Internal shells of the earth diagram. What layers of earth does our earth consist of? (all layers are needed, from the core to the end)

Layers of the Earth pictures for children. The main condition is that the child has an interest in the topics that this science deals with. You can try to awaken your child's desire to learn more about our planet by watching cartoons, movies or children's programs on this topic.

When studying complex, voluminous topics, try to use visual teaching materials. A very good way is to make these manuals together with your child.

You can include a geography lesson on the structure of the Earth in your child’s education at home. To do this, you will need a cross-sectional drawing of our planet, indicating all its layers: the earth's crust, mantle, outer and inner core.

After this, you can invite your child to color and name the different layers in the drawing of the Earth on their own, as well as estimate its size; for this, the approximate diameter of the globe in kilometers is given below.

For greater clarity, prepare several drawings where all layers are black and white, and one is colored. Attach signs to such drawings with the name of the color layer and a brief description of it.

Also, prepare in advance four circles of different diameters from colored paper that matches the color of the layers of the Earth in your drawing. Invite your child to make his own model of the planet. Let him take circles from colored paper, match them with the signs, determining which layer of the Earth each of them corresponds to.

If the child has already learned to read, have him read out loud the corresponding tablet with a brief description. If not, read it yourself. Then you need to properly glue the circles and label all the layers. At the end, repeat all the new information again.

Geography is taught in a similar way to children who cannot yet understand and master too complex topics. Younger children will be interested in making their own model of our planet from a foam ball, painting it with watercolors or gouache. You can use a globe as a sample. First, tell them that the Earth is actually round, and the globe is a small copy of it. As you work, explain to your child that blue on the globe represents seas and oceans, brown represents mountains, green represents plains, and white represents ice.

Depending on how inquisitive your child is, delve into topics that interest him. With a hand-made model of the Earth, you can come up with various games for the development of children: for example, demonstrate how the planet rotates around the Sun and its axis and how night follows day.

Layers of the earth for children in pictures

The Earth is part of the Solar System along with the other planets and the Sun. It belongs to the class of rocky solid planets, characterized by high density and consisting of rocks, in contrast to gas giants, which are large in size and relatively low in density. Moreover, the composition of the planet determines the internal structure of the globe.

Basic parameters of the planet

Before we find out which layers are distinguished in the structure of the globe, let's talk about the main parameters of our planet. The Earth is located at a distance from the Sun of approximately 150 million km. The closest celestial body is the planet's natural satellite - the Moon, which is located at a distance of 384 thousand km. The Earth-Moon system is considered unique, since it is the only one where the planet has such a large satellite.

The earth's mass is 5.98 x 10 27 kg, the approximate volume is 1.083 x 10 27 cubic meters. cm. The planet revolves around the Sun, as well as around its own axis, and has an inclination relative to the plane, which determines the change of seasons. The period of revolution around the axis is approximately 24 hours, around the Sun - just over 365 days.

Mysteries of the internal structure

Before the method of studying the subsurface using seismic waves was invented, scientists could only make assumptions about how the Earth worked inside. Over time, they developed a number of geophysical methods that made it possible to learn about some of the structural features of the planet. In particular, seismic waves, which are recorded as a result of earthquakes and movements of the earth's crust, have found wide application. In some cases, such waves are generated artificially in order to become familiar with the situation at depth based on the nature of their reflections.

It is worth noting that this method allows you to obtain data indirectly, since it is not possible to directly get into the depths of the subsoil. As a result, it was found that the planet consists of several layers that differ in temperature, composition and pressure. So, what is the internal structure of the globe?

Earth's crust

The upper solid shell of the planet is called Its thickness varies from 5 to 90 km, depending on the type, of which there are 4. The average density of this layer is 2.7 g/cm3. The continental type crust has the greatest thickness, the thickness of which reaches 90 km under some mountain systems. They also distinguish between those located under the ocean, whose thickness reaches 10 km, transitional and riftogenic. The transitional one is distinguished by the fact that it is located on the border of the continental and oceanic crust. Rifted crust is found where mid-ocean ridges exist and is thin, reaching only 2 km.

The crust of any type consists of rocks of 3 types - sedimentary, granite and basalt, which differ in density, chemical composition and nature of origin.

The lower boundary of the crust is named after its discoverer, Mohorovicic. It separates the crust from the underlying layer and is characterized by a sharp change in the phase state of the substance.

Mantle

This layer follows the solid crust and is the largest - its volume is approximately 83% of the total volume of the planet. The mantle begins just after the Moho boundary and extends to a depth of 2900 km. This layer is further subdivided into the upper, middle and lower mantle. A feature of the upper layer is the presence of the asthenosphere - a special layer where the substance is in a state of low hardness. The presence of this viscous layer explains the movement of continents. In addition, when volcanoes erupt, the liquid molten substance they pour out comes from this particular area. The upper mantle ends at a depth of approximately 900 km, where the middle mantle begins.

Distinctive features of this layer include high temperatures and pressure, which increase with increasing depth. This determines the special state of the mantle substance. Despite the fact that the rocks have a high temperature in the depths, they are in a solid state due to the influence of high pressure.

Processes occurring in the mantle

The interior of the planet has a very high temperature, due to the fact that the process of thermonuclear reaction continuously occurs in the core. However, comfortable conditions for life remain on the surface. This is possible due to the presence of a mantle, which has heat-insulating properties. Thus, the heat released by the core enters it. The heated matter rises upward, gradually cooling, while cooler matter sinks down from the upper layers of the mantle. This cycle is called convection, it occurs non-stop.

Structure of the globe: core (outer)

The central part of the planet is the core, which begins at a depth of approximately 2900 km, just after the mantle. At the same time, it is clearly divided into 2 layers - external and internal. The thickness of the outer layer is 2200 km.

Characteristic features of the outer layer of the core are the predominance of iron and nickel in the composition, in contrast to the compounds of iron and silicon, of which the mantle mainly consists. The substance in the outer core is in a liquid aggregate state. The rotation of the planet causes the movement of the liquid substance of the core, which creates a powerful magnetic field. Therefore, the outer core of the planet can be called a generator of the planet’s magnetic field, which rejects dangerous types of cosmic radiation, thanks to which life could not arise.

Inner core

Inside the liquid metal shell there is a solid inner core, the diameter of which reaches 2.5 thousand km. At present, it is still not thoroughly studied, and there are disputes among scientists regarding the processes occurring in it. This is due to the difficulty of obtaining data and the possibility of using only indirect research methods.

It is known for certain that the temperature of the substance in the inner core is at least 6 thousand degrees, however, despite this, it is in a solid state. This is explained by the very high pressure, which prevents the substance from going into a liquid state - in the inner core it is supposedly equal to 3 million atm. Under such conditions, a special state of matter may arise - metallization, when even elements such as gases can acquire the properties of metals and become hard and dense.

In terms of chemical composition, there is still debate in the research community about which elements make up the inner core. Some scientists suggest that the main components are iron and nickel, others that the components may also include sulfur, silicon, and oxygen.

The ratio of elements in different layers

The composition of the earth is very diverse - it contains almost all the elements of the periodic table, but their content in different layers is heterogeneous. So, the lowest density, so it consists of the lightest elements. The heaviest elements are located in the core in the center of the planet, at high temperature and pressure, ensuring the process of nuclear decay. This ratio formed over time - immediately after the formation of the planet, its composition was presumably more homogeneous.

In geography lessons, students may be asked to draw the structure of the globe. To cope with this task, you need to adhere to a certain sequence of layers (it is described in the article). If the sequence is broken, or one of the layers is missed, then the work will be done incorrectly. You can also see the sequence of layers in the photos presented to your attention in the article.

Earth is perhaps one of the most unique planets in the Universe. We are the ones who have all the conditions for life and the development of civilization. How is our planet structured?

Basic layers of the Earth

If we consider the Earth from the very center up to the atmosphere, then it consists of four main layers:

• Mantle
• Atmosphere

These four layers create our planet. In addition, each main layer has its own layers.

Core

The core of the globe consists of two parts: the inner core and the outer core. The inner core, made of iron and nickel, has a radius of approximately 1,250 kilometers and a temperature of just over 6,000 degrees Celsius. The outer core is thicker - 2200 kilometers, and it consists exclusively of iron.

Mantle

The mantle, like the core, has two layers: the lower mantle and the upper mantle. The thickness of both layers is almost the same, in total it is about 2890 kilometers. Composition of the Mantle: silicate rocks (mainly iron and magnesium). The temperature of the mantle averages from 500 to 900 degrees Celsius, and near the core reaches up to 4000.

Bark

The thickness of the crust varies from 5 to 70 kilometers depending on the relief surface. It consists of various silicate rocks, mainly basalt. At the very top layers of the bark there is ordinary clay, which allows plants to give life.

Atmosphere

The Earth's atmosphere is divided into five layers at once: the troposphere, stratosphere, mesosphere, thermosphere and exosphere (in increasing order). The troposphere contains about 80 percent of all atmospheric air and clouds. The stratosphere is located at an altitude of 11 to 50 kilometers, having an average air temperature, and it is here that the ozone layer of the earth is located. The mesosphere layer begins at an altitude of 50 kilometers from the Earth and rises to 90 kilometers. In the mesosphere, the higher the altitude, the lower the temperature. The thermosphere and exosphere make up the bulk of the Earth's atmosphere (from 100 to 1,500 kilometers altitude). An interesting fact is that due to the fact that rarefied gas lives in the upper layers of the exosphere, some of the gases of the Earth’s atmosphere are transferred to space and vice versa. That is, we can say that our Earth exchanges gases with space.

The earth consists of different layers, which, in turn, consist of different materials, different in composition, weight, and density. The deeper inside the globe, the denser the layer. Let's consider layers from depth to surface:

1. Inner core - located in the very center of the Earth. It has a solid structure more than 5000 km thick and a temperature of 7000°C. Consists of iron and nickel.

2. Outer core - has a liquid structure of the same metals as the inner core. The thickness of the layer is approximately 5000 km, and the temperature is 5000°C.

3. The mantle is the widest layer. It has a total thickness of approximately 2900 km. The mantle is divided into:

The upper part has a solid structure.

The lower part (asthenosphere) is a viscous structure. It lies at a depth of 150 km under the continents and 15-150 km under the oceans.

4. The earth's crust is the topmost layer. It is a thin layer of hard rock. We go deeper to about 32-48 km under the continents and 5-8 km under the oceans. It contains potassium, aluminum, calcium, silicon, sodium.

Shell structure of the Earth. Physical state (density, pressure, temperature), chemical composition, movement of seismic waves in the interior of the Earth. Terrestrial magnetism. Sources of internal energy of the planet. Age of the Earth. Geochronology.

The Earth, like other planets, has a shell structure. When seismic waves (longitudinal and transverse) pass through the body of the Earth, their velocities at some deep levels change noticeably (and abruptly), which indicates a change in the properties of the medium passed by the waves. Modern ideas about the distribution of density and pressure inside the Earth are given in the table.

Changes in density and pressure with depth inside the Earth

(S.V. Kalesnik, 1955)

The table shows that in the center of the Earth the density reaches 17.2 g/cm 3 and that it changes with a particularly sharp jump (from 5.7 to 9.4) at a depth of 2900 km, and then at a depth of 5 thousand km. The first jump makes it possible to isolate a dense core, and the second - to subdivide this core into outer (2900-5000 km) and inner (from 5 thousand km to the center) parts.

Dependence of the speed of longitudinal and transverse waves on depth

Thus, there are essentially two sharp changes in velocities: at a depth of 60 km and at a depth of 2900 km. In other words, the earth's crust and inner core are clearly separated. In the intermediate belt between them, as well as inside the core, there is only a change in the rate of increase in speeds. It can also be seen that the Earth is in a solid state down to a depth of 2900 km, because Transverse elastic waves (shear waves) pass freely through this thickness, which are the only ones that can arise and propagate in a solid medium. The passage of transverse waves through the core was not observed, and this gave reason to consider it liquid. However, the latest calculations show that the shear modulus in the core is small, but still not equal to zero (as is typical for a liquid) and, therefore, the Earth's core is closer to a solid state than a liquid state. Of course, in this case, the concepts of “solid” and “liquid” cannot be identified with similar concepts applied to the aggregate states of matter on the ground surface: high temperatures and enormous pressures prevail inside the Earth.

Thus, the internal structure of the Earth is divided into the crust, mantle and core.

Earth's crust - the first shell of the Earth’s solid body, has a thickness of 30-40 km. By volume it is 1.2% of the volume of the Earth, by mass - 0.4%, the average density is 2.7 g / cm 3. Consists mainly of granites; sedimentary rocks are of subordinate importance in it. The granite shell, in which silicon and aluminum play a huge role, is called “sialic” (“sial”). The earth's crust is separated from the mantle by a seismic section called Moho border, from the name of the Serbian geophysicist A. Mohorovicic (1857-1936), who discovered this “seismic section”. This boundary is clear and is observed in all places on Earth at depths from 5 to 90 km. The Moho section is not simply a boundary between rocks of different types, but represents a plane of phase transition between eclogites and gabbros of the mantle and basalts of the earth's crust. During the transition from the mantle to the crust, the pressure drops so much that gabbro turns into basalts (silicon, aluminum + magnesium - “sima” - silicon + magnesium). The transition is accompanied by an increase in volume by 15% and, accordingly, a decrease in density. The Moho surface is considered the lower boundary of the earth's crust. An important feature of this surface is that in general terms it is like a mirror image of the topography of the earth's surface: under the oceans it is higher, under the continental plains it is lower, under the highest mountains it sinks lowest (these are the so-called roots of the mountains).

There are four types of the earth's crust; they correspond to the four largest forms of the Earth's surface. The first type is called mainland, its thickness is 30-40 km; under young mountains it increases to 80 km. This type of earth's crust corresponds in relief to continental protrusions (the underwater margin of the continent is included). The most common division is into three layers: sedimentary, granite and basalt. Sedimentary layer, up to 15-20 km thick, complex layered sediments(clays and shales predominate, sandy, carbonate and volcanic rocks are widely represented). granite layer(thickness 10-15 km) consists of metamorphic and igneous acidic rocks with a silica content of over 65%, similar in properties to granite; the most common are gneisses, granodiorites and diorites, granites, crystalline schists). The lower layer, the densest, 15-35 km thick, is called basalt for its resemblance to basalts. The average density of the continental crust is 2.7 g/cm3. Between the granite and basalt layers lies the Conrad boundary, named after the Austrian geophysicist who discovered it. The names of the layers - granite and basalt - are arbitrary; they are given according to the speed of passage of seismic waves. The modern name of the layers is somewhat different (E.V. Khain, M.G. Lomize): the second layer is called granite-metamorphic, because There are almost no granites in it; it is composed of gneisses and crystalline schists. The third layer is granulite-basite; it is formed by highly metamorphosed rocks.

Second type of earth's crust – transitional, or geosynclinal – corresponds to transition zones (geosynclines). Transition zones are located off the eastern shores of the Eurasian continent, off the eastern and western shores of North and South America. They have the following classical structure: a marginal sea basin, island arcs and a deep-sea trench. Under the basins of the seas and deep-sea trenches there is no granite layer; the earth's crust consists of a sedimentary layer of increased thickness and basalt. The granite layer appears only in island arcs. The average thickness of the geosynclinal type of the earth's crust is 15-30 km.

Third type - oceanic the earth's crust corresponds to the ocean bed, the thickness of the crust is 5-10 km. It has a two-layer structure: the first layer is sedimentary, formed by clayey-siliceous-carbonate rocks; the second layer consists of holocrystalline igneous rocks of basic composition (gabbro). Between the sedimentary and basaltic layers there is an intermediate layer consisting of basaltic lavas with interlayers of sedimentary rocks. Therefore, they sometimes talk about the three-layer structure of the oceanic crust.

Fourth type - riftogenic the earth's crust, it is characteristic of mid-ocean ridges, its thickness is 1.5-2 km. At mid-ocean ridges, mantle rocks come close to the surface. The thickness of the sedimentary layer is 1-2 km, the basalt layer in the rift valleys pinches out.

There are the concepts of “earth’s crust” and “lithosphere”. Lithosphere– the rocky shell of the Earth, formed by the earth’s crust and part of the upper mantle. Its thickness is 150-200 km, limited by the asthenosphere. Only the upper part of the lithosphere is called the earth's crust.

Mantle by volume it is 83% of the Earth's volume and 68% of its mass. The density of the substance increases to 5.7 g/cm3. At the boundary with the core, the temperature increases to 3800 0 C, the pressure - to 1.4 x 10 11 Pa. The upper mantle is distinguished to a depth of 900 km and the lower mantle to a depth of 2900 km. In the upper mantle at a depth of 150-200 km there is an asthenospheric layer. Asthenosphere(Greek asthenes - weak) - a layer of reduced hardness and strength in the upper mantle of the Earth. The asthenosphere is the main source of magma, where volcanic feeding centers are located and lithospheric plates move.

Core occupies 16% of the volume and 31% of the mass of the planet. The temperature in it reaches 5000 0 C, pressure – 37 x 10 11 Pa, density – 16 g/cm 3. The core is divided into an outer core, down to a depth of 5100 km, and an inner core. The outer core is molten and consists of iron or metallized silicates, the inner core is solid, iron-nickel.

The mass of a celestial body depends on the density of matter; mass determines the size of the Earth and the force of gravity. Our planet has sufficient size and gravity; it retains the hydrosphere and atmosphere. Metallization of matter occurs in the Earth's core, causing the formation of electric currents and the magnetosphere.

There are various fields around the Earth, the most significant influence on GO is gravitational and magnetic.

Gravity field on Earth it is the gravity field. Gravity is the resultant force between the force of attraction and the centrifugal force that occurs when the Earth rotates. Centrifugal force reaches its maximum at the equator, but even here it is small and amounts to 1/288 of the force of gravity. The force of gravity on earth mainly depends on the force of attraction, which is influenced by the distribution of masses inside the Earth and on the surface. The force of gravity acts everywhere on earth and is directed plumb to the surface of the geoid. The strength of the gravitational field decreases uniformly from the poles to the equator (at the equator the centrifugal force is greater), from the surface up (at an altitude of 36,000 km it is zero) and from the surface down (at the center of the Earth the gravity force is zero).

Normal gravitational field The shape of the Earth is what the Earth would have if it had the shape of an ellipsoid with a uniform distribution of masses. The real field strength at a specific point differs from normal, and a gravitational field anomaly occurs. Anomalies can be positive and negative: mountain ranges create additional mass and should cause positive anomalies, ocean trenches, on the contrary, negative ones. But in fact, the earth's crust is in isostatic equilibrium.

Isostasy (from the Greek isostasios - equal in weight) - balancing of the solid, relatively light earth's crust with a heavier upper mantle. The theory of equilibrium was put forward in 1855 by the English scientist G.B. Airy. Thanks to isostasy, an excess of mass above the theoretical equilibrium level corresponds to a shortage below. This is expressed in the fact that at a certain depth (100-150 km) in the asthenosphere layer, matter flows to those places where there is a lack of mass on the surface. Only under young mountains, where compensation has not yet fully occurred, are weak positive anomalies observed. However, the balance is constantly being disrupted: sediment is deposited in the oceans, and the ocean floor bends under its weight. On the other hand, mountains are destroyed, their height decreases, which means their mass decreases.

Gravity creates the shape of the Earth; it is one of the leading endogenous forces. Thanks to it, atmospheric precipitation falls, rivers flow, groundwater horizons are formed, and slope processes are observed. Gravity explains the maximum height of mountains; It is believed that on our Earth there cannot be mountains higher than 9 km. Gravity holds the gas and water shells of the planet together. Only the lightest molecules - hydrogen and helium - leave the planet's atmosphere. The mass pressure of matter, realized in the process of gravitational differentiation in the lower mantle, along with radioactive decay, generates thermal energy - a source of internal (endogenous) processes that rebuild the lithosphere.

The thermal regime of the surface layer of the earth's crust (on average up to 30 m) has a temperature determined by solar heat. This heliometric layer experiencing seasonal temperature fluctuations. Below is an even thinner horizon of constant temperature (about 20 m), corresponding to the average annual temperature of the observation site. Below the permanent layer, the temperature increases with depth - geothermal layer. To quantify the magnitude of this increase, two mutually related concepts. The change in temperature when going 100 m deep into the ground is called geothermal gradient(varies from 0.1 to 0.01 0 S/m and depends on the composition of rocks, the conditions of their occurrence), and the plumb distance to which it is necessary to go deeper in order to obtain an increase in temperature by 1 0 is called geothermal stage(varies from 10 to 100 m/ 0 C).

Terrestrial magnetism - a property of the Earth that determines the existence of a magnetic field around it caused by processes occurring at the core-mantle boundary. For the first time, humanity learned that the Earth is a magnet thanks to the works of W. Gilbert.

Magnetosphere – a region of near-Earth space filled with charged particles moving in the Earth’s magnetic field. It is separated from interplanetary space by the magnetopause. This is the outer boundary of the magnetosphere.

The formation of a magnetic field is based on internal and external reasons. A constant magnetic field is formed due to electric currents arising in the outer core of the planet. Solar corpuscular flows form the Earth's alternating magnetic field. Magnetic maps provide a visual representation of the state of the Earth's magnetic field. Magnetic maps are compiled for a five-year period - the magnetic era.

The Earth would have a normal magnetic field if it were a uniformly magnetized sphere. To a first approximation, the Earth is a magnetic dipole - it is a rod whose ends have opposite magnetic poles. The places where the dipole's magnetic axis intersects with the earth's surface are called geomagnetic poles. Geomagnetic poles do not coincide with geographic ones and move slowly at a speed of 7-8 km/year. Deviations of the real magnetic field from the normal (theoretically calculated) are called magnetic anomalies. They can be global (East Siberian Oval), regional (KMA) and local, associated with the close occurrence of magnetic rocks to the surface.

The magnetic field is characterized by three quantities: magnetic declination, magnetic inclination and strength. Magnetic declination- the angle between the geographic meridian and the direction of the magnetic needle. The declination is eastern (+), if the northern end of the compass needle deviates east of the geographic one, and western (-), when the arrow deviates to the west. Magnetic inclination- the angle between the horizontal plane and the direction of the magnetic needle suspended on the horizontal axis. The inclination is positive when the north end of the arrow points down, and negative when the north end points up. The magnetic inclination varies from 0 to 90 0 . The strength of the magnetic field is characterized by tension. The magnetic field strength is low at the equator, 20-28 A/m, at the pole – 48-56 A/m.

The magnetosphere has a teardrop shape. On the side facing the Sun, its radius is equal to 10 radii of the Earth; on the night side, under the influence of the “solar wind,” it increases to 100 radii. The shape is due to the influence of the solar wind, which, encountering the Earth’s magnetosphere, flows around it. Charged particles, reaching the magnetosphere, begin to move along magnetic field lines and form radiation belts. The inner radiation belt consists of protons and has a maximum concentration at an altitude of 3500 km above the equator. The outer belt is formed by electrons and extends up to 10 radii. At the magnetic poles, the height of the radiation belts decreases, and areas arise here in which charged particles invade the atmosphere, ionizing atmospheric gases and causing auroras.

The geographic significance of the magnetosphere is very great: it protects the Earth from corpuscular solar and cosmic radiation. Magnetic anomalies are associated with the search for minerals. Magnetic lines of force help tourists and ships navigate in space.

Age of the Earth. Geochronology.

The Earth arose as a cold body from an accumulation of solid particles and bodies like asteroids. Among the particles there were also radioactive ones. Once inside the Earth, they disintegrated there, releasing heat. While the size of the Earth was small, heat easily escaped into interplanetary space. But with the increase in the volume of the Earth, the production of radioactive heat began to exceed its leakage, it accumulated and heated the bowels of the planet, causing them to soften. The plastic state that opened up possibilities for gravitational differentiation of matter– floating of lighter mineral masses to the surface and gradual descent of heavier ones to the center. The intensity of differentiation faded with depth, because in the same direction, due to an increase in pressure, the viscosity of the substance increased. The earth's core was not captured by differentiation and retained its original silicate composition. But it thickened sharply due to the highest pressure, exceeding a million atmospheres.

The age of the Earth is determined using the radioactive method; it can only be applied to rocks containing radioactive elements. If we assume that all argon on Earth is a decay product of potassium-49, then the age of the Earth will be at least 4 billion years. Calculations by O.Yu. Schmidt gives an even higher figure - 7.6 billion years. IN AND. To calculate the age of the Earth, Baranov took the ratio between the modern amounts of uranium-238 and actinouranium (uranium-235) in rocks and minerals and obtained the age of uranium (the substance from which the planet later arose) of 5-7 billion years.

Thus, the age of the Earth is determined in the range of 4-6 billion years. The history of the development of the earth's surface can so far be directly reconstructed in general terms only starting from those times from which the oldest rocks have been preserved, i.e. for approximately 3 - 3.5 billion years (Kalesnik S.V.).

The history of the Earth is usually divided into two eon: cryptozoic(hidden and life: no remains of skeletal fauna) and Phanerozoic(explicit and life) . Cryptose contains two eras: Archean and Proterozoic. The Phanerozoic covers the last 570 million years, it includes Paleozoic, Mesozoic and Cenozoic eras, which, in turn, are divided into periods. Often the entire period before the Phanerozoic is called Precambrian(Cambrian - the first period of the Paleozoic era).

Periods of the Paleozoic era:

Periods of the Mesozoic era:

Periods of the Cenozoic era:

Paleogene (epochs – Paleocene, Eocene, Oligocene)

Neogene (epochs – Miocene, Pliocene)

Quaternary (epochs - Pleistocene and Holocene).

Conclusions:

1. All manifestations of the internal life of the Earth are based on the transformation of thermal energy.

2. In the earth’s crust, the temperature increases with distance from the surface (geothermal gradient).

3. The heat of the Earth has its source from the decay of radioactive elements.

4. The density of the Earth’s substance increases with depth from 2.7 on the surface to 17.2 in the central parts. The pressure in the center of the Earth reaches 3 million atm. The density increases abruptly at depths of 60 and 2900 km. Hence the conclusion - the Earth consists of concentric shells that embrace each other.

5. The earth's crust is composed primarily of rocks such as granites, which are underlain by rocks such as basalts. The age of the earth is determined to be 4-6 billion years.