rocks in which there is a lake. Nevertheless, the mentioned features of the composition and structure of lacustrine clay sediments are quite typical. High porosity and significant organic content, as well as high natural humidity, determine the low engineering-geological characteristics of lake sediments, such as strength and compressibility. Perhaps only low water permeability will give them some positive connotation. About fine earth moraine

As is known, the “moraine” of the Russian Plain consists of more than 90-95% (and sometimes almost 100%) of fine earth (clay, sandy loam, sand); only isolated boulders and pebbles are noted in it. The gravel fraction (which for some reason is usually classified as coarse material) makes up several percent. Therefore, it is important to know the origin of the fine earth “moraine”.

When studying the “moraine” of the Leningrad region, I.P. Gerasimov and K.K. Markov (1939) established that in areas where the bedrock is represented by blue Cambrian clays, the moraine is clayey and bluish in color; to the south of the klint, in the zone of development of Silurian limestones, there is a crushed stone moraine, very carbonate (limestone rikhk). In the field of Devonian red-colored sandstones there is a sandy, red-colored moraine.

A direct relationship between the mineral composition of the fine earth “moraine” and the underlying rocks was also established in Estonia. According to A.V. In Raukas, in the “moraine” overlying carbonate Ordovician and Silurian rocks, the amount of carbonate material sharply increases. Directly to the south, in the area of ​​development of Devonian sandstones, the carbonate material almost disappears, but the “moraine” is enriched with quartz and feldspars, as well as zircon, tourmaline, and rutile. These mineral associations are characteristic of sandstone weathering crusts.

In Lithuania, according to A.Yu. Klimashauskas, the bulk of the fine earth “moraine” from the fine sand to clay fraction is composed of minerals borrowed from the underlying sedimentary rocks.

According to research by S.D. Astapova, in Belarus there are four large mineralogical provinces: northern (Poozerie), western (Ponemanye), eastern (Dnieper region), southern (Polesie), within which “moraines” are characterized by certain associations of terrigenous minerals. Within these provinces, there are also smaller areas with a characteristic mineralochemical composition of the sand-clay fraction. Based on the similarity of the mineral and trace element composition of the pre-Cenozoic formations and the “moraine”, S.D. Astapova comes to the conclusion that local rocks have a strong influence on the composition of “moraines” with local feeding provinces.

Research by M.F. Veklich in Ukraine also showed that the “fine-earth moraine fraction” is strongly dependent on the composition of the underlying preglacial sediments. According to M.F. For Veklich, this indicates the enormous role of local rocks, in particular loess, as sources of nutrition for glacial deposits.

Thus, on the Russian Platform, as well as on the Baltic Shield, the fine earth of the “moraine” is of local origin. In any case, there is no basis for claims about the transport of fine earth by glaciers from Fennoscandia.

5. Granulometric composition of the “moraine”

It has long been known that in the “moraine” of the Russian Platform, together with boulders of sedimentary rocks, there is an admixture of boulders of Precambrian crystalline rocks. The content of these boulders is insignificant, but among them there are blocks sometimes up to 2-3 m in diameter. It is on these boulders and blocks, regardless of their size, that the doctrine of cover glaciations of our plains is based.

But before moving on to the fundamental question of the actual origin of boulders and blocks of Precambrian rocks, let us dwell on the amount of coarse material in the “moraine” on the Russian Platform and, if possible, clarify what percentage in relation to boulders of sedimentary rocks are boulders of Precambrian rocks.

In the monograph by A.A. Kagan and M.A. Solodukhin “Moraine deposits of the north-west of the USSR” (1971) presents the results of numerous granulometric analyzes of the “main moraines” of the Kola Peninsula, Karelia, Arkhangelsk, Vologda, Leningrad, Pskov, Novgorod regions and Belarus.

The results of granulometric analyzes are directly related to the problem under consideration.

As follows from analytical data, on the Baltic shield (Kola Peninsula and Karelia), the “moraine” contains from 11 to 25% of boulders, and the sizes of these boulders (and blocks) vary from 100 mm to 3-4 m in diameter (Kagan, Solodukhin, 1971), but large boulders are not included in the samples, which reduces the number of boulders. In the pebble fraction (100-10 mm), the content of crystalline rock fragments ranges from 10-25%. Thus, the coarse fraction makes up 21-50% of the “moraine” volume. At the same time, in the south of Karelia, where the crystalline basement is covered by a sedimentary cover, the content of boulders drops to zero, and the coarse fraction is represented by fragments measuring 100-10 mm (9-19%). Although it cannot be ruled out that a small percentage of boulders are still present in the South Karelian moraine, they were not included in the samples.

The amount of boulder material in the “moraines” of the Arkhangelsk and Vologda regions sharply decreases and disappears almost to nothing. In fact, the small boulder fraction in the samples is combined with the pebble fraction (10 mm) and their total content is about 1% of the “moraine” volume. At the same time, the number of boulders of crystalline rocks is 10 times less - 0.1%.

There is also a sharp decrease in coarse material in the “moraines” of the Leningrad, Pskov, and Novgorod regions - i.e. immediately south of the Baltic Shield. Here the small boulder fraction (100-10 mm) is combined with the pebble fraction and together they make up from 0 to 3% of the “moraine” volume. Boulders are also present in these moraines, but in insignificant quantities and are practically not included in the samples.

A small number of boulders are also present in the “moraine” of Belarus, where only traces of them are noted, and clastic material measuring 0.2-1 cm is contained in an amount of 7%.

Accordingly, the admixture of small fragments of Precambrian rocks in these areas is less than these already insignificant percentages.

The content of coarse material in the “moraine” of Ukraine varies widely - from 0% to 40% (Veklich, 1961). On the left bank of the Dnieper, boulders come from local sedimentary rocks and are found in small quantities, while in the “moraine” lying on the rocks of the Ukrainian shield, there are many boulders and they are represented by crystalline rocks, the size of individual boulders is up to 18 - 19 m3 (Zamoriy). According to tradition, the boulders of crystalline rocks that make up the “moraine” are also considered here to have been brought by the glacier from Fennoscandia (Veklich, 1961; Dorofeev, 1965).

The presented materials definitely indicate the genetic connection of coarse clastic material and fine earth “moraines” with local bedrock on the vast expanses of the East European Platform, including its protrusion - the Baltic Shield.

At the same time, the issue of finding erratic boulders and erratic pebbles, represented by Precambrian crystalline rocks, in “moraines” requires a solution. The glacial theory solves this problem simply: the boulders were brought by a cover glacier.

moraine glacier lake clay

Bibliography

1. Shantser E.V., Essays on the doctrine of genetic types of continental sedimentary formations, M., 1966.

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Lateral and bottom moraines

Moraine- a genetic type of glacial deposits created directly by a glacier. It is a heterogeneous mixture of clastic material - from giant blocks, up to several hundred meters in diameter, to clayey material formed as a result of grinding of debris during glacier movement.

Morena most researchers refer to both glacial sediments currently being transported by a glacier and sediments that have already been deposited. Therefore, when classifying moraines, they distinguish moving and delayed. The last row is called till by researchers. According to the method of formation, moraines are divided into:

• Basic (bottom) moraines- rock fragments transported within the ice sheet and at its base. After melting and being released from under the ice, bottom moraines form an extensive and fairly even layer of moraine accumulations.
• Lateral moraines.
• Central moraines- are formed as a result of the merger of glaciers.
• Terminal moraines- formation of a transverse embankment of debris in the area of ​​maximum glacier spread. They are often a natural cause of the formation of reservoirs of glacial origin.

Some moraines move near the ice surface. These include lateral moraines, which form along the edges of the glacier, and middle moraines, which form when two lateral moraines merge. Other moraines are transported at the base of the ice sheet. As the ice moves, they break, rub against the bed and are ground. Hard rocks such as granite are sunk into sand, while soft rocks (such as shales) are ground into fine clay. Boulder clay is often deposited on horizontal sheets.

Large boulders can be transported by a glacier for many kilometers while remaining intact. In a new place they look like foreign bodies, often resting on other rocks, and therefore are called erratic (literally, unstable).

The elongated clay mounds are called drumlins. They are composed of masses of boulder clay, which are shaped and smoothed by the ice rushing over them. The drumlins of Northern Ireland are some of the largest in the world: some of them are more than 1.5 km long and 60 m high.

Word " moraine" was first used to refer to ridges and hills composed of boulders and fine earth, found at the ends of glaciers in the French Alps. The composition of the main moraines is dominated by the material of deposited moraines, and their surface is a rugged plain with small hills and ridges of various shapes and sizes and with numerous small basins filled with lakes and swamps. The thickness of the main moraines varies widely depending on the volume of material brought by the ice.

Major moraines occupy vast areas of former glaciation: in the USA, Canada, the British Isles, Poland, Finland, northern Germany and Russia. The areas around Pontiac (Michigan) and Waterloo (Wisconsin) are characterized by basal moraine landscapes. Thousands of small lakes dot the surface of major moraines in Manitoba and Ontario (Canada), Minnesota (USA), Finland and Poland.

At the front (tongue) of a glacier, sediments often accumulate and form ridge, or terminal, moraines. They occur in ablation zones—areas where the edge of a glacier melts over time. Thus, terminal moraines mark the boundaries of the last, or furthest, advance of ice. Terminal moraines form powerful, wide belts along the edge of the ice sheet. They are represented by ridges or more or less isolated hills up to several tens of meters thick, up to several kilometers wide and, in most cases, many kilometers long. Often the edge of the cover glacier was not smooth, but was divided into fairly clearly separated blades. The position of the glacier edge is reconstructed from the terminal moraines. Many researchers believe that during the deposition of these moraines, the edge of the glacier was in a weakly mobile (stationary) state for a long time. In this case, not just one ridge was formed, but a whole complex of ridges, hills and basins, which noticeably rises above the surface of the adjacent main moraines. In most cases, the terminal moraines that are part of the complex indicate repeated small movements of the glacier edge.

Ancient moraines form mixtite horizons characteristic of platform covers and are called

Moraine

Moraine

glacial deposits formed as a result of the accumulation of clastic (moraine) material in the body of a glacier during its movement, plowing out of the bed and subsequent melting. The composition is extremely diverse - from loams to large boulders; very poor sorting; large fragments - pebbles and boulders are dotted with glacial scars, their individual edges are covered with polishing. There are moving, or mobile, and deposited moraines. Among moving– superficial (lateral and median), internal and bottom. Among the superficial ones are lateral and median. Deposited moraines consist of an accumulation of debris left behind by a glacier after its retreat, and are formed from all types of moving moraines; are divided into main (bottom and ablative), local (local), pressure, etc. Collectively, the deposited moraines make up a flat accumulative relief in the area of ​​glacier melting: hilly-western, formed by the main moraine, moraine plains - ridged, wavy or flat surfaces, also formed by a main moraine; relief of finite moraine ridges, drumlin relief. In the mountains, moraines are represented by various forms of lateral moraines, ridges of terminal moraines and the hilly-moraine relief of main moraines. A unique dynamic type is pressure moraines, formed as a result of the pressure of the glacier body. There are pressure moraines, expressed and not expressed in the modern relief. The former are usually represented by swell-like terminal-moraine accumulations at the edge of the glacier. The latter are established by geological methods: by crushed layers of bottom moraine in outcrops and the presence of rocks of the glacial bed.

Geography. Modern illustrated encyclopedia. - M.: Rosman. Edited by prof. A. P. Gorkina. 2006 .

Synonyms:

See what “morena” is in other dictionaries:

MORAINE, deposits of stones and rock fragments accumulated by GLACIERS during their movement. Some rock fragments are the result of erosion; some may have resulted from freezing and thawing activities; some are... ... Scientific and technical encyclopedic dictionary

Moraines, w. [fr. moraine] (geol.). An accumulation of rock fragments and boulders moved from mountains by moving glaciers. Large dictionary of foreign words. Publishing house "IDDK", 2007. morena y, zh. (French moraine). An accumulation of rock fragments... ... Dictionary of foreign words of the Russian language

- (French moraine), an accumulation of rock fragments carried or deposited by glaciers... Modern encyclopedia

- (French moraine) sediments accumulated directly by glaciers during their movement and plowing out of the bed; very diverse in composition (from loams to boulders), unsorted, containing pebbles and boulders with glacial scars and polishing. IN… … Big Encyclopedic Dictionary

Debris transported or deposited by a glacier... Geological terms

- (from French moraine * a. moraine; n. Morane; f. moraine; i. morena) accumulation of unsorted clastic material transported or deposited by glaciers. Accordingly, a distinction is made between moving, or mobile, and deferred M. Moving M... Geological encyclopedia

MORENA, moraines, female. (French moraine) (geol.). An accumulation of rock fragments and boulders moved from mountains by moving glaciers. Ushakov's explanatory dictionary. D.N. Ushakov. 1935 1940 ... Ushakov's Explanatory Dictionary

MORENA, s, female. (specialist.). An accumulation of rock fragments formed by the movement of glaciers. | adj. moraine, oh, oh. M. landscape. Ozhegov's explanatory dictionary. S.I. Ozhegov, N.Yu. Shvedova. 1949 1992 … Ozhegov's Explanatory Dictionary

Franz. a ridge of boulders gradually moved from the mountains by moving glaciers; ridge, mane, dump. Dahl's Explanatory Dictionary. IN AND. Dahl. 1863 1866 … Dahl's Explanatory Dictionary

Noun, number of synonyms: 5 goddess (346) marzhana (2) material (306) ... Synonym dictionary

- (French moraine), an accumulation of unsorted rock fragments brought and deposited by glaciers. Ecological encyclopedic dictionary. Chisinau: Main editorial office of the Moldavian Soviet Encyclopedia. I.I. Dedu. 1989 ... Ecological dictionary

Books

• , Morena Morana. “The time of men slaughtering mammoths is over. Santa Claus has been invented, the fairy godmother has flown away to warm countries and will never return. No one else will decide anything for you. There will be no DADDIES... eBook
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what is moraine?

1. Glacial deposits
2. moraine
3. A moraine is a trace of a glacier that has left behind almost impassable stone placers...
4. Moraine (from the French moraine - sediments) is glacial deposits accumulated directly by glacier ice.

   The word moraine was first used to describe the ridges and hills of boulders and fine earth found at the ends of glaciers in the French Alps. The main moraines are dominated by deposited moraine material, and their surface is a rugged plain with small hills and ridges of various shapes and sizes and with numerous small basins filled with lakes and swamps. The thickness of the main moraines varies widely depending on the volume of material brought by the ice.

   Basic moraines. The word moraine was first used to describe the ridges and hills of boulders and fine earth found at the ends of glaciers in the French Alps. The main moraines are dominated by deposited moraine material, and their surface is a rugged plain with small hills and ridges of various shapes and sizes and with numerous small basins filled with lakes and swamps. The thickness of the main moraines varies widely depending on the volume of material brought by the ice.
   The main moraines occupy vast areas in the USA, Canada, the British Isles, Poland, Finland, northern Germany and Russia. The areas around Pontiac (Michigan) and Waterloo (Wisconsin) are characterized by basal moraine landscapes. Thousands of small lakes dot the surface of major moraines in Manitoba and Ontario (Canada), Minnesota (USA), Finland and Poland.

   Terminal moraines form powerful, wide belts along the edge of the ice sheet. They are represented by ridges or more or less isolated hills up to several tens of meters thick, up to several kilometers wide and, in most cases, many kilometers long.

5. The sea is a geological body composed of glacial deposits.

   It is an unsorted mixture of clastic material of various sizes, from gigantic blocks of outliers with a diameter of up to several hundred meters, to clayey material formed as a result of grinding of debris by a glacier during its movement.

   Based on the method of formation, moving moraines are divided into:

   * Basic (bottom) moraines are rock fragments transported within the ice sheet and at its base. After melting and being released from under the ice, bottom moraines form an extensive and fairly even layer of moraine accumulations.
   * Lateral moraines.
   * Central moraines are formed as a result of the merger of glaciers.

   Ancient moraines form mixtite horizons characteristic of platform covers and are called tillites.

6. GLACIAL DEPOSITS
7. Either a fish or a sea snake
8. glacial deposits
9. An accumulation of rock fragments formed by the movement of glaciers
10. fr. Moraine
    Moraine is sediment accumulated directly by glaciers during their movement and plowing out of the bed. The moraines are very diverse in composition, unsorted, containing pebbles and boulders with glacial scars and polishing. Various glacial relief forms (mesorelief) are formed on moraine deposits: hills, ridges, depressions, etc.
    Depending on the conditions of formation and position relative to the glacier body, surface, internal and bottom moraines are distinguished. Surface moraines are divided into lateral or coastal moraines and median moraines.
    : http://www.glossary.ru/cgi-bin/gl_sch2.c ...
11. Rock mounds brought by the glacier
12. There is such a fish
13. moraine or moray eel?
14. A moraine is a geological body composed of glacial deposits.

    Moraine is the name given to glacial sediments, both those currently being moved by the glacier and the sediments that have already been deposited by it. Therefore, when classifying moraines, moving and deposited moraines are distinguished.

Sediments accumulated directly by glacier ice. The most common are the main moraines, which form under the ice due to the gouging of the bed during the movement of the glacier. Lithologically very diverse (from boulders to loams and clays), always unsorted, containing sparsely scattered pebbles and boulders, including erratic ones with glacial grinding and scars. The long axes of the boulders are oriented in the direction of glacier movement. Layering is usually absent, but is sometimes imitated by banding associated with the alternating supply of destruction products of rocks of different compositions. Clayey varieties of moraine are characterized by high compaction and low porosity, sometimes schistosity. Local main moraines consist mainly of local material. Basic moraines are in places replaced or overlapped by ablative moraines (thawing moraines), formed mainly due to the material contained inside and on the surface of the glacier during its degradation. They have a coarse, usually gravelly or sandy composition, and in some places they are unclearly layered due to washing by melt water.

Source: Geological Dictionary, M: "Nedra", 1978.

Moraine(French moraine) - sediments accumulated directly by glaciers during their movement and plowing out of the bed; very diverse in composition (from loams to boulders), unsorted, containing pebbles and boulders with glacial scars and polishing.

Source: Soviet Encyclopedic Dictionary

A moraine refers to both glacial sediments currently being transported by a glacier and sediments that have already been deposited. Therefore, when classifying moraines, moving and deposited moraines are distinguished. According to the method of formation, moraines are divided into:

• Basic (bottom) moraines are rock fragments transported within the ice sheet and at its base. After melting and being released from under the ice, bottom moraines form an extensive and fairly even layer of moraine accumulations.
• Lateral moraines.
• Central moraines are formed as a result of the merger of glaciers.
• Terminal moraines are the formation of a transverse mound of debris at the site of maximum glacier spread. They are often a natural cause of the formation of reservoirs of glacial origin.

The word moraine was first used to describe the ridges and hills of boulders and fine earth found at the ends of glaciers in the French Alps. The composition of the main moraines is dominated by the material of deposited moraines, and their surface is a rugged plain with small hills and ridges of various shapes and sizes and with numerous small basins filled with lakes and swamps. The thickness of the main moraines varies widely depending on the volume of material brought by the ice.

Terminal moraines form powerful, wide belts along the edge of the ice sheet. They are represented by ridges or more or less isolated hills up to several tens of meters thick, up to several kilometers wide and, in most cases, many kilometers long. Often the edge of the cover glacier was not smooth, but was divided into fairly clearly separated blades. The position of the glacier edge is reconstructed from the terminal moraines. Probably, during the deposition of these moraines, the edge of the glacier was in an almost motionless (stationary) state for a long time. In this case, not just one ridge was formed, but a whole complex of ridges, hills and basins, which noticeably rises above the surface of the adjacent main moraines. In most cases, the terminal moraines that are part of the complex indicate repeated small movements of the glacier edge.