Corundum-bearing metasomatic rocks of North Karelia occur in some localities within the Belomorian mobile belt (BMB). These rocks are connected with the aluminous gneisses of the Chupa complex and the shear zones, which in all cases are close to gabbro intrusions, partially amphibolized at the contact with metasomatites. These metasomatic rocks are characterized by unique oxygen isotope composition: δ¹⁸О down to −27‰ (Vienna standard mean ocean water, or VSMOW) [1]-[3], and are anomalous in comparison with all known silicate Earth’s rocks which have positive δ¹⁸О values [4].

A lot of models, which have been proposed for the genesis of these rocks, are based on the idea that glacial meltwaters contributed into the fluid that was responsible for the formation of these rocks, because only the subpolar glaciers are characterized by extremely light oxygen (−30‰ - −40‰). These models may be divided into three groups:

Ÿ Infiltration of glacial meltwaters from the surface to the depth about 20 km towards the endogenous zone of mineral formation [2] [5] [6].

Ÿ Volcanism beneath the glacier, prior to the formation of metasomatic rocks [3] [7] [8].

Ÿ Formation of ultralight protolith due to the interaction between glacial meltwaters and mafic intrusions before the metamorphism [1] [9].

The foregoing models have a lot of contradictions with the existing geologic, petrologic and geochronologic data.

Particularly evident is the assumption of glacial meltwaters infiltration to the depth about 20 km without interaction with the host rocks. Also the participation of glacial melt waters in the formation of metasomatic fluid assumes that the area of BMB in the Paleoproterozoic was in the high-latitude zone which contradicts the paleomagnetic data [10]. Furthermore, Paleoproterozoic volcanic rocks are not known within the Belomorian mobile belt [11].

The role of endogenous and surface waters connected with an atmospheric reservoir can be estimated by investigation of noble gas isotopic geochemistry, in particular, argon and helium isotopic geochemistry. Difference in isotopic ratios of these elements in surface waters and deep-seated fluids is at least one order of magnitude [12] [13].

Samples of Khitoostrov corundum-bearing rocks with anomalous oxygen isotopic composition and samples of host rock with anomalous and normal δ¹⁸О values were investigated to identify the presence of surface component in the fluid.

Analysis of argon and helium isotope composition in gas-liquid inclusions contained in minerals were carried out at the Centre of Isotopic Research of the A. P. Karpinsky Russian Geological Research Institute by the method [14] of vacuum crushing to extract trapped gas from fluid inclusions and isotopic measurements on the isotopic static gas mass-spectrometer Micromass NG-5400. The results are presented in Table 1. Oxygen isotopic composition of the samples were obtained previously and described in [1].

Probable contribution of cosmogenic component was evaluated because some samples were collected from the surface, except metasomatic rocks. In situ production of nucleogenic helium was possible by reaction ⁶Li(n, α)³H à ³He. Estimated input of cosmogenic and nucleogenic helium could affect the ³He/⁴He ratio less than to 10%.

Solubility data for noble gas in water [12] is used to estimate the noble gas concentration in the surface water produced by melting of high latitude glaciers. Estimations for argon and helium in the endogenous fluid were evaluated by the data for the noble gas isotopic and elemental ratios in endogenous continental rocks: ³He/³⁶Ar = 0.001 - 0.1; СО₂/³⁶Ar = 10⁹ - 10¹⁰; CO₂/H₂O = 0.05 - 0.15 [15], so the calculated ³⁶Ar concentration in the fluid

is from 2.5 * 10⁻⁷ to 2.5 * 10⁻⁶ cm³/mol Н₂О, and ³He-from 2.5 * 10⁻⁹ to 2.5 * 10⁻⁷ cm³/mol Н₂О. The mixing lines were calculated to specify a possible model of the surface melted water and the endogenous fluid mixing (Figure 1).

Calculated mixing lines for the metamorphic fluid and surface water do not fit the experimental points. This means, that participation of any surface water, including glacial meltwater, in formation of fluid with the anomalously light oxygen is impossible. That also relates to hypothetic pre-metamorphic alteration zones in mafic intrusions. Isotopic data point to the participation of endogenous fluid in corundum-bearing rock formation, so rock forming fluid in the shear zone was depleted in heavy oxygen isotopes for some reason.

Isotopic data for helium combined with elemental ⁴He/⁴⁰Ar ratio (Figure 2) demonstrate: 1) preferential loss of helium took place in the shear zone, which confirms the existence of thermal gradient between the central hotter

part of the shear zone and the colder outer host rocks for the gneisses, and just opposite scenario was for the amphibolized gabbro as compared to unalterated gabbro; 2) essential increase of ³He/⁴He isotopic ratio (up to 1000‰) in the metasomatic rocks in the central part of the shear zone in comparison with the host gneisses and the opposite effect is observed in the altered and primary gabbros; 3) correlation between the first two effects.

Helium and oxygen isotopic compositions correlate in the system. Light isotopes (³He and ¹⁶O) are concentrating in the central hot part and the heavy isotopes (⁴He and ¹⁸O) are concentrating in the outer cold part, especially in amphibolized gabbro. Isotopic effect for helium is much stronger, than for oxygen, so isotopic fractionation of oxygen is mass depended and has no connection with isotopic exchange effects between the fluid and the rock.

The results may suggest that isotope and element fractionation in the fluid system was realized by thermodiffusion mechanism (Soret effect). It leads to separation according the molecular or isotopic mass due to the temperature gradient in the system. Such conditions can be realized in the fluid permeable shear zones. The effect of isotope separation, or molecular combinations with various mass, by thermodiffusion is described in terms of the non-equilibrium thermodynamics [16] [17] and leads to concentration of the light species (and light isotopes) in the central hotter part of the system.

During metasomatism the fluid migrates from the hot center part of the permeable zone into the colder host rock by means of the external convection and according the foregoing mechanism the host rocks are enriching in heavier oxygen and helium isotopes. Gabbro amphibolization takes place under the influence of the fluid and the growing amphibole traps into its crystal cell a portion of the fluid as the (ОН)⁻ groups, which are enriched in the heavy isotopes, i.e. amphibole is a pump analogue. The factor of isotopes separation in the individual thermodiffusion cell is very small and close to unity, however the effect can be greatly increased by cascading of cells [18]. During this process each part of shear zone with better permeability is an individual vertical cell, where isotopes are undergoing separation. Therefore the foregoing mechanism is multiplied in the rocks and the cascading mechanism can be realized (Figure 3).

In nature, thermal diffusional mechanism of isotope separation with cascading of elementary separating cells requires the removal of fluid from the cold outer part of the shear zone, i.e. it demands a special “fluid pump”. Intrusive gabbroids amphibolized at the contacts with corundum-bearing plagioclasites in the fluid permeable shear zones (Figure 3) can play the role of such pumps. It is the difference between the studied corundum- bearing rocks and analogous metasomatic rocks in the other complexes where no anomalous isotopic composition of oxygen was found.

Initial water-rock ratio (W/R) is from 0.01 to 0.06 at the entrance of the separation column, i.e. from 1 to 6 weight percents of H₂O, as follows from estimations of ⁴⁰Ar concentration and ⁴⁰Ar/³⁶Ar ratio in metasomatic rocks (Table 1) and from estimation of СО₂/³⁶Ar = 10⁹ - 10¹⁰, CO₂/H₂O = 0.05 - 0.15 in the endogenous fluid and from estimation of the Rayleigh exhaustion factor f = 0.0007. From 0.5 to 2.5 volume fraction of the amphibolites developed over gabbro should account for a single elementary volume of the metasomatic rock, as follows from the estimation of volume fraction of water in amphibolites developed over gabbros, average 2.5 - 2.7 weight % Н₂О. This is consistent with the geological settings of locations according to the geological schemes and cross-sections [1] [2] [7].

The absence of isotopic equilibrium in coexisting minerals of corundum metasomatites [19] and marked out in [3] also indicates the thermal diffusion mechanism, under the influence of which the thermodynamic equilibrium is impossible. This can be applied to the local equilibrium as well.

The foregoing model is suitable for describing all localities of corundum-bearing rocks within the Belomorian mobile belt in a single process [20]. Localities with the weak effect of oxygen isotope separation are on the bottom of the separation column cascade and localities with the strong effect are on the top of the separation column.

Further isotopic research of these objects is necessary to clarify the present model. It is expected that classic metasomatic zoning in similar objects can be disturbed by thermodiffusion mechanism.

We thank Dr. P. Ya. Azimov (IPGG RAS, St. Petersburg) for the samples for this study and Prof. E. M. Pasolov (VSEGEI, St. Petersburg) for the help with analytical work.

This work was partly supported by Saint-Petersburg State University grant 3.37.86.2011.

E. Yu. Akimova,K. I. Lokhov, (2015) Ultralight Oxygen in Corundum-Bearing Rocks of North Karelia, Russia, as a Result of Isotope Separation by Thermal Diffusion (Soret Effect) in Endogenous Fluid Flow. Journal of Materials Science and Chemical Engineering,03,42-47. doi: 10.4236/msce.2015.312008