Ocean geochemistry

An ocean parentage

It is known, that almost three quarters of a surface are coated by ocean waters. On the makeup sea-water is an aqueous solution of anorganic electrolytic conductor. The parentage of waters of world ocean and salts containing in them represents rather interesting question.

In determination of an elemental composition of water of ocean in the past paleontologic explorations can render major advantage. If to judge on data available now physical and chemical properties of ocean, apparently, during a geologic time essentially did not vary. This leading-out is substantiated by that biological aspects of the past more or are less similar to up-to-date aspects.

The geochemical solution of this problem consists in trying of confrontation of quantity of makeup of bald-headed igneous and sedimentary rocks with quantity and makeup of the salts dissolved at ocean. However there are difficulties in a contents explanation in sea-water and a sedimentary rock of enormous quantities of such anions, as carbonaceous, chloride and sulphate. Erosion of igneous rocks it is impossible to explain presence at up-to-date ocean of many of volatile, and the bulk of such devices as C, Cl, S, N, B, Br, F etc., containing at up-to-date ocean and bundled in a sedimentary rock, should enter from interiors of the Earth.

Probablly, chlorine, nitrogen, brimstone and fluorine entered in the form of HCl, NH₃, H₂S and HF; Carboneum in the form of CH₄, CO and CO₂, and a considerable proportion of oxygen in the form of H₂O, СО₂ and CO.

What mode this process proceeded? To answer this question, it is necessary to observe some requirements of formation of the Earth.

According to an early hypothesis the Earth initiatingly was in molten condition and consequently there could be a particulate volatile loss, but also their major part should be maintained in the Earth. This part of the volatile enters after refrigeration on a surface of the Earth in the form of a gradual continuous flow.

If the volatile have been lost on a formation initial stage pH fundamental ocean should be nearby 0,3 and so highly acid solute should dissolve significant amounts of igneous rocks easily. As soon as concentration Са²⁺, Mg²⁺, and СО^2-₃ in an aqueous solution has attained points of dissolution of a calcite and dolomite, carbonates have started to be precipitated sweepingly. Thereof from fundamental aerospheres and kickoff hydrospheres sweepingly to be taken carbonic acid, that finally has led to originating of requirements, applicable for existence of alive organisms.

It is necessary to observe the alternative assumption about gradual forming of ocean. We will guess, that the initial partial pressure of a carbon dioxide was more low 1 atm and that blanket atmospheric pressure approximately on 10 % more up-to-date. Then sedimentation of carbonates should begin by the erosion moment nearby 240 x 1020 g of igneous rocks and after achievement pH approximately 5,7. In this case the quantity redundant in a hydrosphere should not exceed volatile 1/10 from their up-to-date contents from interiors of the Earth. Collaterally oxygen entered and at the expense of habitability of alive organisms. Thus there was a gradual forming of an up-to-date hydrosphere.

Further we will consider the problem on a water entry at the expense of hot wells. It is considered, that aqueous pairs of hot wells of Jeloustonsky fleet contain 10-15 % of plutonic water, and hot wells of Idaho - 2,5 its %. But even if the contents of plutonic water in water of hot wells would be less than 1 % in flow of 4,5 billion years they could throw out enough of water for an explanation of existence of ocean. At least, existence of such plutonic water bolsters idea that water of up-to-date ocean has collected at the expense of gradual influx from interiors of the Earth.

There is one more point of view expressed Culp, that the hydrosphere could be generated gradually at the expense of a water entry from interiors of the Earth, after cooling of its surface to any certain temperature. Though the temperature of more penetrating regions of earth crust and a mantle precisely is not known, but, apparently, it not above 1000C°. At so heat Н₂О cannot enter into a crystal lattice of any minerals. Therefore, like gas, gaseous Н₂О, migrating through mucks, it was lost by earth crust. However unlike gas at water approach to a surface its part was bridged to material of a cortex and has formed hydrates: other part entered in a hydrosphere and an aerosphere.

Theological demonstrations of gradual forming of ocean

Like many, Revel [1955] considered, that ocean formation descended gradually. In its opinion, are available that demonstration, that the ocean considerable proportion has originated after serotinal Mesozoic. Presence of flat-topped marine mountains, coral atolls and guyots in vast terrains so-called «андезитного» Pacific ocean points belts descent of marine day concerning a sea level. To this descent is answered with accretion of total amount of sea-water approximately the quarter of up-to-date bulk of waters of ocean. Other demonstrations of possibility of descent of seabed in flow of last 100 million years have been gained at paleontologic explorations of a fossil fauna in a core of the holes driven in Pacific ocean. Besides, this statement is affirmed by flat-topped marine mountains between the Hawaiian Islands and the islands Vejk uplifted from depth of 5000-6000 metres below an up-to-date sea level.

Revel notes, that in view of sharp blossoming in serotinal Mesozoic pelagic a foraminifer substantial growth of influx of a carbon dioxide from interiors of the Earth, tracked by the conforming accretion of a water entry was possible.

Physical properties of sea-water

Density

For short the sea-water gravity р is expressed through, spotted as follows:

σ=(ρ-1)*1000

At normal atmospheric pressure the sea-water density depends on temperature T, saltiness S or chlorinity CV. Interrelations of density and a chlorinity, at normal temperature and pressure are expressed by the formula of Knudsen:

σ₀=-0,069+1,4708Cl-0,001570Cl²+0,0000398Cl³

Expansion ratio

In table 1 values of an expansion ratio of sea-water are produced at pressure, equal 1 atm.

Specific warmth

Dependence of specific warmth (С_р) sea-water at 0C° and pressure in 1 atm from saltiness can be expressed formula Kuwahara.

C_p=1,005-0,006136S+0,0001098S²-0,000001324S³

Where S - saltiness

Table 1. A sea-water Coefficient of thermal expansion at various temperature and saltiness.

Freezing point

Δt=-0,102710Cl,

Where Δt - value of a freezing point, Cl - magnitude of a chlorinity

Osmotic pressure:

р=(1,240+0,00454t)Cl

Elasticity of steams:

p=1000pR(273,1+t)Δp/M₀

Where p - osmotic pressure, р - density; R - gas characteristic; M₀ - a water molecular weight; p - elasticity of steams.

Conductivity

L (depending on a chlorinity of sea-water CL). (Table 2).

Table 2. A conductivity of sea-water (Lх10⁶).

Viscosity:

µ=µ₀/1+αt+βt²

Where µ₀ - coefficient of viscosity at 0 C°; t - sea-water temperature; α and β - the constants varying with alteration of saltiness.

Interfacial tension (dyn/sm²)

α=75,64-0,114t+0,0399Cl

Refractive index of light

In sea-water at 25 C° for a sodium D-line it is equal:

n25D=1,332497+0,000334Cl

Factor of an extinction of light α

In sea-water can be found by formula:

I_z=I₀*10^-az

Where I₀-intensity of monochromic light with wave length at a sea surface λ, I_z - light wave length on some depth z at an assumption, that dropping and driving rays of light are normal to the surface waters.

A sea-water elemental composition

Main and small chemical builders of sea-water. (Tab. 3 and 4).

Table 3. A sea-water Elemental composition.

Table 4. Small builders of sea-water.

Saltiness and the chlorine contents in sea-water.

To specify salt content in sea-water it is inconvenient, as at sea-water evaporation to dryness the acid carbonate part decomposes, and the chloride part is hydrolyzed, following definition concept of "saltiness" therefore has been made:

Saltiness is a blanket contents of a fixed residue in 1 kg of the sea-water, spotted after all carbonate is translated in monoxide, bromine and iodine and are substituted for by chlorine, and organic matter is completely oxidised.

Knudsen gives a following empirical-formula dependence between a chlorinity (Cl, %) and saltiness (S, %):

S=0,03+1,8050Cl,

Where Cl - «chlorine total in the grammes, containing in 1 kg of sea-water after the complete displacement of bromine and iodine of chloromas or the chlorinity is a magnitude in grammes on 1 kg of sample of sea-water, equal to numeral magnitude of mass in grammes of "combining weight silver", indispensable for sedimentation of halogens in sample of sea-water in weight in 0,3285233 kg.

Variations of saltiness and ocean temperature

Vertical frame of ocean. The ocean can be observed as bilayered system. The capping pass attaining power from ten metres to the first hundreds below aqueous level, tests agitation and in it both the temperature, and saltiness of water in a vertical direction manifest homogeneous allocation.

In the course had more low which one power from an interface region with a capping pass to the bottom attains several thousand metres, the temperature with depth diminishes. Vertical variations of saltiness in different places are various, nevertheless the density with depth always increases, owing to what water is distinctly delaminated as effect of vertical stability in a course.

According to it in low layer velocity of horizontal mixing is rather significant, and vertical agitation is committed sluggishly.

1. Lateral variations of saltiness at a surface
2. Saltiness alterations in ocean surface layer it is controlled by such requirements as saltiness alterations in surface layer
3. Letting-down of a salting liquid of sea-water afferent sea-water, deposits, waters of melting glaciers and icebergs, and on the other hand accretion of its concentration as a result of transpiration. And magnitude of transpiration directly proportional velocities of a wind and an odds between pressure of water vapours immediately at a surface fuming and their pressure in an aerosphere

As a whole, saltiness above in warm flows and more low in the cold.

Lateral variations of temperature in surfaces to region seas. Most heats of a surface of a sea are observed a little northward from equator, where also most air heat.

The gases dissolved in sea-water

Oxygen

The oxygen dissolved in sea-water is borrowed from an aerosphere on contact of water to air. It is formed also at a photosynthesis of marine plants. On the other hand, oxygen is consumed at breath of alive organisms and at oxidising of various materials of a sea, mainly an organic detritis.

The oxygen miscibility in sea-water depends on temperature and saltiness; this dependence can be expressed Yakobson's formula:

V(O₂)=10,062-0,2822-0,006144t²-0,000061t³-Cl(0,1073-0,003586t+0,000055t²),

Where V(O₂) - an oxygen miscibility in 1 sm³ on 1 l of sea-water at normal temperature and pressure in water and air equilibrium conditions at a normal pressure; Cl - a chlorinity; t - temperature of water, C°.

It is interesting, that at all oceans there is a course with the minimum contents of oxygen which one depth varies depending on geography.

However Richards [1955] point, that courses with the minimum contents of oxygen at ocean are most often dated for a surface of the same density - σ_t=27,2/27,3.

Sverdrup [1938] has observed the possible causes of equal balance between dynamic inflow and biochemical consumption to a course of the minimum contents of oxygen. Considered that, existence of a course with the minimum contents of oxygen is caused mainly by the biochemical charge of oxygen and character of allocation in a sea of organic matter and has made the inference, that the relevant cause of a minimum of the oxygen contents is existence at ocean of horizon of break.

Rackstraw [1947] spotted velocities of the charge of oxygen in the water samples seeded on a surface, in a course with the minimum contents of oxygen and in a deep-water course. Thus the reference temperature of samples was bolstered for a long time by a stationary value. He has fixed, that the oxygen charge for two years in water of a course with the minimum contents, no less than in water of a deep-water course, is rather inappreciable. On the other hand, day water after a small cure has got the same concentration of oxygen, as a water sample from a course with the minimum contents of oxygen. Rackstraw has come out with the guess, that organic matter in a vertical column of water, at least to a course with the minimum contents of oxygen, enters C its natural surface area and it the oxygen deficit speaks.

The Miyake and the Saruhashi [1956] having investigated the upright migration causes in a sea of dissolved oxygen, have come to leading-outs, that the oxygen deficit is intimately connected to contents accretion in sea-water of carbonic acid and C locally proceeding oxidative breaking-up of organic matter.

The first exploration of isotope makeup of the air oxygen dissolved in sea-water has been made Rackstraw and by the Dole.

Effects of mass spectrometric definitions have demonstrated, that between magnitude of attitude О¹⁸/О¹⁶ and quantity of the oxygen dissolved in sea-water on different depth, there is the significant apostatis of the below zero sign. Having used in the capacity of the standard attitude О¹⁸/О¹⁶ in air (0,2039 %), it was possible to fix, that the odds between percentage О¹⁸ and that of air with depth gradually increases, attaining a maximum in +0,006 % in a course with the minimum contents of the oxygen, laied out on depth about 700 m. After transit of a course with the minimum contents of oxygen d again relieves, dropping on depth of 2870 m approximately to +0,001 %. The Dole [1952] has fixed, that the oxygen freed at a photosynthesis, has lower magnitude of attitude О¹⁸/О¹⁶, than atmospheric oxygen; on its data, the fractionation factor is equal 0,983. It should result in to abatement of fraction О¹⁸ in the oxygen dissolved in sea-water as this oxygen is particulate effected by a phytoplankton.

On the other hand, oxygen in sea-water is immersed at breath of alive organisms, at bacterial processes, at oxidising of an organic detritis etc.; thus the oxygen light isotope is immersed selectively. Thereof it is necessary to expect, that the residual oxygen being in water in comparison with air should be rather dressed О¹⁸. According to definitions of the Dole [1954], the factor of a fractionation of isotopes of oxygen at processes of the deoxygenation dissolved in sea-water, is equal 0,991. It is necessary to note, that nitrogen in the gas dissolved in water of ocean as well as the atmospheric nitrogen, has normal isotope makeup.

Nitrogen and rare gases

The nitrogen miscibility in sea-water is presented Fox's by following formula:

V (N2) =18,639-0,4304t / 0,00745t2-0,0000549t3-Cl (0,2172-0,00718t+0,0000952t2).

Effects of definitions demonstrate, that the contents of dissolved nitrogen, and also an argon, a neon and helium, unlike oxygen changes with the depth a little and is always close to saturation.

In table 5 the instance of data about vertical variations of the contents of the neon dissolved in water and helium in Atlantic ocean is resulted.

Table 5. Contents variations in sea-water of the dissolved neon and helium

Atlantic ocean (35°55 ’ N and 67°39 ’ W), April

Electrochemical processes at ocean

As sea-water represents electrolytic conductor it is natural, that at ocean manifold electrochemical processes proceed.

Ocean water is an electricity conductor, therefore at its excursion through a magnetic field of the Earth according to the electroinduction law originates electromotive force

Dependence between an odds of potentials and a water flow velocity at ocean has a following appearance:

Where H-intensity of a magnetic field of the Earth; u a-flow velocity; φ - an odds of potentials.

Electric currents at the ocean, called by combined action of terrestrial magnetism and water excursion, can influence many underwater questions. For example, the subaqueous cable laid on a bottom of a narrow strait with the strong ebb-tide streams, will be corroded very sweepingly. Now acknowledging of the guess of the author that corrosion begins under the influence of an electric current, a changing as a function of tidal stream is gained; corrosion is sped up under the influence of the sec polarisation originating on a corroded surface of a cable.

Other electrochemical phenomenon of ocean consists in originating of concentration meshes. The potential difference is e spotted by formula:

E=(RT/nF)lC₁/C₂,

Where С1 and С2 - concentrations of known ions. At open ocean magnitude of attitude С1/С2 is close to 1 and consequently here it is difficult to expect originating of a major odds of potentials.

Moreover, in view of presence at water of the dissolved oxygen often possessing the significant concentration gradient, the significant redox potential is observed. If onboard the vessel to seat a calomel half-cell, and in water to dip a platinum welding rod it is possible to metre easily a potential difference between the welding rods, changing with the depth depending on the oxygen contents.

Nomura [1941] has fixed, that in shoal region seas between bottom and overhead the significant potential difference attaining sometimes 0,4v. in fresh and a brackish water when buffer reactions are feeble can originate sheets of water, a redox potential is close to hydrogen ionisation value pH.

Goldberg [1954] considers, that at the heart of formation of the manganous concretions met in deep-water region electrochemical process of accumulation of manganese and iron lays.

Last explorations of deep-water region have fixed, that sea-water tests disalignments even near the bottom. Thereof the ocean floor high side will serve as a welding rod. If underwater disalignments of water to bundle to the tidal excursions the bottom - a welding rod should get different polarity alternately. Freoxide salts in the sea-water, having a negative charge, will be precipitated owing to electrophoresis at positive charge of a welding rod, and iron will be precipitated at acquisition by a negative charge welding rod. If polarity of a welding rod variates through equally equal periods in concretions the equal quantity of iron and manganese will be store uped.

Exchange of a carbon dioxide between an aerosphere and ocean

Free air on the average contains 0,03 %₀ carbonic acid. The blanket contents of a carbon dioxide in an aerosphere is sized up in 0,0233 x 10²⁰ gramme. At ocean the carbon dioxide is present at aspect Н2СО3, НСО-3, СО2-3, organic matter; its blanket contents is sized up in 1,4 x 10²⁰ g, that approximately in 60 times surpasses its quantity in an aerosphere.

On design data the greatest quantity of carbonic acid is effected by alive organisms, that the quantity of carbonic acid outlayed at erosion and sedimentation, silicates tracked by transforming to carbonates at the same time is supposed, is low fidelity equal to its quantity entering at the expense of vulcanic activity, activity of fumaroles, hot wells, etc.

The quantity of Carboneum containing in organisms, being is expressed through СО2, compounds nearby 0,145 x 10²⁰ g, that in 6 or 7 times exceeds contents СО2 in an aerosphere.

Other important point consists that in ocean in a dissolved condition also there is an enormous quantity of carbonic acid. Medial blanket concentration СО2 in sea-water compounds 2,3 millimol/litre. At a sea surface where water is abutted with air, the trend to determination of equal partial pressure СО2 in an aerosphere and in sea-water is observed. Thus, by ocean contents СО2 in an aerosphere can be controlled.

As it will be told more low, the data rate carbonic acid moleculas between sea-water and an aerosphere can be easily fixed ground available definitions of radiocarbon age of marine deposits and organisms.

Magnitude of attitude С13/С12 in marine carbonates approximately on 2,5 % above this magnitude at land flora. Accordingly the factor of upgrading С14 in them two times more than the factor of upgrading С13. Taking into account agency of effect of an isotope fractionation concentration С14 in the marine stuffs, depressed concerning its concentration in standards, should be referred to bodily at the expense of radioactive disintegration on which one the absolute age of material can be spotted.

Kreg [1954] has fixed, that though expected magnitude of upgrading of up-to-date marine pockholes С14 is equal 5 %; that matches to 400 years of absolute age of Carboneum in ocean day waters. Kreg has come out with the guess, that it, was possiblly, effect of a slow exchange of a carbon dioxide, between ocean and an aerosphere.

According to Suess [1954, 1955], the medial radiocarbon age of marine organisms (on samples from Atlantic ocean) compounds 430 years.

Carbon dioxide allocation at ocean

In fresh water carbonic acid dissociates as follows:

[H⁺][HCO₃^-]/[H₂CO₃]=K₁

[H⁺][CO₃^-]/[HCO₃]=K₂

Where К1 and К2 - accordingly the first and second dissociation constants, which one magnitude changes as a function of temperatures, saltiness and a water chlorinity. At 20 C° К1=4,15 x 10^-7, рК1=6,38 and К2 = 4,20 x 10^-11, рК2=10,38.

Carbon dioxide data rate between an aerosphere and ocean

In connection with possible accumulation of a carbon dioxide as a result of burning of considerable quantities of fossil fuel the significant attention is given to questions on carbonic acid allocation on the Earth as a whole and about a data rate by a carbon dioxide between air and sea-water. If the quantity of an atmospheric carbon dioxide is really incremented, should descend and the increase of temperature of air caused by occlusion of caloric radiation that should cause essential alterations in a climate of the Earth. Such possibility will depend largely from a data rate carbonic acid between an aerosphere and a hydrosphere.

Proceeding from overseeing by behaviour С14 in an aerosphere and ocean Revel and Suess [1957] size up a carbonic acid residence time in an aerosphere of 14-30 years.

Parcional pressures of carbonic acid in air and in day waters of Atlantic ocean Takahashi [1959] have fixed definition, that concentration of a carbon dioxide in air immediately over a surface fuming is constant enough, on the average nearby 317,4 ррm, and that the ocean occludes carbonic acid all square of the surface. According to Takahashi, medial concentration of carbonic acid in free air 320,8 ррm.

Definition paleotemperatures ancient seas

Scale paleotemperatures on a relationship of isotopes of oxygen in an organic calcite.

Juri and its employees [1951] have tendered an interesting method of definition of temperatures of the ancient seas, grounded on dependence of isotope makeup of oxygen of water and carbonaceous ions on temperature. In explorations made by them percentage of heavy isotope О18 in a stuff of carbonaceous fossil remnants of ancient seas which one were formed at the expense of dying off of alive organisms dwelling in them was spotted.

According to Seaborg and Perlman [1948] isotopes of oxygen have a following relative abundance: О16 - 99,757, О17 - 0,039, О18 - 0,204. These magnitudes can fluctuate, being rejected by a maximum on 4 %.

α((3(CO¹⁸O^2-₃)=2(C¹⁶O¹⁸O^2-₂)+(C¹⁶O¹⁸₂O^2-))/(3(C¹⁶O^2-₃)=2(C¹⁶O¹⁸₂O^2-)+(C¹⁶O¹⁸O^2-₂)))/((H¹⁸₂O)/(H¹⁶₂O))

The dodge of an isotope fractionation at an equilibrium exchange has been investigated Juri and the Feel [1935], Juri [1947] and other explorers. The significant amount of data is gained concerning a deuterium and protium exchange.

For exchange reaction of isotopes of oxygen between carbonaceous ions (СО2-3) and water moleculas (Н2О) the fractionation factor can be spotted on the equation:

Where magnitude a is low fidelity equal to equilibrium constant To following exchange reaction:

H¹⁸₂O+¹/₃C¹⁶O^2-₃=H¹⁶₂O+¹/₃C¹⁸O^2-₃

Thus, having counted To for reaction 1,17 it is possible to gain the fractionation factor a and its variations depending on temperature.

By calculations it is fixed, that a fractionation proceeds more effectively at low temperatures and magnitude of the factor of a fractionation from 0 to 25 C° variates on 0,44 %, i.e. 0,176 % on 1C°. Therefore spotting concentration О18, it is possible to learn water temperature.

By definition of contents О18 in pockholes of the marine animals living at known temperature, Epstein, Buhsbaum and Juri [1953] have fixed the following dependence between temperature and deviations of contents О18.

t=16,5-4,3d + 0,14d²,

d - is spotted by formula:

d=(Rprobe/Rstand-1)*1000

Where R - the attitude of number of moleculas С16О18О to number of moleculas С16О2 in sample and the standard. In the capacity of the carbonate standard the belemnite from formation Pidi was used.

Abundance in sea-water О18. For exact definition of temperature on an oxygen scale it is necessary to know saltiness of water as abundance О18 in sea-water strongly varies depending on its saltiness. As pressure of the water vapours consisting from Н2О16 on 0,8 and 1,1 %, above that Н2О18 at 25 and 0C° accordingly contents О18 in water of oceans should depend on transpiration and condensation processes essentially.

Epstein and Mayeda [1953] spotted contents О18 on 93 samples of sea-water and 7 samples of soft water. At day waters of ocean deviation of contents О18 varies approximately from-3,3 to 3,5%о. The Average value d for sea-water from depth from 500 to 2000 m with medial saltiness 34,7%о has appeared (-0,04) - (+0,1) %о. The under magnitude of attitude О18/О16 is observed in superficial sea-water for which one the contamination of thawed snow of ices is possible. On the other hand, in sea-water, thin water of diverse parentage, than the water originating at thawing of ice and snow, deficit О18 is less, as the soft water originating at thawing of snow, has essentially under contents О18. Therefore sea-water approximately equal saltiness can manifest various abundance О18. It is interesting, that sea-water from depths more than 1000 m at the same saltiness contains smaller quantity О18.

In table 6 data Emiliani [1965] about medial isotope makeup of oxygen of a hydrosphere are cited.

Table 6. Isotope makeup of oxygen of a hydrosphere d, %о.

Paleotemperatureses of seas

Method Juri presented above and its employees [1951], using in the capacity of samples belemnites, have tried to spot paleotemperatureses of sea-water of the Upper Cretaceous season.

Radioelements in a seawater and deep-water deposits

Appreciable concentration of radium in deep-water deposits has been fixed for the first time Jolie [1908], made definitions of the contents of radium in the sediment core samples collected by expedition of Challenger. Since then the significant amount of data about concentration of radium in deep-water deposits is already accumulated. Has gained acknowledging the fact, that marine dottom sediments from depths more 2000m routinely contain radium more than granitoid mucks of a land. The enhanced concentration of radium specially is appreciable in red clay. (Tab. 7).

Table 7. The radium contents in continental mucks and marine dottom sediments, 10-12 g of Ra/l

Apparently from table 7 data the greatest contents of radium among continental mucks is observed in granite; however deep-water deposits contain radium much more. As to the dodge of concentration of radium in deep-water deposits, that, according to an available explanation, the ionium which is an isotope of thorium and the parent of radium, is precipitated in them together with ferrous hydroxide. Particulate concentration of radium can be bundled to accumulation in settlements of the radium; at the same time it is considered, that sedimentation of uranium from a seawater is much less.

There is a number of analytical data about the radium contents in a seawater. Evans and others [1938] have made definition of the medial contents of radium in the difficult sample of a seawater and have fixed, that it is equal 0,08 x 10^-12 gm/l, and the medial contents of uranium in a seawater compounds 1,5 x 10^-6 gm/l.

Pertaining to radium accumulations in deep-water deposits Hamagushi [1939] has come out with the guess, that radium is precipitated together with the colloidal corpuscles of hydrated oxide and iron oxide and manganese. Its guess is affirmed by concentration of manganese and iron in deep-water deposits.

Duration of the season from a time of a kickoff of generation by ionium of radium till formation of a maximum quantity of radium by calculations compounds about 10 000 years.

On Krehl, on radium allocation in deposits in the core oscillations in a settling rate of ionium, a variation of blanket velocity of sedimentation, and also diffusion and adsorption in radium and ionium settlements influence. Krehl has gained an approximate rate of speed of sedimentation of ionium about 1-20 mm/1000 of years, and the ionium contents at ocean compounds (3,1/1) x 1010^-15/ml

Holland and Culp [1956] investigated a radium and ionium cation exchange on a surface of pelagic deposits, using for ionium (Th230) and radium (Ra236) in the capacity of flares radio thorium (Th238) and thorium (Ra224). The gained effects have demonstrated, that quantities of the ionium occluded by deposits and radium comparably with observed in up-to-date deep-water deposits. This fact testifies that one of dodges of extraction of ionium and radium of ocean water are adsorption and a basic exchange.

The Arrhenius, Bramle and Piciotto [1957] have learnt allocation α-activity in deep-water settlements of the north of an equatorial part of Pacific ocean. The effects gained by them testify that about half α-activity is bundled to pieces and fragments of skeletal bones of fishes, excrement of animals of region of benthos and small (1 mk) highly refractiving crystals (it is probable, baryta); other half, in pores of deposits. Maculae with high α-activity, observed at fragments of bones of fishes, routinely contact isotopes of thorium and their derivatives.

Piciotto and Vilgeym [1954] have tendered the new chronological method grounded on the attitude of ionium and thorium (Th230/Th232). As ionium or Th230, has a half-life much more (1,4 x 10¹⁰years) it is possible to spot absolute age if in sample of a deep-water deposit the detrital stuff does not contain. On their data the ionium contents in a seawater less than 2 x 10^-13 g of Io/l.