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Article

The Origin of Hydrocarbon Gases in the Lovozero Nepheline-Syenite Massif (Kola Peninsula, NW Russia), as Revealed from He and Ar Isotope Evidence

by
Valentin Nivin
Geological Institute, Kola Science Centre, Russian Academy of Sciences, 14 Fersman St., 184209 Apatity, Russia
Minerals 2020, 10(9), 830; https://doi.org/10.3390/min10090830
Submission received: 15 August 2020 / Revised: 16 September 2020 / Accepted: 16 September 2020 / Published: 21 September 2020
(This article belongs to the Section Mineral Deposits)
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Abstract

:
The occurrence of hydrocarbon gases (HCG) in unusually high concentrations for magmatic complexes, in the Lovozero and some other alkaline massifs, is of both geochemical and practical interest. The nature of these gases, despite the long history of research, remains the subject of debate. As an approach to solving this problem, we studied the coupled distribution of occluded HCG and the recognized tracers of various geological processes, such as helium and argon isotopes. The extraction of the gas components trapped in fluid micro-inclusions was carried out by the mechanical crushing of rock and mineral samples. A positive correlation was found between the 3He/4He and CH4/C2H6 ratios, whereas a negative correlation of the latter was found with the 36Ar concentration, which in turn was directly related, in varying degrees, to the content of HCG and most strongly with pentanes. Conjugacy of the processes of the heavier gaseous hydrocarbons, a loss of the deep component of the fluid phase and dilution of it with the atmogenic component was established. In the absence of a correlation between CH4 and 3He, the value of the CH4/3He ratio in the Lovozero gas substantially exceeded the estimates of it in gases of a mantle origin, and mainly corresponded to the crustal values. However, in some samples, a small fraction of mantle methane was allowed. The peculiarities of the relationships between hydrocarbon gases and the isotopes of noble gases indicate a sequential process of abiogenic generation and transformation of HCG at the magmatic and post-magmatic stages during the formation of the Lovozero massif. The obtained results confirm the usefulness of this approach in solving the origin of reduced gases in alkaline igneous systems.

1. Introduction

A notable feature of some nepheline syenite and foidolite massifs, primarily in the world’s largest Khibiny and Lovozero alkaline plutons and the related huge deposits of phosphorus and rare elements, as well as in Ilimaussaq in Greenland, is a concentration of reduced hydrogen-hydrocarbon that is unusually high for igneous rocks, with a predominance of methane gases [1,2,3,4,5,6]. Commonly, hydrocarbon gases (HCG) are found in vacuoles of micro-inclusions in minerals (occluded gases—OG). Still, the occurrence of other forms (morphological types) of such gases are also known in the Khibiny and Lovozero massifs. These freely released, or free gases (FG), are filling systems with varying degrees of interconnected fractures (mainly microfractures), as well as other cavities in the rocks, and diffusely dispersed gases (DDG) that are found in closed and half-open thin and sub-capillary cracks, retained, to a considerable extent, in the adsorbed state, and where diffusion transfer predominates when they are moving [1,4,6,7,8,9].
The presence and nature of HCG in the rocks of agpaitic complexes is of both geochemical and practical interest. In particular, the first matter is due to the importance of clarifying the role of reduced fluids as possible agents and indicators of the conditions and sequence of the rock and mineral formation, including various types of ore mineralization (e.g., References [5,10,11,12,13,14,15,16,17]). The applied value is due to the release of hazardous natural combustible and explosive gases into the atmosphere of the underground mines working on mineral deposits associated with nepheline-syenite massifs [1,4,6,9]. The solution to these and other problems is impossible without learning more about the origin of these gases.
However, despite more than half a century history of studies focused on HCG in the rocks of these massifs, the mechanisms and the relative time of their formation are still subject to discussion [6,7,11,12,13,14,15,17,18,19,20,21,22,23,24,25]. With a wide range of assumptions being made about the genesis of HCG (from biogenic to mantle origins), most researchers consider these gases to be abiogenic. To explain the pre-, early-, late-, or post-magmatic formation of these gases, various authors have considered all the processes and mechanisms of abiogenic methane formation, such as, in Etiope and Sherwood Lollar [26], Sephton and Hazen [27]. Different directions of the evolution of the hydrocarbons—from complex compounds to the simplest and vice versa—have also been assumed.
The various points of view on the nature of HCG (in most cases, OG are referred to) proposed by the authors, especially in recent publications, have been based on data concerning the features of their distribution in rocks and minerals, the isotopic composition of the carbon and hydrogen, thermodynamic calculations and the thermometry of individual fluid inclusions. Meanwhile, rare gas isotopes have long been used and are increasingly recognized as geochemical tracers for various processes in the fluid and fluid-containing systems of different geological environments [28,29,30,31,32,33,34,35,36,37,38,39,40,41,42,43,44,45,46,47,48,49,50]. In our case, we used an approach that was not previously employed to understand some aspects of the origin of the reduced fluid in nepheline-syenite magmatic complexes, as well as for studying the coupled distribution of occluded HCG and helium and argon isotopes in the rocks of the Lovozero massif. The results of these studies are presented in this article.

2. Geological and Gas Geochemical Settings

2.1. Lovozero Massif

The Lovozero massif of agpaitic feldspathoid (mainly nepheline) syenites and foidolites has been the subject of detailed and comprehensive studies. Research results on various aspects of its geology, petrology, mineralogy, geochemistry and metallogeny are revealed in hundreds of publications, including monographs (e.g., References [51,52,53,54]) and relatively recent articles [55,56,57,58,59,60,61,62,63]. The presence of such an extensive range of literature has allowed us to confine the scope of the current research to only the most general information on the geology of the massif, sufficient for understanding the subject of the article. For some rocks, the names that are not generally accepted, but are the most commonly used, have been preserved.
According to the totality of the available data, the laccolith-type Lovozero alkaline massif was emplaced 360–370 million years ago into Archean gneisses and gneiss-diorites covered by Devonian sedimentary-volcanogenic rocks, at the peak of the Palaeozoic tectono-magmatic activation of the eastern part of the Fennoscandian shield. The rocks of the differentiated complex (DC, also known as layered and loparite-bearing) and the eudialyte complex (EC), are predominant within the recent erosional truncation (Figure 1). The names of these complexes are somewhat arbitrary.
The DC, where the ore (loparite) bodies are mainly concentrated, is composed of numerous (up to 200) gently pitching, rhythmically alternating horizons (layers) of lujavrites (trachitoid nepheline syenites of the foyaite-malignite-shonkinite series), as well as massive foyaites and urtites forming two-member and three-member sequences. The thickness of the individual layers varies from several centimeters to dozens of meters. The DC is usually divided into series (I–V from top to bottom) consisting of several (up to 16) rhythms. For the marker foidolite horizons, including the ore-bearing ones, a nomenclature that involves a serial and order number of the horizon from the upper border of the series (for example, I-4, II-7, III-14, etc.) is acceptable. In addition to the above-mentioned rocks, the differentiated complex also includes alkaline rock varieties, such as ijolite and malignite. The main rock-forming minerals are nepheline, K-Na feldspar and aegirine. The ore mineral of loparite, or more exactly, loparite-(Ce) with the general formula (Na,Ce,Ca)2(Ti,Nb)2O6, occurs in sheet-like zones and ledges of dissemination related mostly to areas of contact between rocks of different petrographical compositions. Near the contact of the massif, the DC rocks are gradually being replaced by massive coarse-grained and pegmatoid nepheline syenites. The gneisses in the exocontact intrusion are fenitized to varying degrees. The fenites themselves form narrow zones, ranging from fractions of a meter to several meters.
The EC is generally made up of a slightly differentiated stratum of inequigranular eudialyte lujavrites (eudialyte malignites), locally changing into foyaites, and rarely into foidolites. The rocks are enriched with (mangano) eudialyte in amounts of 5 to 10 vol.%, while sometimes reaching 90 vol.%.
Both complexes contain numerous bodies of poikilitic and inequigranular nepheline, sodalite-nepheline and nosean-nepheline syenites, concordant lens-like or sheet-like xenoliths of olivine basalts, tuffs and tuffites of the Lovozero Suite, as well as alkaline pegmatites and hydrothermalites, in various sizes and shapes.

2.2. Occluded Hydrocarbon Gases

As in other morphological types of the gas phase in the Lovozero massif [6,8,9], methane is the main component of the gases occluded in vacuoles of fluid inclusions in the minerals [1,4,6,25,64,65]. Most often, these inclusions are gaseous and secondary in the relative formation time. When a gas extraction is carried out by mechanical grinding of the samples, the CH4 concentration in OG according to a chromatographic analysis is mainly 70–90 vol.%. In varying subordinate and trace amounts, hydrogen, ethane, other methane homologues (up to pentanes inclusive), unsaturated HCG (alkenes), nitrogen and helium are always present. Dioxide, and especially carbon monoxide, are occasionally detected and, as a rule, exist only in low concentrations. The specific content of CH4 in the rocks and minerals on average (median) values of 6–8 cm3/kg can reach 100 cm3/kg. With a decrease in this characteristic, the relative concentration of non-hydrocarbon components in the exhaust gas increases.
The most important gas concentrating minerals are nepheline and K-Na feldspar [14,66]. Of the three main types of rocks, lujavrites are generally less gas-saturated than foyaites and urtites. However, the HCG content level is more dependent on the position of the sample in a vertical section of the massif, not on the petrographic type of the rock. So, in the differentiated complex, the same rocks gas saturation is significantly higher in the III–V series compared to the I and II series [4,15,22]. The content of HCG in EC rocks is comparable with that of the upper part of the DC. A positive correlation has been found between the gas saturation of the Lovozero rocks and the content of late- and post-magmatic sodalite, analcime, albite and villiaumite in these rocks, as well as a negative correlation between the contents of the gases and low-temperature zeolites of the natrolite group [4,15]. An important indicator role was also established for the CH4/C2H6 ratio (RME), where a decrease in this ratio, as well as an increase in the slope of the HCG molecular weight distribution corresponding to the classic Anderson–Schulz–Flory distribution, reflects a decrease in the temperature range of the post-magmatic processes, gas generation and the capture of fluid inclusions [14,15,22,23,66].
As was already noted, the mechanisms, conditions and relative time for the formation of HCG in the rocks of the Khibiny, Lovozero and Ilimaussaq nepheline-syenite massifs have been the subject of discussion for an extended period of time. Reviews of the hypotheses concerning their origin (from biogenic to mantle origins) contain varying degrees of detail; for example, in References [4,6,15,22,67]. Nonetheless, the vast majority of modern researchers, with rare exceptions (e.g., Reference [24]), consider these gases to be predominantly abiogenic, and one way or another related to the formation of the massifs.

2.3. He and Ar Isotope Compositions

The data on the isotopic composition of helium and argon in the rocks and minerals of the Lovozero massif was partially published earlier [68,69], and is systematized and generalized in Reference [70]. Compared with the other Palaeozoic complexes of the Kola alkaline province, especially alkaline ultrabasic with carbonatites in the mantle fluid of which the contribution of a 3He-rich plume component was established [71,72], the rocks of the Lovozero massif that are undoubtedly the mantle source of parental melts [73,74,75] have retained the primary mantle gases to the least extent, and on the contrary, are more susceptible to the influence of surface meteoric waters containing dissolved atmospheric air. They differ in terms of the lowest 3He/4He and 40Ar/ 36Ar ratios in the gases occluded in fluid inclusions. Thus, the estimated initial 3He/4He ratio in the trapped fluid here was 1.2 × 10−6 [70], while in the Seblyavr and Kovdor alkaline-ultrabasic massifs with carbonatites, this ratio was ~3.3 × 10−4 [72]. The Lovozero rocks and minerals are characterized by wide variations in the concentrations of helium isotopes ((0.45–960) × 10−6 and (0.37–600) × 10−13 cm3/g respectively, 4He and 3He), as well as argon ((7.6–2200) × 10−8 and (2.2–210) × 10−10 cm3/g respectively, 40Ar and 36Ar) and the indicator isotopic ratios 3He/4He and 40Ar/36Ar ((0.5–110) × 10−8 and 311–5450, respectively) in the occluded gases [70]. It has been established that the 3He in OG is mainly mantle, while the 36Ar is predominantly atmogenic. The decrease in the 3He/4He and 40Ar/36Ar ratios generally reflects an increase in the degree of degassing in the primary fluid and/or adding to it the core, in particular, the atmogenic component. The variations in these indicators, as in the case of HCG, are caused to a great extent by the positions of the samples in the vertical section of the massif, and not by the petrographic type of rock.
In general, the features of the distribution of the isotopes of noble gases in the rocks and minerals of the Lovozero massif confirm: (a) the general direction of the evolution of the melt and the complementary fluid phase in the magma chamber as a whole, in the three-membered (urtite-foyaite-lujavrite) units and in each individual layer. (b) The relative closeness of the fluid-rock-melt system during the magmatic crystallization and in the early stages of the epimagmatic transformations, with a predominantly auto-metasomatic character. (c) A shorter time interval and a temperature gradient between the formation of a crystalline matrix and fluid inclusions in the ore rocks relative to the barren rocks. (d) The possibility of transforming the ore horizons at a relatively late post-magmatic stage and (e) the important role of paleometeor waters in the low-temperature mineralogenesis [70].

3. Samples and Analytical Methods

The distribution of He and Ar isotopes and the content of HCG were studied in the same rock samples. To a lesser extent, the minerals of the massif itself, as well as the zone of its contact with the gneisses, were included in the study (Table 1).
The extraction of the gas components contained in the fluid inclusions was carried out by the mechanical grinding of rock and mineral samples. Two modifications of this method were used for the extraction of HCG from large (200–350 g) and small (0.5–1 g) weights [4]. Crushing of the large samples was carried out for 20 min on a vibration eraser in special, sealed stainless-steel cups with grinding balls, which were previously vacuumized up to 1.3 Pa. When the fraction −10 + 1 mm was loaded into the beaker, about 60–70% of the sample was crushed to 0.05 mm particles. After grinding the sample, the evolved gas was pumped out via a mercury unit and was then introduced into the chromatograph PE F-30 (PerkinElmer Inc., UpplandsVäsby, Sweden) and TSVET-102 (LLC “Tsvet”, Dzerzhinsk, Russia), using a syringe. In the second case, a small (about 2.5 cm3) volume vibrochamber built into the gas system of the TSVET-102 chromatograph was used, into which the sample fraction of −0.63 + 0.25 mm was loaded together with the grinding balls and purged with helium. The grinding was carried out for 20 min in a helium atmosphere at room temperature and pressure. After switching the metering valve, the evolved gases were washed out by the carrier gas into the chromatographic column. The minimum detectable concentrations of the individual gases varied somewhat, depending on the type of chromatograph and the sorbent that was used. They averaged (as a percentage by volume) 0.0005, 0.00005 and 0.00001 for methane, ethane and the heavier HCG, respectively. The root-mean-square error of the analysis of individual components was 0.4–0.8, while the coefficient of variation ranged from 2.7% to 4.6%.
The methodology used to study the isotopic composition of helium and argon has been repeatedly published in earlier research, for example in References [70,71,72] (and references therein). The extraction of the occluded noble gases was carried out by a mechanical grinding of the samples. A 0.25–0.6 mm fraction of a sample weighing 1.5–2 g was placed in a glass ampoule together with the grinding steel rollers and/or balls and was then evacuated and soldered. The grinding was carried out on a vibration unit. Titanium-zirconium getters absorbed the chemically active components of the released gases. Separation of the light and heavy noble gases was carried out using coal traps cooled by liquid nitrogen. The contents and isotopic composition of helium and argon were measured on a MI-1201 static mass spectrometer. The sensitivity for helium and argon is 5 × 10−5 and 3 × 10−4 A/torr, respectively. The error in determining the concentrations (determined using the peak height method) was 5% (±1 σ). The 3He/4He ratios at values of 10−6 and 10−8 were measured with errors of ±2% and ±20%, respectively. The measurement error of the 40Ar/36Ar ratio of 3000 was 0.3%, while for a value of 50,000, the error was 25%. The volume of the gas was reduced to normal conditions. The measurements were performed by I. L. Kamensky and under his methodical guidance by the author.

4. Results and Discussion

When the distribution of the isotopes of noble gases was separately studied in earlier research, as well as methane and its homologues in Lovozero rocks, attention was drawn to the similar peculiar properties of the variations in the vertical section of the massif in the average 3He/4He and CH4/C2H6 ratios [22,23,70]. As was noted above (Section 2.2 and Section 2.3), a decrease in the first of these indicator ratios indicates a loss in the fluids of the primary mantle component [70,72]. In contrast, the second ratio reflects a decrease in the temperature range of the HCG generation, post-magmatic changes in the minerals and the formation of fluid inclusions [14,23,66,70]. In each of the three main types of Lovozero rocks (lujavrite, foyaite and urtite), from the top to the bottom of the section, both of these indicators slightly increased from the eudialyte complex to the first series of DC, followed by a significant decrease in the lower zone of the first and upper parts of the second series, reaching its minimum in the ore (loparite) ledges, then gradually and significantly increased with a greater depth. In the same direction (from top to bottom), the 40Ar/36Ar ratio increased and the 36Ar concentration decreased more smoothly. The most likely and main source of the latter phenomenon was paleometeor water with air dissolved [70]. The peculiarity of the change in RME is consistent with the molecular mass distribution of heavier gaseous alkanes in both rocks and minerals [14,23].
Additional studies and a direct comparison of the gas-geochemical characteristics of the same samples confirmed these presumed relationships. Table 2 presents the results of measurements in the rocks and minerals of the concentrations, with the ratios of the isotopes of noble gases and the content of hydrocarbon gases. The concentrations of 4He, CH4, C2H6 and the ratio 3He/4He were determined in almost all the samples, while the isotopic composition of argon and the content of pentanes were determined in less than half of them. Variations in most of these parameters, with the exception of 40Ar and 40Ar/36Ar, reached three orders of magnitude.
Between the ratios of CH4/C2H6 and 3He/4He, a generally positive correlation was found (Figure 2). A negative, weaker, but still significant, correlation between RME and the light argon isotope concentration was also revealed (Figure 3). As it turned out, the latter was related in varying degrees with the concentration of hydrocarbon gases, with an increase in the molecular weight intensifying this bond. Thus, the calculated pairs of correlation coefficients of 36Ar with pentanes (Figure 4), ethane and methane were 0.96, 0.59 and 0.45, respectively.
Figure 2, Figure 3 and Figure 4 show that the processes causing the fraction of its deep constituent in the fluid phase to decrease and the concentration of heavier hydrocarbons and the proportion of the atmogenic component to increase, largely coincided in both time and space. These observations are consistent with the previously established parallel increase in the proportion of a high molecular weight HCG and a decrease in the 3He/4He ratio among the main Khibiny and Lovozero rock-forming minerals (aegirine–K-Na feldspar–nepheline) [76]. In the same sequence, the total average gas content of the minerals and the intensity of their post-magmatic transformations increased. Furthermore, a previous calculation [70] of the balance of helium and argon isotopes in the minerals of the Lovozero zeolitized juvite-urtite (feldspar urtite) from Series II of DC showed that zeolites, which make up about 20% of the sample volume, accounted for only 4% of the helium contained in the rock with a low 3He/4He ratio, and 96% of the total 36Ar with a near atmospheric value of 40Ar/36Ar. Therefore, in comparison with the associated nepheline, sodalite, feldspar and aegirine, the zeolites differed with the lowest CH4/C2H6.
No relationship was found between the concentrations of CH4 and 3He (Figure 5), whereas in the case of methane from a predominantly mantle source, a positive correlation between these components could be expected. The same figure showed that the value of the CH4/3He ratio in the Lovozero rocks significantly exceeded the estimates of those in mantle gases (1 × 105−1 × 107) and mainly corresponded to the crustal values estimated at 1 × 1010–1 × 1013 [31,33,37,77].
More than 30 years ago, Marty and Jambon [29] showed the possibility that combining carbon-helium and isotope-helium systems could be the most important characteristic of deep fluids in mantle and subduction zones. Thus, a double diagram of the 3He/4He (R/Ra, 4He/3He)–CH4/3He type, in one form or another, is often used to determine the methane sources in the gases of different geological environments [30,33,35,38,39,41,45,46,47].
The figurative points of the Lovozero gas samples in such a diagram form a vast field that partially overlaps the region of the crustal values of the considered parameters and the adjacent part of the hypothetical mixture of the mantle and crust sources (Figure 6). The latter usually refers to gases of a thermogenic origin. However, the high (from 1 × 1011 to 1 × 1014) CH4/3He ratios in the Sea of Japan’s oil and gas fields are considered to be the result of abiogenic methane formation by a CO2 reduction [28]. In the present case, about a quarter of the Lovozero samples (mainly the upper part of the DC, including the rocks of the endocontact massif) are characterized by “crustal” values. Of the remaining ones, more than half of the points are located below these areas. In general, the field of Lovozero gases is located at a considerable distance from gases with methane of a distinct or predominantly mantle origin, which include the gases of geothermal fluids from the East Pacific Rise 13° N and 21° N and the Mid-Atlantic Ridge [43], as well as micro-inclusion gases in the olivinites and pyroxenites of the Kovdor and Seblyavr massifs of the Kola alkaline province (data on the 3He/4He ratios have been borrowed from Reference [72]).
The intermediate position between the mantle region and the field of Lovozero samples is occupied by magmatic gases of the Zambales Ophiolite in the Philippines [78] and carbonatites from the Sallanlatwa and Sokli complexes of the Kola alkaline province (previously unpublished data collected by the author), abiogenic methane from the hot springs in China [37], as well as magmatic gases that partially enter the Lovozero field from the Xujiaweizi area of the Songliao Basin (China) [38] and abiogenic methane from the geothermal field of the Vicano–Cimino Volcanic District (Italy), which is formed due to the reduction of CO2 [44]. In the latter cases, even if the samples included in the diagram fell into the mixing zone of the crust and mantle end members or, for example, in the Xujiaweizi area of the Songliao Basin, China, a strong correlation between CH4/3He and 3He/4He was found [38], in the aggregate of the different criteria the methane was not a mixture of thermogenic (or bacterial) and mantle. It can be assumed that only the latter’s presence in one proportion or another, or the possibility of a mantle source of carbon, was involved in the formation of methane.
The presence of, albeit a weak, negative correlation among the CH4/3He and 3He/4He ratios in the entire set of Lovozero samples, and the location of some of them in the diagram, also allows for the presence of a very insignificant fraction of mantle methane in the rocks of the lower DC series, and especially in the exocontact of the massif. It is this source, at least primarily magmatic, that can be determined for CH4 in the agpaitic and miaskitic rocks of the Ilimaussaq and Khibiny massifs, based on an analysis of the mineral equilibria [11,12,13] and the isotopic compositions of carbon and hydrogen of the HCG [25,67]. The authors believe that methane could be the predominant carbon component of the fluid during the magmatic crystallization of such rocks. However, the observed ratios of methane and helium isotopes in the Lovozero rocks can only be due to mantle-derived carbon, which later becomes part of the CH4. Estimates of the crystallization process’ redox and temperature conditions showed that the carbon was in the form of CO2 in equilibrium with the melt fluid [80]. According to the thermodynamic calculations of Ryabchikov and Kogarko [19,20], under the redox conditions characteristic of the Khibiny massif, at high temperatures, carbon should also be in the form of CO2 in the fluid and carbonate anions during the melt. According to these calculations, the presence of CH4 in the fluid phase can be allowed only in small quantities.
However, the previously established [70] increasing concentrations of CH4 and 3He, and the ratios of 3He/4He and CH4/C2H6 in the fenites and fenitized gneisses of the exocontact of the Lovozero massif, as compared with the rocks of the endocontact (Figure 7), may indicate the appearance of a significant amount of methane in the fluid even during the magmatic stage in the formation of the massif. The rocks of the endocontact are represented by uneven coarse-grained and pegmatoid massive nepheline syenites (up to microclinites), which are typical for this situation. Changes in the mineral composition of the Archean orthogneisses also corresponded to those described earlier, for example in References [81,82].
It can be assumed that a fenitization halo around the nepheline-syenite massifs was formed mainly during the late magmatic stage of their evolution, under the influence of several pulses of alkaline heterophase fluid, whose generation took place in the relatively narrow (up to 200 m) endocontact zone [83,84]. The separation of the fluid phase led to a change in the mineral and chemical composition of the rocks in this zone, which are very different from the nepheline syenites in the massif’s interior. Judging by the peculiar properties of the distribution of CH4 and 3He in the exocontact, the ratios of these components in different portions of the acting fluid was not the same. The formation temperatures of such fenitization halos are estimated to be 500–800 °C [84,85]. The maximum value in this zone of 3He/4He = 111 × 10−8 in the fenite 15 cm from the contact nearly coincides with the highest value found in the massif’s intrusive rocks. It is close to the upper estimate of the initial ratio in the trapped helium [70].
Thus, along with: (a) the features of the distribution of HCG in the rocks and minerals [4,14,22,66], (b) variations in the isotopic compositions of carbon and hydrogen [21,25,86] as well as noble gases [70], (c) the molecular mass distribution of gaseous alkanes [9,18,22,23] and (d) the data thermodynamic calculations [20,21], thermobarometry and Raman spectroscopy of the fluid microinclusions [64,65,87], the peculiarities of the relationship between the Lovozero hydrocarbon and the isotopes of noble gases could also indicate that the abiogenic generation HCG and their transformations occurred at different stages of the mineral formation.
In the magmatic stage, methane could appear in the fluid, particularly during the crystallization of aegirine and alkaline amphibole [13]. The interaction of water and previously formed graphite [20] is another probable way of generating hydrocarbon gases. As the temperature decreased under favorable conditions, reactions of the Fischer–Tropsch-type (RTFT)—(nCO2 + (3n + 1)H2 = CnH2n + 2 + 2nH2O) could have started. The iron-containing phases, aluminosilicates and especially the zeolites [88,89,90] and microporous aqueous titano-, niobo- and zircon-osilicates, to which accumulations of bituminous substances are constantly confined in these massifs [91], could also be the catalysts and promoters of such reactions that can self-sustain due to the heat generation. The initial RTFT, along with the magmatic CO2 and hydrogen, being a product of the evolution of the magmatic fluid, was probably also generated by the interaction of iron-containing minerals and aluminosilicates with water, which occurs during the formation of aegirine, magnetite, cancrinite and zeolites [7,64,65]. Together with other data, the results of this work show that the RTFT synthesis could be part of a complex multistage process of hydrocarbon formation, which included oxidation and dehydrogenation, polymerization and condensation reactions, and occurred during the further evolution of the system [88,92,93], when the magmatic was diluted fluid with circulating paleometeor waters.

5. Conclusions

Despite the long history of research, the origin of the hydrocarbon gases naturally occurring in some nepheline-syenite massifs in concentrations that are unusually high for magmatic complexes remains a subject of discussion. One of the approaches to understanding the nature of these gases in the Lovozero massif rocks involves coupling their distribution with the abundances of helium and argon isotopes, which are recognized as geochemical tracers. In our study, extraction of the gas components contained in fluid micro-inclusions was carried out by a mechanical grinding of rock and mineral samples.
Along with wide (mainly up to three orders of magnitude) variations in the characteristics of the gases in general, a positive correlation was found for such important indicators as 3He/4He and CH4/C2H6. In contrast, a negative correlation of the latter with the concentration of 36Ar was revealed. The distribution of 36Ar was also directly, to varying degrees, associated with the distribution of HCG, with this bond being strengthened along with increasing molecular weight. It turned out that the processes of increasing the share of heavier hydrocarbons in the composition of the gases, the loss of the deep component and the addition of the atmogenic one to the fluid phase, largely coincided in both time and space. In the absence of any correlation between CH4 and 3He, the value of the ratio of CH4/3He in the Lovozero gases substantially exceeded the estimates of the ratio in the gases of a mantle origin and mainly corresponded to the crustal values. Nevertheless, the observed ratios of methane and helium isotopes allowed for the presence of an insignificant fraction of mantle CH4, or at least the initial carbon, in the rocks of the lower series of DC and in the exocontact of the massif.
Together with other data, the peculiarities of the relationship between the Lovozero hydrocarbon and the isotopes of noble gases could indicate extended abiogenic generation and transformation of the HCG at different stages of the magmatic and post-magmatic mineral formation.
It seems that a more detailed study of the relationship between the distribution of HCG, H2 and noble gas (Ne, Ar and Ne) isotopes in the Lovozero and other nepheline-syenite massifs will significantly advance the long-standing problem of the origin of reduced gases in alkaline magmatic systems. Such studies should preferably be combined with the C and H isotopy and thermobarometry of fluid micro-inclusions.

Funding

This paper was prepared in the framework of State contract No 0226-2019-0051 of GI KSC RAS.

Acknowledgments

The author is very grateful to I. L. Kamensky for the methodological guidance and direct measurements of noble gas isotopes, S. V. Ikorsky for the methodological and technical support of gas chromatographic analyses, A. A. Avedisyan for performing part of the latter, and to the anonymous reviewer for valuable suggestions and comments.

Conflicts of Interest

The author declares no conflict of interest.

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Figure 1. Geological sketch-map of the Lovozero massif (based on the map of PGO Sevzapgeologiya). 1 and 2—rocks of the eudialyte and differentiated complexes, respectively; 3—marker ore horizons; 4—poikilitic and inequigranular feldspathoid syenites; 5—remnants of the sedimentary-volcanogenic series; sampling sites (the sample numbers correspond to those in Table 1): 6—natural outcrops; 7—boreholes; 8—underground mine workings.
Figure 1. Geological sketch-map of the Lovozero massif (based on the map of PGO Sevzapgeologiya). 1 and 2—rocks of the eudialyte and differentiated complexes, respectively; 3—marker ore horizons; 4—poikilitic and inequigranular feldspathoid syenites; 5—remnants of the sedimentary-volcanogenic series; sampling sites (the sample numbers correspond to those in Table 1): 6—natural outcrops; 7—boreholes; 8—underground mine workings.
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Figure 2. Correlations of the CH4/C2H6 and 3He/4He ratios. Samples: 1—eudialite complex; 2 and 3—differentiated complex, Series I + II and III–V, respectively; 4 and 5—endocontact and exocontact zones of the massif.
Figure 2. Correlations of the CH4/C2H6 and 3He/4He ratios. Samples: 1—eudialite complex; 2 and 3—differentiated complex, Series I + II and III–V, respectively; 4 and 5—endocontact and exocontact zones of the massif.
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Minerals 10 00830 g003 550
Figure 3. Relationships between the CH4/C2H6 ratios and 36Ar concentrations. The symbols are as in Figure 2.
Figure 3. Relationships between the CH4/C2H6 ratios and 36Ar concentrations. The symbols are as in Figure 2.
Minerals 10 00830 g003
Minerals 10 00830 g004 550
Figure 4. Correlations of the amount of pentanes and the 36Ar concentrations. The symbols are as in Figure 2.
Figure 4. Correlations of the amount of pentanes and the 36Ar concentrations. The symbols are as in Figure 2.
Minerals 10 00830 g004
Minerals 10 00830 g005 550
Figure 5. Relationship of the methane and 3He concentrations. Samples: 1—eudialite complex; 2 and 3—differentiated complex, Series I + II and III–V, respectively; 4 and 5—endocontact and exocontact zones of the massif. The inclined lines are equal ratios of CH4/3He.
Figure 5. Relationship of the methane and 3He concentrations. Samples: 1—eudialite complex; 2 and 3—differentiated complex, Series I + II and III–V, respectively; 4 and 5—endocontact and exocontact zones of the massif. The inclined lines are equal ratios of CH4/3He.
Minerals 10 00830 g005
Minerals 10 00830 g006 550
Figure 6. Plot of the CH4/3He vs. 3He/4He of abiogenic gases from the Lovozero massif and some other geological settings. The Lovozero samples are from: EC—eudialite complex, DC12 and DC3–5—differentiated complex (Series I and II and III–V, respectively), ENC and EXC—endocontact and exocontact of the massif, respectively. UMKS—ultramafites from the Kovdor and Seblyavr complexes of the Kola Alkaline Province ([72] and the unpublished author’s data), CSS—carbonatites from the Sallanlatva and Sokli complexes of the Kola Alkaline Province (unpublished author’s data), EPR—the East Pacific Rise 13° N and 21° N [43], MAR—the Mid-Atlantic Ridge (ibid), ZO—the Zambales Ophiolite in the Philippines [78] and CHS—hot springs in China [37]. The dashed lines show the crust and mantle fields [31,33,34,37,45,46,77,79]; VCVD—the Vicano–Cimino Volcanic District, Italy [44], and XASB—the Xujiaweizi area of the Songliao Basin, China [38].
Figure 6. Plot of the CH4/3He vs. 3He/4He of abiogenic gases from the Lovozero massif and some other geological settings. The Lovozero samples are from: EC—eudialite complex, DC12 and DC3–5—differentiated complex (Series I and II and III–V, respectively), ENC and EXC—endocontact and exocontact of the massif, respectively. UMKS—ultramafites from the Kovdor and Seblyavr complexes of the Kola Alkaline Province ([72] and the unpublished author’s data), CSS—carbonatites from the Sallanlatva and Sokli complexes of the Kola Alkaline Province (unpublished author’s data), EPR—the East Pacific Rise 13° N and 21° N [43], MAR—the Mid-Atlantic Ridge (ibid), ZO—the Zambales Ophiolite in the Philippines [78] and CHS—hot springs in China [37]. The dashed lines show the crust and mantle fields [31,33,34,37,45,46,77,79]; VCVD—the Vicano–Cimino Volcanic District, Italy [44], and XASB—the Xujiaweizi area of the Songliao Basin, China [38].
Minerals 10 00830 g006
Minerals 10 00830 g007 550
Figure 7. Distribution of the 3He and CH4 concentrations and 3He/4He and CH4/C2H6 ratios in the contact zone of the Lovozero massif. Symbols: 1—nepheline syenites of the endocontact; 2—fenites and fenitized gneisses; 3—unaltered gneisses; 4—sampling localities. From Reference [70], with minor modifications.
Figure 7. Distribution of the 3He and CH4 concentrations and 3He/4He and CH4/C2H6 ratios in the contact zone of the Lovozero massif. Symbols: 1—nepheline syenites of the endocontact; 2—fenites and fenitized gneisses; 3—unaltered gneisses; 4—sampling localities. From Reference [70], with minor modifications.
Minerals 10 00830 g007
Table
Table 1. Brief sample characteristics.
Table 1. Brief sample characteristics.
Sample NumberRock 1/MineralGeological Position 2
1Eudialyte feldspar urtite with lopariteEC
2Eudialyte foyaiteEC
3Eudialyte lujavriteEC
4Eudialyte lujavriteEC
5Eudialyte lujavriteEC
6Murmanite-eudyalite lujavriteEC
7Feldspar urtiteDC, I-1
8Loparite urtiteDC, I-4
9Zeolitized feldspar urtiteDC, I-4
10Nepheline from feldspar urtiteDC, I-4
11Feldspar from urtiteDC, I-4
12Sodalite from feldspar urtiteDC, I-4
13Feldspar urtiteDC, series I
14Zeolitized urtiteDC, II-4
15Loparite maligniteDC, II-4
16Zeolitized urtiteDC, II-5
17UrtiteDC, III-1
18Feldspar urtiteDC, series IV
19Ijolite-urtiteDC, series V
20Trachytoid feldspar urtiteDC, series V
21Trachytoid feldspar urtiteDC, series V
22Trachytoid feldspar urtiteDC, series V
23Nepheline from feldspar urtiteDC, series V
24Zeolitized foyaiteDC, above I-2
25FoyaiteDC, II-1
26Foyaite with villiaumite and eudialiteDC, II-3
27Analcime-bearing foyaiteDC, II-4
28Albitized foyaiteDC, II-4
29Zeolitized foyaiteDC, below II-4
30FoyaiteDC, below II-4
31Foyaite with sodalite and cancriniteDC, below II-4
32Nepheline from foyaiteDC, below II-4
33Feldspar from foyaiteDC, below II-4
34Clinopyroxene from foyaiteDC, below II-4
35Sodalite from foyaiteDC, below II-4
36Eudialite-bearing foyaiteDC, above II-5
37Eudialite-bearing foyaiteDC, above II-5
38Eudialite-bearing foyaiteDC, above II-5
39FoyaiteDC, below II-5
40FoyaiteDC, above II-7
41Apatite- and eudialite-bearing foyaiteDC, above III-1
42Foyaite with eudialiteDC, above III-1
43FoyaiteDC, above III-8
44Villiaumite-bearing foyaiteDC, III-14
45Villiaumite-bearing foyaiteDC, III-14e
46FoyaiteDC, above III-15
47Eudialite-bearing foyaiteDC, below III-16
48Eudialite-bearing foyaiteDC, below III-16
49FoyaiteDC, above IV-1
50FoyaiteDC, below IV-5
51FoyaiteDC, below IV-5
52Zeolitized lujavriteDC, I-4
53Zeolitized loparite lujavriteDC, I-4
54Lujavrite with amphiboleDC, II-7
55Amphibole lujavriteDC, series II
56LujavriteDC, III-14
57LujavriteDC, III-14
58Loparite lujavrite with villiaumiteDC, III-14
59Loparite lujavriteDC, III-14
60Poikilitic nepheline syeniteDC, below III-2
61Poikilitic nepheline syeniteDC, above III-14
62Coarse-grained nepheline syeniteENCM
63Coarse-grained nepheline syeniteENCM
64Coarse-grained nepheline syeniteENCM
65Pegmatoid nepheline syeniteENCM
66Pegmatoid nepheline syeniteENCM
67Pyroxene-feldspar feniteEXCM
68Pyroxene-feldspar feniteEXCM
69Fenitized gneissEXCM
70Fenitized gneissEXCM
71Fenitized gneissEXCM
72Fenitized gneissEXCM
73Biotite gneissEXCM
1 If other characteristics are not given, the rock is mesocratic medium-grained massive (all lujavrites are trachytoid). 2 DC is the differentiated complex (I-1–III-16 is the number of the series plus the number of the horizon (layer), EC is the eudialite complex, ENCM and EXCM are the endocontact and exocontact of the massif.
Table
Table 2. He and Ar isotope abundances and concentrations of hydrocarbon gases.
Table 2. He and Ar isotope abundances and concentrations of hydrocarbon gases.
Sample 14He
10−6 cm3/g		3He/4He
10−8		40Ar
10−6 cm3/g		40Ar/36ArCH4
10−3 cm3/g		C2H6
10−4 cm3/g		∑C5H12 2
10−7 cm3/g
10.912.02.552411.52.5n.a. 3
20.810.23.43785.02.0n.a.
30.617.53.360320.76.843.0
42.46.4n.a.n.a.2.51.46.4
53.35.81.54964.61.6n.a.
61.85.5n.a.n.a.1.41.1n.a.
72.14.2n.a.n.a.16.84.5n.a.
81901.0n.a.n.a.2.26.0n.a.
92607.2n.a.n.a.31.218.9n.a.
1071.07.74.557327.821.363.0
1120.38.54.151331.217.538.9
1233.08.87.836256.339.4137
132.32.21.259023.07.9n.a.
1447.03.0n.a.n.a.9.89.1n.a.
156321.0n.a.n.a.2.75.8n.a.
162.44.0n.a.n.a.7.79.5n.a.
1736.134.04.99443.71.4n.a.
185.315.37.7344635.810.1n.a.
1964.819.213.9360241.010.0n.a.
2063.715.8n.a.n.a.1.50.6n.a.
2132916.0n.a.n.a.16.33.87.3
2229520.02.249116.33.87.3
2329720.25.6276022.73.1n.a.
241.24.93.539417.77.4n.a.
251.64.11.44616.13.012.0
264.93.8n.a.n.a.20.55.3n.a.
2737.04.5n.a.n.a.13.03.4n.a.
2825.02.3n.a.n.a.0.40.2n.a.
2947.01.2n.a.n.a.26.314.6n.a.
302.24.3n.a.n.a.4.44.2n.a.
3121.95.2n.a.n.a.47.218.7n.a.
3242.55.34.266141.126.646.0
337.75.412.2114172.441.172.0
349.610.81.04001.81.1n.a.
3529.05.07.166147.931.482.0
361.16.5n.a.n.a.64.312.627.4
371.43.7n.a.n.a.5.63.39.9
380.88.6n.a.n.a.4.31.6n.a.
390.89.62.94815.34.6n.a.
402.09.44.511150.70.1n.a.
416.024.0n.a.n.a.73.733.5n.a.
427.726.8n.a.n.a.86.639.7360
4320.728.34.2156541.88.8n.a.
4425.526.06.2167596.633.3n.a.
456.825.22.779246.816.7n.a.
4632.029.13.968156.710.2n.a.
4732.025.0n.a.n.a.87.730.6n.a.
4824.030.2n.a.n.a.10136.4116
4930.340.06.854490.70.1n.a.
5018.723.65.0152455.714.8n.a.
5126.727.48.8143246.818.7n.a.
524.41.6n.a.n.a.0.10.1n.a.
531450.5n.a.n.a.0.50.8n.a.
546.33.2n.a.n.a.2.50.7n.a.
5514.42.1n.a.n.a.2.32.9n.a.
567.610.96.6157919.35.6n.a.
5713.015.06.111239.51.5n.a.
5849.51.65.0157214.38.0n.a.
5970.01.03.912318.67.4n.a.
6057.525.96.228362.00.7n.a.
6127.027.0n.a.n.a.1.10.5n.a.
621.54.8n.a.n.a.0.60.4n.a.
636.04.8n.a.n.a.6.04.1n.a.
640.84.4n.a.n.a.1.00.5n.a.
65n.a.n.a.n.a.n.a.0.90.4n.a.
661.03.7n.a.n.a.1.30.4n.a.
670.585.0n.a.n.a.2.90.51.3
680.5110.7n.a.n.a.4.50.4n.a.
690.878.0n.a.n.a.n.a.n.a.n.a.
707.093.0n.a.n.a.7.00.5n.a.
710.754.0n.a.n.a.13.00.8n.a.
72n.a.n.a.n.a.n.a.5.30.3n.a.
730.717.4n.a.n.a.1.9n.a.n.a.
1 The sample numbers correspond to those in Table 1. 2 iC5H12 + nC5H12. 3 n.a.—not analyzed.

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Nivin, V. The Origin of Hydrocarbon Gases in the Lovozero Nepheline-Syenite Massif (Kola Peninsula, NW Russia), as Revealed from He and Ar Isotope Evidence. Minerals 2020, 10, 830. https://doi.org/10.3390/min10090830

AMA Style

Nivin V. The Origin of Hydrocarbon Gases in the Lovozero Nepheline-Syenite Massif (Kola Peninsula, NW Russia), as Revealed from He and Ar Isotope Evidence. Minerals. 2020; 10(9):830. https://doi.org/10.3390/min10090830

Chicago/Turabian Style

Nivin, Valentin. 2020. "The Origin of Hydrocarbon Gases in the Lovozero Nepheline-Syenite Massif (Kola Peninsula, NW Russia), as Revealed from He and Ar Isotope Evidence" Minerals 10, no. 9: 830. https://doi.org/10.3390/min10090830

APA Style

Nivin, V. (2020). The Origin of Hydrocarbon Gases in the Lovozero Nepheline-Syenite Massif (Kola Peninsula, NW Russia), as Revealed from He and Ar Isotope Evidence. Minerals, 10(9), 830. https://doi.org/10.3390/min10090830

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