_{1}

^{*}

The geotemperature gradient is considered as taking main part in generating the Earth’s magnetic field. It is shown that geotemperature gradient functions as a generator of both nuclear and mantle thermoelectrical currents thanks to the great temperature difference between the core and the mantle. The movement of those currents is close to the radial direction towards the Earth’s crust. However, the nuclear thermocurrents movement tends to cyclically change into opposite one. If the mantle and core thermocurrents move oppositely, the Earth’s crust cools down globally and ice age comes, but if they move unidirectionally then global warming comes. The calculation show that the Earth’s surface can warm up to not more than 10°C. The latter, considering how human factor affects the warming of Earth, is incomparably great. There are calculations that show power of the Earth’s thermocurrents being enough to generate and maintain the Earth’s magnetic field, its modern dynamics and the poles inversion.

At the present time, the most elaborate theory of substantiating electrical currents generation in the planet’s metal core is based on hydromagnetic dynamo which works on the self-excitation principle. There are a lot of theoretical and experimental works to prove this model [

Besides, based on the browsed professional reviews and works [

Nevertheless, even in the first half of the last century there were attempts to explain the Earth’s magnetic field with thermoelectromotive forces existing in the core, which are conditioned by turbulent convective movements of the core’s liquid [

There is another reminder of thermoelectrical currents’ role in forming magnetic fields of hot CP stars and, probably, planets in a work of A. Z. Dolginov, where the scientist got the equation of field generation [

∂ B ∂ t = [ ∇ , [ v B ] ] + c 2 4 π [ ∇ , ( 1 σ [ ∇ , B ] ) ] − [ ∇ , [ j B ] e N e ] − c [ ∇ η , ∇ T ] (1)

(where η is thermoelectrical coefficient).

He thought that the forth from right member [ ∇ η , ∇ T ] was different from zero and generated the star’s magnetic field, whereas the first three members could be neglected because they were small and could not be performed at the considered model of moving unmagnetized plasm. His calculations showed that the dipole field of a star on its surface can be about 10^{−}^{4} T. Unfortunately, A. Z. Dolginov never presented a detailed theory of making magnetic fields of space objects with thermoelectrical currents, which are immanent to “hot” objects.

Below, there is the third attempt to reanimate geothermoelectrical currents below. It is shown on the example of Earth that those geothermocurrents, moving directionally inside the conducting shells (the core and the lower mantle) and affected by the great difference of geotemperatures, can generate not raw but real powerful magnetic fields of Earth and other “hot” planets of the solar system, because the phenomenon is universal.

That attempt is based on the results of geophysical field work for many years, experimental and academic research, which let the author elaborate a new model of thermo-electrochemical nature of the Earth’s core natural electric field [

Hereinafter all the calculations of a planet’s magnetic field are based on the known physical laws and known scientific data of inner structure and physical properties of Earth. The results show that the actual Earth’s thermoelectrical currents generate and maintain the current geomagnetic field by themselves. Besides, it is the first time when a model specifies complexity of the geomagnetic field, which consists of two parts: main magnetic field of the metal core and additional field of the lower mantle.

Accordingly, the schematic geothermoelectrical model (protomodel) of the Earth’s magnetic field is considered for the first time in the author’s article [

To form the geomagnetic model one should procced from the known scientific data of the planet’s shells thicknesses, temperature values in the shells and their borders. For example, most of the researchers hold on to the following defining temperatures in the body of our planet: on the depth of about 100 km the temperature is close +1800 K, on the depth of about 400 km (C layer, phase transition zone) the temperature is +1900 K, on the “mantle-core” border the temperature is +4000, …, +5000 K, in the core center the temperature is (+5000, …, +6230) ± 500 K [^{6} S・m^{−1} [

That data implies that the globe can be presented as a spherical geothermoelecrical element (further, SGTE) (_{Т} can be calculated [

Δ φ T = ∫ T 1 T 2 β d T (2)

where β is the averaged temperature coefficient, which is 0.0001 V・deg^{−1}. for pure metals, while it is 0.0015 V・deg^{−1}. for some semiconductors [

To find the parameters of the lower mantle thermocurrents I_{top} the following must be known:

- thermofield intensity E_{T};

- electron concentration per unit volume of the lower mantle ores (it equals n =

10^{20} m^{−3} by default);

- electron gas drift velocity v d ;

- electron mean free path in a semiconductor l;

- current density j.

According to the (2), the maximum thermo-EMF Δφ_{Т} for SGTE is 0.45 V, and the electric field intensity can be found from the following equality:

E T = Δ φ T / l SGTE , V / m ; (3)

where l SGTE is SGTE radius length, which equals the distance between the planet center and the middle part of the C shell and is defined as 5438 km or 5650 km to the upper mantle.

Hence, the electric field Е_{Т} generated by the existing temperature difference ΔТ makes planetary flows of “hot” electrons move directionally from the planet center to its outer shells along the radii. At the same time the electron quantity (concentration) in a volume unit of metal (Fe) can be calculated with the formula [

n = ρ N A / A , m − 3 , (4)

where ρ is the metal Fe density in the inner core, (12.2 g・cm^{−3}); N_{A} is the Avogadro constant, 6.02 × 10^{23} mol^{−1}; A is atomic mass Fe (55.847 g). Substituting that data into the (4) we get n = 1.32 × 10 29 m − 3 . n should be compared to the calculation for the real conditions when electron gas is in free state at pressures p, that corresponds to the metal core, i.e. at p = 3.55 million atm [

n = ( 5 m е ℏ 2 ( 3 π 2 ) − 2 / 3 ) 3 / 5 p 3 / 5 (5)

Knowing that electron mass m e = 9.11 × 10 − 31 kg and p = 3.59 × 10 11 Pa a new magnitude can be found n = 3.25 × 10 29 m − 3 . Despite there is a slight discrepancy between magnitudes n_{i} (just 2.5 times), the magnitude n = 3.25 × 10 29 m − 3 is used for the further calculations, as it meets the real planet conditions most. In its turn, the total sum of electron gas in the metal core is defined as

m Σ = 4 3 π R c 3 m е n = 5.09 × 10 19 kg .

The same must be performed for the lower mantle, spherical shell circle thickness is Δ R l m = 2.22 × 10 6 m , n = 1 × 10 20 m − 3 (average value for semiconductors from 5 × 10^{19} m^{−3} to 5 × 10^{20} m^{−3} [

To calculate the electron gas drift velocity v d , according to the quantum theory of the electrical conductivity of metals, the following formula should be used [

v d = e E T l 2 m v , m ⋅ s − 1 , (6)

where e is the effective electron charge, C (1.6 × 10^{−19}); m is the effective electron mass, kg (0.91 × 10^{−30}); l is the electron mean free path, it equals

l = σ ℏ ( 3 π 2 ) 1 / 3 e 2 n 2 / 3 , m ; (7)

where σ is the planet’s core electroconductivity, S/m;

ħ is the Plank’s constant, 1.05 × 10^{−34}, J・s;

v is the average velocity of electrons thermal movement, it can be derived from the formula:

v = 8 k T π m , m ⋅ s − 1 (8)

where k is the Boltzmann constant, 1.38 × 10^{−23} J/K;

As seen, it is necessary to calculate the velocity of the electron thermal movement at T = 6000 K preliminary, according to (8), to calculate Е_{Т} and the electron mean free path l between their concussions with the crystal cell to find v d . l directly depends on the metal core’s electroconductivity , which can be taken as 10^{5} S/m as the smallest magnitude from the above interval (0.1 ÷ 1.0) × 10^{6} S・m^{−1}. Substituting the corresponding values into (8), (7) and (6) one will get v = 4.81 × 10 5 m ⋅ s − 1 , l = 2.7 × 10 − 11 m and drift velocity of the electron gas flow v d = 4.79 × 10 − 13 m ⋅ s − 1 respectively. The value Е_{Т} of the latter was 9.73 × 10^{−}^{8} V/m: {(0.0001 (В × K^{−}^{1}) × 5500(K)/(5650 × 10^{3})(м)} for the interval “metal core center-lower mantle-1/2 of the C shell”. To calculate Е_{Т} two parameters were used: 1) radius of the shells G + F + E + D + 1/2C, which is about 5650 km, and 2) the temperature difference ΔТ between the planet center and the middle border of the C shell, which is close to 5500 K.

The density of the lower mantle thermoelectrical currents j can be found from the formula, according to [

j = e 2 n E T l p F (9)

where p F is Fermi momentum, defined as:

p F = ℏ ( 3 π 2 n ) 1 3 , (10)

Now the lower mantle thermocurrents I_{top} must be quantified, as well as the amplitude of the magnetic field they generate. The following must be taken into consideration: 1) the ores are semiconductors, 2) the specific conductance of the mantle solid ores (semiconductors) is a way lower than the core’s one, and it is 0.1 ÷ 10.0 S・m^{−1} [^{−1} [^{20} m^{−3} [

Then the total value of the lower mantle thermocurrents I_{top}, coming through its outer spherical surface S_{D} with the radius R_{D} can be derived from the following formula:

I t o p = j S D , (11)

And, finally, according to the Biot-Savart-Laplace law, the Earth’s magnetic induction B Т Т t o p on the bottom surface equator can be calculated:

d B Т Т t o p = μ 0 I t o p d R D sin 90 ∘ 4 π R Earth 2 (12)

However, the magnetic moment of the current element I t o p d R D is considered here only in a one-dimensional space towards the current movement along the radius R D . Integration over d R D allows to find the total of the current elements I t o p R D just along the way R D . This won’t go for our case, when the radial currents, like I_{low}, move from the source (sphere’s center) to the interface with the lower mantle spherical surface, directed azimuthally from 0 to 4π in a spherical conductor. There is no decision on valuation magnetic induction when currents move radially in a spherical conductor in technical literature.

That’s why it is better to consider the following model. A small spherical conductor with the radius d R i is put into the spherical conductor with the radius R Σ . The currents, moving from the spheres center make a magnetic field in the volume of the initial small sphere. That field is always directed to its volumetric surface tangentially. Then, according to the circulation theorem,

d B ⋅ 4 3 πd R i 3 = μ 0 μ r I i ⋅ 4 πd R i 2 where the currents I i , coming through the small

sphere surface 4 πd R i 2 . When the current is distributed evenly over the sphere’s

section I i = I l o w ( d R i R Σ ) 2 . Hence, after substituting and shortening, here is the

Biot-Savart formula for calculating the magnetic field induction inside the sphere (metal core) as the following rationalized form:

d B Т Т l o w = 3 μ 0 μ r I l o w d R i 4 π R Σ 2 or B Т Т l o w = 3 μ 0 μ r I l o w R Σ 4 π R Earth 2 sin α , (13)

where R Earth is the Earth’s radius, R Σ is the metal core radius.

In its turn, the magnetic field on the Earth’s surface for the lower mantle spherical layer can be calculated with considering the thickness of that layer ΔR_{D}, which is denoted as d R D in (12).

B Т Т t o p = 3 μ 0 μ r I t o p Δ R D 4 π R l m 2 sin α (14)

The heat Q, which is produced in the lower mantle V_{lm} because thermocurrents interact with active resistance of this mantle’s ores. It can be found from the following formula [

Q l m = 1 σ j 2 V l m Δ t (15)

where j is the current density in the lower mantle, A・m^{−2}; σ is the lower mantle’s electroconductivity Sm^{−1}; Δ t is the time of producing heat for 31,536,000 c (year); V l m is the volume of the lower mantle’s spherical circle.

All the calculations for the lower mantle, including the used constants, are tabulated to

As seen from the table, the value of the magnetic induction B T T t o p on the Earth’s surface is ~4.62 × 10^{−6} T, which is much lower than the really measured for the same terrestrial conditions В 0 = 3.4 × 10 − 5 T . The heat Q, which is produced in the lower mantle volume and determined by thermocurrents I_{top}, is 2.84 × 10^{14} J per year (2.84 × 10^{21} erg per year), and this is much lower than the thermal heat loss of the planet per year, which is determined by the value of 3 × 10^{21} J per year (3 × 10^{28} erg per year).

Analogic calculations were performed for the thermocurrents I_{low} moving under the influence of thermoelectrical field Е_{Т} inside the metal core according to (3) too. To calculate its value two main parameters were taken into consideration: 1) the metal core radius, which is 3500 km (sum of thicknesses of the inner core, of the transitive F zone and the outer core) and 2) the discussed below difference of temperature ΔТ between the center of the planet and the border “core-lower mantle”.

According to the literary sources the magnitude ΔТ is for the metal core is quite uncertain and fluctuates within extreme values from 0 K to 1957 K ± 227 K. At the same time, it is known from the same sources that such factors as pressure, electroconductivity, thermal conductivity in the metal core are particularly high, and the electron concentration doesn’t practically depend on tem-

Constants and calculated parameters | Units | Used formulas, their numbers | Calculation results |
---|---|---|---|

μ_{0} | H/m | 1.26 × 10^{−6} | |

Distance between the middle point of the lower mantle layer and the bottom surface, R_{нм} | m | 6.37 × 10^{6} | |

Radius of the lower mantle outer surface, R_{D} | m | 5.68 × 10^{6} | |

Lower mantle layer thickness, ΔR_{D} | m | 1.9 × 10^{6} | |

Spherical surface S_{D} area with radius R_{D} | m^{2} | S D = 4 π R D 2 | 4.05 × 10^{14} |

Thermofield Е_{T} density in the lower mantle D at ΔT = 4000˚C | V/m | Е T = β ⋅ Δ T / Δ R D , (3) where β = 0.0003 V/deg. | 1.58 × 10^{−7} |

Plank’s constant, ħ | J・s | 1.05 × 10^{−34} | |

Electron concentration in a unit volume of the lower mantle ores, n | m^{−3} | 1.0 × 10^{20} | |

Electron charge, е | C | 1.6 × 10^{−19} | |

Electron mass, m_{е} | kg | 9.1 × 10^{−31} | |

Lower mantle electroconductivity, σ | S/m | 0.4 | |

Fermi momentum, p_{F} | m・kg/s | p F = ℏ ( 3 π 2 n ) 1 / 2 (10) | 1,51 × 10^{−27} |

Electron mean free path, l | nm | l = σ ℏ ( 3 π 2 ) 1 / 3 e 2 n 2 / 3 10 9 (7) | 0.237 |

Current density, j | A/m^{2} | j = e 2 n E T l p F (9) | 6.34 × 10^{−8} |

Total amount of current of lower mantle D coming through the S_{D} surface, I_{top} | А | I t o p = j S D (11) | 2.57 × 10^{7} |

Magnetic induction on the Earth’s bottom surface B Т Т t o p (according to the measurements, В_{0} is 3.4 × 10^{−5} T on the equator) | T | B Т Т t o p = 3 μ 0 I t o p Δ R D 4 π R н м 2 sin α (14) | 4.62 × 10^{−6} |

The heat, emitted in the lower mantle by the thermocurrents I_{top} in a year, Q l m | J・year | Q l m = 1 σ J 2 V l m Δ t (15) | 2.84 × 10^{14} |

perature [^{9})^{−}^{1} years [

Now let us calculate electric, magnetic and thermal parameters of the solid core, which has temperature dynamics. To do this, let us use the mentioned formulas (2)-(11) (13) (15).

In particular, we must use the initial data when calculating:

μ 0 μ Fe = 1.26 × 10 − 6 H / m ;

Earth’s radius, R Earth = 6.37 × 10 6 , m ;

Inner core radius, R G = 1.4 × 10 6 , m ;

Total radius, R Σ = R G + Δ R F + Δ R E = 3.65 × 10 6 , m ;

Spherical surface S_{G} area with radius R_{G}: = 4 π R G 2 = 2.46 × 10 13 , m;

Core electroconductivity, σ = 5.0 × 10 5 S / m .

From the formulas (3) (4) (5) (7) (9) (10) accordingly we have:

Thermofield density of the Earth’s core at the temperature difference ΔT = 10˚C and radius R_{Σ} Е T = 2.86 × 10 − 10 V / m ;

Electron concentration in a unit volume of metal (Fe), n 1 = 1.32 × 10 29 m − 3 , n 2 = 3.25 × 10 29 m − 3 ;

Fermi momentum, p F = 1.41 × 10 − 23 m ⋅ kg / s ;

Electron mean free path, l = 0.85 nm.

Substituting the corresponding meanings of the calculated parameters to the current density formula (9), we get j = 1.43 × 10 − 4 A / m 2 . From the formula (11) we can find the total amount of current of the inner core G: I l o w = j S G = 3.52 × 10 9 A .

According to the formula (15) let us additionally calculate the heat Q b c produced by the thermocurrents I_{low}, which is 2.25 × 10^{14} J year (2.25 × 10^{21} erg per year) and is comparable with the thermocurrents I_{top} heat in magnitude. There is also a calculation of the Earth’s magnetic momentum M = 4 π R G 2 I l o w , which is 8.67 × 10^{22} А・m^{2} when the current I_{low} is 3.52 × 10^{9} А and the spherical surface at the solid core radius is R_{G} = 1400 km. That is close to the known magnitude М = 8.2 × 10 22 А ⋅ m 2 .

For the readers’ convenience, all the calculations are presented in the compact

The table shows that the thermocurrents I_{low} are all-sufficient, they are able not only generate the main dipole field of Earth В T T l o w , but to maintain it for a long time at 3.64 × 10^{−5} T level. This value is calculated for the points of Earth on its equator and, as seen, it is close to the real and modern intensity of the EMF. At the same time, the heat, produced by the thermocurrents I_{low}, is only Q b c = 2.25 × 10 14 J per year (2.25 × 10^{21} erg per year) and is comparable to the heat of the thermocurrents I_{top}. The Earth’s magnetic moment was also calculated as M = 4 π R G 2 I l o w . At the current I_{low} of 3.52 × 10^{9} А and spherical surface with the solid core’s radius of R_{G} = 1400 km (see in ^{22}

Constants and calculated parameters | Units | Used formulas, their numbers | Calculation results |
---|---|---|---|

μ_{0}μ_{Fe}, where μ_{Fe} = 1 (Т above the Curie point) | H/m | 1.26 × 10^{−6} | |

Earth’s radius, R Earth | m | 6.37 × 10^{6} | |

Inner core radius, R_{G} | m | 1.4 × 10^{6} | |

Total radius, R Σ = R G + Δ R F + Δ R E | m | 3.65 × 10^{6} | |

Spherical surface S_{G} area with radius R_{G} | m^{2} | S G = 4 π R G 2 | 2.46 × 10^{13} |

Thermofield Е_{T} density of the Earth’s core at the temperature difference ΔT = 10˚C and radius R_{Σ} | V/m | Е T = β Δ T / R Σ , (3) where β = 0.0001 V/deg. | 2.86 × 10^{−10} |

Plank’s constant, ħ | J・s | 1.05 × 10^{−34} | |

Electron concentration in a unit volume of metal (Fe), | m^{−3} | n = ρ N A / A 4) n = ( 5 m е ℏ 2 ( 3 π 2 ) − 2 / 3 ) 3 / 5 p 3 / 5 (5) | 1.32 × 10^{29 } 3.25 × 10^{29} |

Electron charge, е | C | 1.6 × 10^{−19} | |

Electron mass, m_{е} | kg | 9.1 × 10^{−31} | |

Core electroconductivity, σ | S/m | 5.0 × 10^{5} | |

Fermi momentum, p_{F} | m・kg/s | p F = ℏ ( 3 π 2 n ) 1 / 2 (10) | 1.41 × 10^{−23} |

Electron mean free path, l | nm | l = σ ℏ ( 3 π 2 ) 1 / 3 e 2 n 2 / 3 10 9 (7) | 0.85 |

Current density, j | A/m^{2} | j = e 2 n E T l p F (9) | 1.43 × 10^{−4} |

Total amount of current of the inner core G, Bordered by the S_{G} surface, I_{low} | A | I l o w = j S G (11) | 3.52 × 10^{9} |

Magnetic induction on the Earth’s bottom surface B Т Т l o w (according to the measurements, В_{0} is 3.4 × 10^{−5} T on the equator) | T | B Т Т l o w = 3 μ 0 I l o w R Σ 4 π R З 2 sin α (13) | 3.64 × 10^{−5} |

The heat, emitted by the thermocurrents I_{low} at movement to the lower mantle per year, Q b c | J・year | Q b c = 1 σ J 2 V b c Δ t (15) | 2.25 × 10^{14} |

А・m^{2}, which is close to the known value М = 8.2 × 10 22 А ⋅ m 2 .

Let us briefly note, that a toroidal magnetic field forms within the metal core. The field’s field lines are spherical circles that do not leave the conducting core (_{Т} have been generating a through channel with electron deficit for 3.5 billion years in the toroidal field in the core center. The channel is the entrance/exit for the poloidal magnetic field which is self-generating in the conductive medium. The field is definitely dipole and it has local poles with diameter to 500 km for entrance/exit of the field lines bundles of the poloidal field with tilt of 90^{0} - 89^{0}. There is a confirmation for it [

First, let us pay attention to a feature of the core: its outer part (outer core) is in a melted state at the temperature T_{0}, whereas the inner part (inner core), divided with the transitive F zone, is in a solid state, but at the lowered temperature T_{i}. Hence, we can conclude that the solid core can be colder than the outer one, and its temperature is T_{i} = T_{0} ? 10 K. In its turn, it shows that there obviously must be geotemperature gradients, directed oppositely to the melted outer core. Those gradients generate thermoelectric currents “outer core-lower mantle” I_{top}, directed oppositely to the Earth’s surface, and “outer core-inner (solid) core’s center” I_{low} to the planet’s center (_{i} is expected to get T_{0}, and then get higher than T_{0} i.e. T_{i} > T_{0}. Such happens when the flows of the thermocurrents I_{low} move to the Earth’s center and their electron concentration n in the inner core because of the absence of drains (outer borders) and, consequently, absence of dissipation of the charge energy. As a result, current density increases, which contributes to higher producing of Joule heat and its accumulation in the Earth’s central part. Eventually, the inner core’s temperature T_{i} reaches the temperature of the melted core T_{0} (T_{i} = T_{0}) and at this moment the field intensity Е_{Т} gets equal to zero (Е_{Т} = 0) in the “outer core-inner core” branch. From that very moment thermocurrents I_{low} stop moving, and the Earth’s dipole magnetic field disappears, but the lower mantle magnetic field В T T l o w remains.

Nevertheless, thermocurrents I_{low} of low intensity are able to not only appear for a short time and several times but change their directions to the opposite ones, because the thermal process is not homogeneous at different points of the inner core.

The inner core temperature eventually gets higher and reaches a persistent state T_{i} > T_{0} because of the thermal process inertia. At this state thermocurrents of opposite direction instantly appear and signs of the inner SGTE charges finally change (_{i} = T_{0} thermocurrents I_{top} and I_{low} move to the Earth’s surface unidirectionally and their mutual current I sums up. Ores of the lower mantle gets extra heat because a part of the thermocurrents I_{low} permeates in. That heat spreads predominantly to the bottom surface’s side, and when it is reached, the Earth’s crust and atmosphere reach the mode of dynamic heating gradually. From the other hand, electron flows leave the core, and it slowly cools down after electron concentration gets less. But when the moment of the persistent state T_{i} < T_{0} comes, a new and opposite process begins-thermocurrents I_{low} go to the inner core and warm it. At the same time the mutual current I decreases and Earth comes into its cooling mode, and the dipole magnetic field restores. The cycles repeat.

The results of the calculations in _{low} (^{5} ÷ 10^{6} years [^{−6} T at any reversal sign.

In this connection, there can be made a preliminary estimate of the time interval Δt between adjacent coinciding phases of I_{top} and_{ }I_{low} thermocurrents movement, for example, to the Earth’s crust. In this case that interval can correspond to the period of two maximum Earth warmings or cooling if the thermocurrents move in an antiphase direction (

That can be represented by the following model of multidirectional movements of thermocurrents I_{low} towards the persistently unidirectional movement of thermocurrents I_{top}:

1^{st} cycle: core-lower mantle; 2^{nd} cycle: lower mantle-core; 3^{rd} cycle: core-lower mantle.

For a quantitative estimation of the model one should take into consideration drift velocity v d (7) of electrons, which move directionally in the electric field Е_{Т} from the inner core’s side to the upper mantle (1^{st}, 3^{rd} cycles) and backwards (2^{nd} cycle).

However, that velocity is average and it is defined from the interval v d between 0 and max. But if the velocity of an electron after the collision has nothing to do with its velocity before the collision [

v d = e E T l m v (6а)

However the existing scientific argument if it is right to use the formula (6) or the formula (6a) can be resolved only in course of time and only by comparing theoretical calculations with the practice.

All the calculations to define warming periods are in

Constants and calculated parameters | Units | Used formulas, their numbers | Calculation results |
---|---|---|---|

Number of seconds in a year, С | s | 31,536,000 | |

The core radius + lower mantle, R | m | 5.65 × 10^{6} | |

Thermofield Е_{T} density in the interval core G-transition zone С at ΔT = 5530 K | V/m | Е T = β ⋅ Δ T / R , (3) where β = 0.0003 V/deg. | 2.94 × 10^{−7} |

Plank’s constant, ħ | J・s | 1.05 × 10^{−34} | |

Electron concentration in a unit volume of the lower mantle, n | m^{−3} | It is presumed, that the density of n in the lower mantle increases to 3.25 × 10^{22} when е moves from the core to the mantle | 3.25 × 10^{22} |

Electron charge, е | C | 1.6 × 10^{−19} | |

Electron mass, m | kg | 9.1 × 10^{−31} | |

Core electroconductivity, σ | S/m | 8.3 × 10^{4} | |

Fermi momentum, p_{F} | m・kg/s | p F = ℏ ( 3 π 2 n ) 1 / 2 (10) | 1.04 × 10^{−26} |

Electron mean free path, l | nm | l = σ ℏ ( 3 π 2 ) 1 / 3 e 2 n 2 / 3 10 9 (7) | 1039 |

Average velocity of electron thermal motion in a semiconductor v, м/с | m/s | ~10^{5} | |

Drift velocity of the electron flow in the field Е_{T} | m/s | v d = e E T l m v (6,а) | 5.36 × 10^{−7} |

Time from the 1st cycle beginning till its end, t_{1} | year | t 1 = R G / ( v д ⋅ C ) | 8.29 × 10^{4} |

Time from the 1st cycle beginning till the end of the 3^{rd} cycle, t_{1-3} | year | t_{1-3} = 3t_{1} | 2.49 × 10^{5} |

All the calculations to define warming periods are in

It is seen from ^{−1}, as in ^{−1}. for semiconductors instead of 0.0015 V deg^{−1}. [

Periods of cooling and warming cycles also change noticeably, if n for the lower mantle ores is increased only by 1 order, i.e. n = 3.25 × 10 23 m − 3 (the initial value for calculations is taken as n = 3.25 × 10 22 m − 3 ). Then the period of direct warming is about 385,000 years, and the time lapse between the consecutive warmings Δt is now about 1.15 million years.

It appears from the roughly evaluative calculations, that despite the large range of numbers they are still within the assumptive time intervals, which the researchers get by an indirect analysis of geologic and climatological material of our planet, accumulated numerously [

To solve the task, we should consider the following conditions. Earth is now under a steady nonequilibrium thermodynamic state, because there are pressure and temperature gradients, that can be concluded from the I. R. Prigogine’s work [_{low} of the solid and the melted cores move to the lower mantle. Their velocity, defined by the electron velocity, is about 2 × 10^{−8} m・s^{−1}, and their distance, for example, for 10^{3} years is not more than 60 - 70 km. That thin shell layer, being in the “core-mantle” border zone, is warmed to 4510 K (the initial temperature on the line of 4500 K) by the heat of the core Q thermocurrents (see _{1}. Let us take the temperature of the Earth’s bottom surface as Т_{2} = 273.1 K.

In this connection, a simplified heat-exchanging model of Earth can be represented as a hollow spherical shell with two sides. One of them is the inner one with radius R Σ = 3.65 × 10 6 m , corresponding the surface of the

section “core-lower mantle”. The other one is the outer side with radius R Earth = 6.37 × 10 6 m , corresponding the bottom surface. The inner side is affected by the inner core heat Q b c = 2.25 × 10 14 J year (see ^{−}^{1} [_{1} = 283.1 K (10˚C), and the outer side is Т_{2} =273.1 K (0˚C) at the beginning, but after heating it gets Т_{2} = Х K.

To find Т_{2} the homogeneous differential heat equation in spherical coordinates can be used [

∇ 2 T = d 2 T d r 2 + 2 r d t d r = 0 (16)

Nevertheless, these values of interglacial periods (warming) or cooling can be essentially clarified, if there was exact data of the β coefficient value for not only pure metals, but different materials of the planet’s shells, more complicated ones.

Here are the border conditions:

if r = R Σ , T = T 1 ; if r = R Earth , T = T 2 ; } (17)

Then at the predetermined border conditions the solution of the Equation (16) is the temperature field Equation (17) in the spherical layer of Earth:

T ( r ) = T 1 − T 1 − T 2 1 R Σ − 1 R Earth ( 1 R Σ − 1 r ) , R Σ ≤ r ≤ R Earth (18)

Fourier’s law should be used to find the amount of the heat Q, coming through the spherical surface S_{D} per unit time [

Q = − λ d T d r S D = − λ 4 π r 2 d T d r (19)

Let us denote the temperature gradient d T / d r from (18). If we substitute it to the (19), a new expression can be derived [

Q = 4 π λ ( T 1 − T 2 ) 1 R Σ − 1 R Earth = 2 π λ ( T 1 − T 2 ) 1 d Σ − 1 d Earth = π λ d Σ d Earth ( T 1 − T 2 ) (20)

The temperature T 2 can be found with that expression, if the heat Q is known:

T 2 = T 1 − Q δ π λ d Σ d Earth (21)

where δ = ( d Σ + d Earth ) 2 is the spherical layer “lower mantle-bottom surface”

thickness;

Q = Q b c = 2.25 × 10 14 / 31536000 = 7.13 × 10 6 J .

Substituting the corresponding parameter values into (21) gives us increasing of the temperature on the bottom surface by T 2 = 273.2 K when the heat of the core I_{low} thermocurrents affects the lower mantle permanently. As seen, the minor difference between T 2 and T 1 9.92 K can be explained by the fact, that the spherical layer thickness is not great, not much more than 0.37 at the correlation thickness/diameter of the warmed side.

However, to check the calculated T 2 , a more accurate analytical solution of the task of determining the temperature inside the sphere and on its surface at any moment of time should be used [

T ( X , F o ) = T 1 + 2 [ T ( X , 0 ) − T 1 ] ∑ n = 1 ∞ ( − 1 ) n + 1 sin ( δ n X ) δ n X exp [ − ( δ n ) 2 F o ] (22)

where F o = λ ⋅ τ c ′ p R 2 is Fourier’s number;

Λ 1 = ( − 1 ) n + 1 sin ( δ n X ) X is the lambda function;

X = r / R is the dimensionless radial coordinate of a random point of the sphere;

r is the radial coordinate a random point of the sphere, m;

R is the inherent size of the sphere body, m;

τ is the time, s;

c ′ p = ρ ⋅ c p is the specific volumetric isobaric heat capacity of the lower mantle ores, which is distributed over both the upper mantle and the Earh’s crust contingently, J・(m^{3}・K)^{−1};

ρ is the average density of the ores of the lower mantle, the upper mantle and the Earth’s crust, 4500 kg/m^{3};

c_{p} is the specific mass isobaric heat capacity, 1260 J・(kg・K)^{−1} [

T 1 is the temperature of the inner side (surface) when X = 0.54 and τ = 0 equals 283.2 K;

δ n = n π at n = 1 , 2 , ⋯ , ∞ is nth root of the characteristic equation sin ( δ n ) = 0 for the Dirichlet boundary conditions;

λ is the thermal conductivity coefficient, it is 2.5 W/(m∙K) for the lower mantle [

Substituting the above numbers into the Equation (22), here is the solution for the temperature, which is demonstrated in

n | τ | δ = nπ | r | r/R | Т(Х,Fo) = Т_{2} |
---|---|---|---|---|---|

1 | 0 | 0 | 3470 | 0.54 | 277.89 |

2 | 1 | 1 | 3570 | 0.56 | 282.236 |

3 | 2 | 2 | 3670 | 0.58 | 284.338 |

4 | 3 | 3 | 3770 | 0.59 | 284.164 |

5 | 4 | 4 | 3870 | 0.61 | 283.256 |

6 | 5 | 5 | 3970 | 0.62 | 282.691 |

7 | 6 | 6 | 4070 | 0.64 | 282.648 |

8 | 7 | 7 | 4170 | 0.65 | 282.876 |

9 | 8 | 8 | 4270 | 0.67 | 283.125 |

10 | 9 | 9 | 4370 | 0.69 | 283.285 |

11 | 10 | 10 | 4470 | 0.70 | 283.351 |

12 | 11 | 11 | 4570 | 0.72 | 283.357 |

13 | 12 | 12 | 4670 | 0.73 | 283.338 |

14 | 13 | 13 | 4770 | 0.75 | 283.312 |

15 | 14 | 14 | 4870 | 0.76 | 283.29 |

16 | 15 | 15 | 4970 | 0.78 | 283.272 |

17 | 16 | 16 | 5070 | 0.80 | 283.256 |

18 | 17 | 17 | 5170 | 0.81 | 283.238 |

19 | 18 | 18 | 5270 | 0.83 | 283.214 |

20 | 19 | 19 | 5370 | 0.84 | 283.186 |

21 | 20 | 20 | 5470 | 0.86 | 283.155 |

22 | 21 | 21 | 5570 | 0.87 | 283.132 |

23 | 22 | 22 | 5670 | 0.89 | 283.126 |

24 | 23 | 23 | 5770 | 0.91 | 283.14 |

25 | 24 | 24 | 5870 | 0.92 | 283.162 |

26 | 25 | 25 | 5970 | 0.94 | 283.175 |

27 | 26 | 26 | 6070 | 0.95 | 283.169 |

28 | 27 | 27 | 6170 | 0.97 | 283.157 |

29 | 28 | 28 | 6270 | 0.98 | 283.156 |

30 | 29 | 29 | 6370 | 1.00 | 283.159 |

the latter, the temperature graph goes asymptote at τ = 20 s and varies within (283.125 ¸ 283.175) K or (9.966 ¸ 10.015)˚C, that confirms the pervious calculation enough. Besides,

Note, that the performed calculations are simplified and preliminary for now, because the taken model does not take into consideration other values of the thermal conductivity coefficients of the transitive zone C shells, the lower mantle B and the Earth’s crust A. That is why accurate calculations for the spherically heterogeneous heat-exchange model of Earth can differ from the obtained results noticeably because the thermocurrens under different continents are heterogeneous.

The calculated magnitude of the magnetic induction В T T l o w can be real only if the used physical parameters and constants strictly meet the requirements of the physical law within which one or the other phenomenon can be correctly described, emergence and development of the Earth’s magnetic field in particular. The calculations analysis shows that the main element of their conformity is geothermoelectrical field Е_{Т} with its small intensity according to (3). At the same time, the known scientific conception of a planet’s metal core allowed to use the averaged temperature coefficient β, which is 0.0001 V/K for pure metals. The magnitude of the latter affects all the following parameters: Е_{Т}, j, I_{low}, which form the magnetic induction of the Earth’s field В T T l o w . That is why all the deliberate deviations from this value makes the В T T l o w magnitude get too low or extremely high. Hence, the taken magnitude β which is close to 0.0001 V/K indicates high probability of our planet’s core being metal.

Besides, the planet’s inner core electroconductivity σ affects the В T T l o w magnitude, but in a less degree. Thus, for instance, σ, which was taken by selecting, is equal to 5.0 × 10^{5} S/m and meets the calculated magnitude of the geomagnetic field on the planet’s equator, which is 3.64 × 10^{−5} T. But if one takes the electroconductivity of about 1.0 million cm/m, the magnetic field on the equator will be 6.98 × 10^{−5} T, which is much higher than the real magnitude of В_{0}. Therefore, the present range of the planet’s core electroconductivity 0.1 ÷ 1.0 million S/m can be constricted to some extent.

Besides, the considered model allows to explain the tilt of the magnet axis toward the Earth’s one by the Coriolis forces affecting the electron currents. The preliminary calculation shows that the Coriolis forces can displace the normal from the axis of rotation to the electron circular path plane by about 10^{0} - 11^{0} to the West, which corresponds the modern magnetic axis of Earth.

It is important to notice, that the suggested model allows to explain the causes of smallness or absence of magnetic fields of the other Solar System planets more correctly. In particular, any cooled planet with a cold metal core can have only a relict magnetic field.

The article shows that the Earth’s body has an advantageous combination of such physical elements as the electroconductivity of the metal core and the temperature difference between the planet center and the lower mantle, which is determined by the geotemperature gradient. It is known from the physics, that interaction of those factors inevitably leads to appearance of both thermo e.m.f. between the shell boundaries and radially directed thermoelectrical currents of high value (3.52 × 10^{9} А, see ^{19} kg. The latter’s moving cause appearance of the primary toroidal magnetic field, which is spherically asymmetric because of the thermo e.m.f. and the Earth’s inertial forces. The secondary poloidal field is self-generated through the central channel in the toroidal field and is dipole with two oppositely directed magnetic poles.

Thermoelectrical currents energy, as the calculations show, is enough not only for generating the Earth’s main dipole magnetic field on its early formation phase, but for maintaining it at the modern level of (3 - 5) × 10^{−5} T for a long time.

Thermoelectrical model of the Earth’s geomagnetic field is a brand new one and it is close enough to the real thermoelectrical processes of Earth. The latter are universal from the physical point of view and proceed inside our planet according to the known physical laws, which do not need any theoretical limitations or additions for the model to function. For the first time the considered EMF model in comparison with the magnetohydrodynamo model can give physically and logically reasonable answers to the questions related to the behavior of a geomagnetic field in space and time. In particular, this model lets us explain the cause of the magnetic fields inversion, forecasts the magnitude of the residual (mantle) magnetic field during the polarity reversal and cyclic change of warming and cooling periods, it also clarifies the magnitude of the Earth’s core electroconductivity and structure, allows to use a new and physically justified mechanism for calculating electrical and, indirectly, lithological characteristics of the Solar system planets. The latter, i.e. inversion problem solving, is likely if the magnetic fields of those planets are measures beforehand by spacecraft.

For the first time the temperature which the bottom surfaces of the continents and oceans bottom warm up to in case when the core’s thermocurrents move to the lower mantle was calculated using the thermoelectrical model of the Earth’s magnetic field.

Nevertheless, noe the considered thermoelectrical model of the Earth’s magnetic field is on its first stage, so this is a protomodel. It is based on the description of a homogeneous structure of a magnetic field, which should be the reason for developing a real heterogeneous model, using differential equations.

Thanks to Abramovich S.А. for checking mathematical calculations and Proskurnina T. V. for efforts to translate the manuscript to English.

Dmitriev, А.N. (2017) Thermoelectric Currents of Earth’s Core Generate the Earth’s Magnetic Field. International Journal of Geosciences, 8, 1048-1071. https://doi.org/10.4236/ijg.2017.88059

The manuscript “Thermoelectric currents of earth’s core generate the earth’s magnetic field” was not published in any magazine and it is not being edited in any editorial office.

An article close by meaning was published in 2016:

Dmitriev A. N. A New Look On the Nature of the Earth’s Magnetic Field//IOP Conf. Series: Earth and Environmental Science 44 (2016) 022001. DOI:10.1088/1755-1315/44/2/022001

I made the manuscript on my own in the Tyumen Industrial University, where I am working. Here is no competing finantial or any other interests of any organization as I did not get any subsidies, grants or ordinary shares. I, A.N. Dmitriev, am the only author of the manuscript and there is no legal claim to me from anyone. The manuscript author, A. N. Dmitriev.

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