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Article

Graphite and Diamond Formation in the Carbide–Oxide–Carbonate Interactions (Experimental Modeling under Mantle P,T-Conditions)

by
Yuliya Bataleva
1,2,*,
Yuri Palyanov
1,2,
Yuri Borzdov
1,2,
Ivan Novoselov
1,2 and
Oleg Bayukov
3
1
Sobolev Institute of Geology and Mineralogy, Siberian Branch of Russian Academy of Sciences, Koptyug ave 3, Novosibirsk 630090, Russia
2
Department of Geology and Geophysics, Novosibirsk State University, Pirogova str 2, Novosibirsk 630090, Russia
3
Kirensky Institute of Physics, Siberian Branch of Russian Academy of Sciences, Akademgorodok 50, bld. 38, Krasnoyarsk 660036, Russia
*
Author to whom correspondence should be addressed.
Minerals 2018, 8(11), 522; https://doi.org/10.3390/min8110522
Submission received: 5 September 2018 / Revised: 8 November 2018 / Accepted: 8 November 2018 / Published: 11 November 2018
(This article belongs to the Section Crystallography and Physical Chemistry of Minerals & Nanominerals)
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Abstract

:
Experimental modeling of the formation of graphite and diamond as a result of carbide–fluid interactions was performed in the Fe3C–SiO2–Al2O3–(Mg,Ca)CO3 systems at 6.3 and 7.5 GPa and 1100–1650 °C. In the experiments with ƒO2-gradient (7.5 GPa, 1250–1350 °C), graphite + magnesiowüstite + garnet ± cohenite assemblage was formed. Graphite was produced through the redox interactions of carbide with carbonate or CO2 (reducing conditions), and redox reactions of magnesiowüstite and CO2 (oxidizing conditions). At 1450–1650 °C, crystallization of graphite, garnet, magnesiowüstite and ferrospinel, as well as generation of Fe2+,3+-rich carbonate–silicate melt occurred. This melt, saturated with carbon, acted as a medium of graphite crystallization and diamond growth on seeds. In the experiments without ƒO2-gradient (6.3 GPa), decarbonation reactions with the formation of CO2-fluid and Fe,Mg,Ca-silicates, as well as C0-producing redox reactions of CO2-fluid with cohenite were simultaneously realized. As a result, graphite (± diamond growth) was formed in assemblage with Fe2+,Fe3+,Mg-silicates and magnetite (1100–1200 °C), or with Fe3+-rich garnet and orthopyroxene (1300–1500 °C). It has been established that a potential mechanism for the crystallization of graphite or diamond growth is the oxidation of cohenite by CO2-fluid to FeO and Fe3O4, accompanied by the extraction of carbon from Fe3C and the corresponding reduction of CO2 to C0.

1. Introduction

Establishing the specific features of the redox profile throughout the Earth’s mantle with corresponding changes of structure, phase and chemical rocks compositions is one of the primary goals of modern mantle mineralogy and petrology. The oxidation state of mantle rocks may be defined by heterogeneous reactions between oxygen and iron- or carbon-bearing minerals [1,2]. Under redox conditions of the upper mantle, formation of metallic iron (or Fe–Ni alloy) occurs below the metal precipitation curve, the position of which is defined by the oxygen fugacity (ƒO2) at which Fe precipitates from mantle silicates, and the depth or pressure of metal precipitation line depends on bulk rock composition. Pressures of some metal precipitation reactions were established experimentally and theoretically [3,4,5,6,7,8], and it was predicted that, at depths greater than 250 km (P ≥ 7 GPa), the Earth’s mantle is reduced enough to become metal-saturated. More specifically, it was experimentally demonstrated [6] that pure metallic iron could be formed as a result of disproportionation reaction, where majoritic garnet acted as a sink for ferric iron, with Fe3+/ΣFe ratios varying from 0.02–0.12 (~7 GPa) to 0.4 (14 GPa). Besides the stabilization of Fe3+-bearing garnet species, presence of highly reduced metal-saturated mantle rocks at great depths has a number of petrologic consequences, affecting the behavior of redox-sensitive elements, e.g., carbon. Under these conditions, such carbon-bearing phases as carbides, diamond and graphite, as well as fluid [4,9,10,11], are stable. According to the data in [4,9,10,12], under metal-saturated conditions in the depleted mantle (20–120 ppm C), carbon presents as a solution in metal and in the undepleted mantle (300–800 ppm C) it presents as carbides (Fe3C and Fe7C3), diamond and graphite. Presence of iron carbides at great depths is evidenced by inclusions in diamonds [13,14,15,16,17]. Recent experimental studies [18,19,20] show that iron carbide participates in the deep carbon cycle processes, involving redox graphite- and diamond-forming reactions, metasomatic interactions, generation of Fe–C-based melts and formation of ferrous and ferric silicates.
Studies on the deep carbon cycle [9,21,22,23] demonstrate that subduction is one of the main mechanisms of the transport of carbonate-bearing rocks, oxidized melts and fluids into the Earth’s mantle. Discovery of xenoliths of strongly oxidized rocks with ƒO2~FMQ + 1 log unit [5,24] evidences that part of the lithospheric mantle was subjected to the action of mobile metasomatic agents—carbonate melts or oxidized components of C–O–H fluid [2,25,26,27,28]. Subduction of crustal material into the mantle also enables redox interactions between oxidized (carbonate–oxide–silicate) species and reduced metal- or carbide-bearing rocks [7]. Possibility of this interaction is confirmed by data on inclusions in diamonds, varying in composition from highly reduced [13,29,30,31], to oxidized, including silicates and oxides [32,33,34,35], carbonates and pure CO2 [36,37]. Recently, the model of diamond-forming mixing process was proposed based on the complex study of the carbon isotopic compositions of sub-lithospheric diamonds and oxygen isotopic compositions of inclusions therein [38]. The relationship between δ13C and δ18O for Brazil diamonds suggests the diamond formation via interaction of slab-derived carbonate melt with reduced (carbide- or metal-bearing) mantle and confirms the presence of iron carbide phase in the deep mantle.
To date, carbide behavior under mantle pressures and temperatures has been experimentally investigated in Fe–C, Fe–Ni–C, Fe–C–S and Fe–Ni–C–S systems [12,19,39,40,41,42], as well as in more complex systems, modeling carbide interaction with mantle minerals–oxides [43], sulfides [20] and carbonates [18]. However, there is a lack of studies devoted to the modeling of the iron carbide behavior in the presence of fluid, under silicate mantle P,T,x-conditions, which can be valuable sources of new data on mantle oxygen fugacity (ƒO2) patterns, potential graphite/diamond-producing processes and characteristic features of the formation of Fe-bearing silicates as well as carbonate-silicate melts.
The main goals of the present study, which can be achieved by high-pressure experiments, were: (1) to model carbide–fluid reactions in the carbide–oxide–carbonate systems at the pressures close to metal-precipitation line (6.3 and 7.5 GPa); (2) to reconstruct the graphite- and diamond-forming reactions, in which carbide and carbonate are both sources of carbon; and (3) to study the conditions of formation of ferric and ferrous silicates and Fe-rich carbonate-silicate melts under lithospheric mantle P,T-parameters.

2. Materials and Methods

Experiments were carried out using a multi-anvil high-pressure apparatus of a “split-sphere” type (BARS) [44] in the Fe3C–SiO2–Al2O3–(Mg,Ca)CO3 (carbide–oxide–carbonate) systems at the pressures of 6.3 and 7.5 GPa, in the temperature range of 1100∓1650 °C, and a run duration from 8 to 40 h. Details on high pressure cell design as well as the calibration data were published previously [45,46]. To model carbide–fluid interactions, oxide–carbonate mixtures were used as a CO2-fluid source due to the decarbonation reactions in high pressure-high temperature experiments. Silicates, formed via decarbonation, acted as a sink for oxidized iron. Initial reagents were synthetic Fe3C (cohenite), SiO2, Al2O3 (99.99% pure) as well as natural specimens of magnesite and dolomite (<0.05 wt % of impurities, Satka deposit, Urals, Russia). Cohenite was preliminarily synthesized in a Fe–C system at P = 5.7 GPa and T = 1450 °C, and thoroughly analyzed by X-ray powder diffraction (Stoe IPDS-2T diffractometer, STOE, Darmstadt, Germany). The initial mixture of the carbonates had a bulk composition of Mg0.9Ca0.1CO3. Proportions of initial materials (Table 1 and Table 2) were chosen to produce CO2-dominated fluid and garnet via decarbonation reaction (Reaction (1)) and to realize further interaction of these phases with cohenite (Reaction (2)):
3SiO2 + Al2O3 + 3(Mg,Ca)CO3 → (Mg,Ca)3Al2Si3O12 + 3CO2
2Fe3C + 3CO2 → 6FeOin silicates + 5C0
Two different methodical approaches were used for experiments at 6.3 and 7.5 GPa. The experimental technique and methodical approach for the series at 7.5 GPa (so-called “sandwich”-type experiments) was developed and described in detail in [47]. The elaborated technique made it possible to perform experimental modeling of fluid- and melt-generating processes as well as of redox interaction of these fluids and melts with Fe-rich mantle minerals (ilmenite, chromite, wüstite, Fe0, pyrrhotite, and cohenite) under P,T-conditions of the lithospheric mantle [18,47,48,49,50]. Using this technique ensures the formation of a redox gradient by separation of the reaction volume of ampoules into peripheral (carbonate–oxide, i.e., oxidized) and central (containing an iron concentrator, i.e., reduced) parts (Figure 1a). This enables decarbonation reactions and generation of Fe-enriched carbonate-bearing melts as well as C0-producing redox interaction of the newly formed fluid or melt with the Fe-concentrating phases under mantle P,T-parameters. It should be emphasized that “sandwich”-type experiments were developed to study specific reactions on a base of reaction zoning of samples, without reaching equilibrium conditions.
When assembling, an ampoule made of the pressed mixture of oxides and carbonates was placed into a Pt capsule (6 mm in outer diameter). A pellet made of pressed Fe3C was mounted in the center of this ampoule. Therefore, the iron-bearing phase was separated from the Pt-capsule. This methodical approach guarantees minimal iron loss, when even runs at 1650 °C and 7.5 GPa are characterized by Fe loss about 1.0–1.2 wt %, which is confirmed by analysis of Pt-capsule material after experiments and by the mass balance calculations. When assembling, synthetic diamond seed crystals of the cuboctahedral shape (~0.5 mm in size) were placed in the carbonate–oxide ampoule (Figure 1a) to estimate whether the redox conditions in the reaction ampoules correspond to the stability field of diamond and to evaluate the possibility of diamond growth.
The methodical approach used for the series of experiments in carbide–oxide–carbonate system at 6.3 GPa (so-called “mixture”-type experiments) was described in detail in [43]. Even though Pt is the optimal capsule material for experiments under high pressures and high temperatures, it cannot be used for Fe-bearing systems if there is a direct contact of Pt with phases of iron. Considering our previous experience in a field of carbide-involving experiments under mantle P,T-conditions [39,43], we used graphite as appropriate capsule material. These graphite capsules set the upper limit of the oxygen fugacity values in samples close to the C–CO buffer equilibrium [47]. Starting materials, placed in graphite capsules, were powdered (particle size ~10–20 µm) and thoroughly homogenized. It should be noted that some part of the iron carbide was added into charge as relatively large crystals (300∓400 µm) to enable the processes of the carbide–oxide, carbide–carbonate and carbide–silicate interactions. For this reason, a small excess of iron carbide relative to the other reagents of Reaction (1) was created. Diamond seed crystals of cuboctahedral habit (~500 µm in size) were placed into the ampoules, to evaluate the possibility of diamond growth under conditions of the experiments.
We should separately emphasize the problem of the oxygen fugacity buffering of the samples in the present research. Iron carbide and CO2 fluid are extremely fO2-contrast, with ∆fO2 of about 5 log units. When modeling carbide–fluid reactions, which can occur as a result of subduction of oxidized material in the deep reduced mantle, it is inappropriate to use outer buffer that will set ƒO2 values at IW level. If this were done, CO2 fluid, generated as a result of decarbonation reactions, would be immediately reduced to form elemental carbon without participation of iron carbide. Thus, in the “sandwich”-type experiments, we used excess of cohenite to model reduced conditions in the central part of the sample and, in “mixture”-type experiments, we used outer buffer—graphite capsules, setting upper limit of fO2 values close to C–CO (and FMQ) buffer, which are believed to be average upper mantle values.
The chemical composition of final phases was analyzed by energy dispersive spectroscopy (Tescan MIRA3 LMU scanning electron microscope, TESCAN, Brno, Czech Republic) and microprobe (WDS) analysis (Camebax-micro analyzer, CAMECA, Gennevilliers, France).
Microprobe analyses of silicates, oxides, and carbides were performed at an accelerating voltage of 20 kV, a beam current of 20 nA, a counting time of 10 s for each analytical line, and electron beam diameter of 2∓4 µm. The electron beam diameter of 20∓100 µm was used when studying the composition of microdendrites of quenched metal–carbon melt. Quantitative analysis (both microprobe and energy dispersive spectroscopy) of carbon performed using mineral standards of cohenite, calcite and magnesite. Polished samples and standards for microprobe were coated with carbon; samples for energy dispersive spectroscopy were coated with carbon for first series of analyses, and with chromium for second series of ones. The phase relationships were studied by scanning electron microscopy. Analytical studies mentioned above were performed at the Center for Collective Use of Multi-element and Isotopic Analysis of the Siberian Branch of the Russian Academy of Sciences. Analysis of the composition of iron-bearing phases and valence state of iron therein was performed using Mössbauer spectroscopy. Measurements were carried out at room temperature on a MS-1104Em spectrometer (Cordon, Rostov on Don, Russia) with a Co57(Cr) source and a powdered absorber with a thickness of 1∓5 mg/cm2. The methodology of measurements and analysis of Mössbauer spectra was described in detail in [51] (and Supplementary Information therein).

3. Results

3.1. Experimental Results in the Carbide–Oxide–Carbonate System at the Pressure of 7.5 GPa (“Sandwich”-Type Experiments with ƒO2-Gradient)

The results of experiments are shown in Table 3 and Figure 1. At relatively low temperatures (1250–1350 °C), reduced central parts of samples are presented by cohenite lenses (Figure 1b), surrounded by reaction zones (Figure 2a) of cohenite, magnesiowüstite, garnet and unevenly distributed graphite. The oxidized peripheral parts of samples are presented by garnet + magnesiowüstite + graphite assemblage. Initial growth patterns on (111) and (100) faces of diamond on seeds is established by SEM (Figure 2c). The compositions of the final phases from different zones of samples, established by microprobe analysis and Mössbauer spectroscopy, are shown in Table 4 and Table 5.
Cohenite in all samples demonstrates perfect stoichiometry with carbon content of ~6.7 wt %. The compositions of silicate and oxide phases crystallized in assemblage with iron carbide in the reduced parts of samples show higher FeO with respect to oxidized parts (Figure 3a). Thus, in central part of the samples, magnesiowüstite composition corresponds to Fe0.92Mg0.08O (1250 °C) and Fe0.9Mg0.1O (1350 °C), and garnets contain of ~13 wt % FeO. In the peripheral parts, composition of magnesiowüstite is of Fe0.84–0.85Mg0.15–0.16O (Table 4, Figure 3), and FeO content in garnets is of ~9–10 wt %. Mössbauer spectroscopy results show that the most abundant phase in the samples under 7.5 GPa and 1250–1350 °C is wüstite (Fe1-xO), which incorporates up to 80% of all Fe in the system. Wüstite from the reduced parts of the samples is found to be free of trivalent iron. In the oxidized parts of the samples, Fe3+/ΣFe values in wüstite amount up to 7.5% (Table 5). The carbide phase is identified only in the reduced part of the samples. Mössbauer parameters of silicates, revealed in the samples, corresponds to Fe2+ in garnet (Table 5 and Figure 4).
A principal scheme of the carbide–oxide–carbonate interaction at 7.5 GPa and in the temperature range of 1450–1650 °C is presented in Figure 1c. As a result of these experiments, cohenite is totally consumed, and reaction volume does not demonstrate subdivision to reduced and oxidized parts. However, in the central parts of the samples, large graphite crystals (up to 600 μm) with inclusions of cohenite and magnesiowüstite are formed (Figure 2b). These crystals are localized at the initial boundary between iron carbide and the carbonate–oxide ampoule. Growth of (100) and (111) faces of diamond seeds occurs, with the formation of the grown layers of ~70 and 120 μm, respectively. In the upper part of samples, pools of segregated carbonate–silicate melt are established (Figure 2d), in the central part—garnet + ferrospinel + graphite assemblage with interstitial melt (Figure 2e,f) was formed and crystallization of magnesiowüstite + garnet + graphite assemblage (Figure 2e) in the lower part occurred. The compositions of mineral phases and melt are constant within the samples. As temperature grows, garnet demonstrates a slight increase in FeO content from 18.2 (1450 °C) to 20.7 wt % (1650 °C), and magnesiowüstite is characterized by a MgO content of 8–9.5 wt % (Table 4 and Figure 3a). Ferrospinel has composition of ~(Fe0.5Mg0.5)(Al1.58Fe0.42)O. Quenched carbonate–silicate melt consists of orthopyroxene, ferromagnesite, garnet and magnetite microdendrites as well as graphite microspheres of 3–30 μm in size (Figure 2d–e). Bulk analysis of the quenched aggregates shows that SiO2 and Al2O3 content in the melt increases, and MgO and CaO concentrations decrease with temperature (Table 4). CO2 content in this melt is of 26–30 wt %. The Mössbauer spectroscopy data demonstrate that quenched carbonate–silicate melt, garnet and ferrospinel contain trivalent iron (Table 5 and Figure 4a). It is established that bulk aggregate of quenched carbonate–silicate melt is characterized by values of 0.18–0.19, and all Fe3+ therein presents in form of quenched magnetite; garnet, crystallized in this melt, has a value of ~0.20–0.22.

3.2. Experimental Results in the Carbide–Oxide–Carbonate System at the Pressure of 6.3 GPa (“Mixture”-Type of Experiments without ƒO2-Gradient)

The experimental results, compositions of final phases, and structures of experimental samples are given in Table 3 and Table 6 and in Figure 3b and Figure 5. An assemblage of garnet, orthopyroxene, magnetite, graphite, ± ferropericlase as well as small amounts of corundum and coesite are obtained at the lowest temperatures (1100∓1200 °C) (Figure 5b and Figure 6a). After experiments, there are no carbide and carbonate in ampoules. Magnetite occurs primarily in the ampoule parts where large carbide crystals were initially placed. Crystals of newly formed silicates and oxides are characterized by a size of 5∓20 μm. Graphite forms elongated crystals and their aggregates are up to 70 μm in size. According to the difference in iron concentrations, garnet can be subdivided into two groups, with FeO content of ~17 wt % and ~30 wt %, respectively. Higher-ferrous garnets occur primarily in the ampoule parts where large carbide crystals were initially placed. Orthopyroxene formed in the experiments has a homogeneous composition and is characterized by a FeO content of ~33 wt % and a very low CaO concentration of ~0.7 wt %.
At temperature of 1300 °C and pressure of 6.3 GPa, the carbide–oxide–carbonate interaction led to the formation of an assemblage of garnet, orthopyroxene, graphite, and magnetite (Figure 5b). The prevailing phase in the reaction volume of ampoules is garnet. Most garnet crystals have a zonal structure (Figure 6b); their central parts have high FeO content of about 28 wt %; their rims are characterized by higher concentrations of MgO as well as lower CaO concentrations (Table 6). The size of garnet crystals is 5∓40 μm. Some garnet crystals have inclusions of a quenched Fe–C melt and graphite. Fine-crystalline orthopyroxene, magnetite, and graphite present in interstices of a polycrystalline garnet aggregate (Figure 6b). The orthopyroxene composition is heterogeneous. The FeO concentration in orthopyroxene varies from 11.5 to 40.4 wt %.
At higher temperatures (1400 and 1500 °C), the carbide–oxide–carbonate interaction leads to the formation of the garnet + orthopyroxene+graphite assemblage (Figure 4b,c). Garnet is characterized by a homogeneous composition with high FeO content of about 28 wt % and a crystal size of ~30∓70 μm (Figure 6c). It should be separately noted that garnet has Fe3+/ΣFe values of 0.24 (Table 5). Garnet has inclusions of a quenched Fe–C melt and graphite. Interstices of the garnet matrix are comprised by a fine-crystalline aggregate of orthopyroxene and graphite. The parts of samples, where large carbide crystals were initially placed, contain highly-ferrous orthopyroxene and large graphite crystals (Figure 5C). The composition of orthopyroxene crystallized at 1400 °C and 1500 °C is Fe1.41Mg0.56Si2.02O6 and Fe1.22Mg0.34Ca0.33Si2.08O6, respectively (Table 6).
The experimental data and Mössbauer spectroscopy results revealed the main patterns of a Fe3+ distribution between the final phases. In the experiments at 6.3 GPa and 1100 °C, all ferric iron is included in magnetite. In a range of 1200∓1300 °C, Fe3+-garnet coexists with magnetite; at 1400 and 1500 °C, garnet is the only sink for ferric iron (Table 5 and Figure 4b,c). It should be noted that inclusions of a Fe–C melt are found in garnets enriched with ferric iron, which indicates the presence (and participation) of a predominantly metal melt in the processes of the crystallization of Fe3+-bearing garnet.

4. Discussion

4.1. General Reconstruction of Carbide–Oxide–Carbonate Interaction Processes

4.1.1. Carbide–Oxide–Carbonate System (“Sandwich”-Type Experiments, P = 7.5 GPa)

Results of the present study and previous experimental research [18,48] demonstrate that the main processes occurring in the system are redox interactions involving iron carbide and decarbonation reactions. In the reduced part of the reaction volume, redox interaction between carbonates and iron carbide are realized to produce an association of magnesiowustite + graphite + Ca-rich carbonate (Reaction (3)) [18]:
2Fe3C + 4(Mg,Ca)CO3 → 9(Fe,Mg,Ca)O + (Ca,Mg,Fe)CO3 + 5C0
Partial oxidation of cohenite results in the formation of Fe,Ca-bearing pyrope in the reaction zone by the parallel realization of Reactions (4) and (5):
3(Fe,Mg,Ca)O + 3SiO2 + Al2O3 → (Fe,Mg,Ca)3Al2Si3O12
3(Mg,Ca,Fe)CO3 + 3SiO2 + Al2O3 → (Fe,Mg,Ca)3Al2Si3O12 + 3CO2
In the course of decarbonation (Reaction (5)), minor amounts of CO2 fluid are released and then consumed via redox interaction with iron carbide that results in the formation of graphite near the boundary of the central reduced zone with the peripheral oxidized part of the sample (Reaction (2)). In the oxidized part of the reaction volume, crystallization of garnet proceeds through decarbonation (Reaction (5)) with CO2 fluid generation (Figure 7). However, part of garnet crystallizes in experiments as a result of (Fe,Mg)O–SiO2–Al2O3 interaction without the participation of carbonate. Mössbauer data on the formation of Fe3+-bearing magnesiowüstite evidence that crystallization of graphite in the oxidized part of the reaction volume in assemblage with garnet and magnesiowüstite (Figure 1b) can occur via redox interaction of magnesiowüstite with CO2 fluid (Reaction (6)). During reduction of CO2 to C0, ferrous iron from magnesiowüstite is partially oxidized to Fe3+:
(Fe,Mg)O + CO2 → 3(Fe2+,Mg, Fe3+)1−xO + 2C0
The phase compositions of reduced and oxidized parts of the samples show that, at the temperature range of 1250–1350 °C, redox gradient is preserved in the reaction ampoule. In the center of the samples, where only cohenite is present, and in the reaction zone consisted of cohenite, magnesiowüstite, garnet and graphite, the ƒO2 values are close to those of the iron–wüstite buffer. In the peripheral oxidized part of the ampoule, where Fe3+-bearing magnesiowüstite + garnet + graphite assemblage are formed, ƒO2 values are close to CCO buffer (moreover, these are provided by graphite capsules).
Under higher temperatures (1450–1650 °C), final samples do not demonstrate subdivision into reduced and oxidized parts; however, redox gradient at early stages of experiments can be considered as a powerful driving force of the phase formation processes. During carbide–oxide–carbonate interaction, a series of processes are realized, involving redox interaction between carbonates and iron carbide, decarbonation reactions and partial melting. Most probably, at the first stages of interaction, phase formation occurred through Reaction (3), with Fe,Mg,Ca-carbonates, magnesiowüstite and graphite crystallization, as well as decarbonation (Reaction (5)) which led to the formation of Fe-enriched garnet and CO2 fluid. Next, the generation of carbonate–silicate melt occurs. As a result, the redox interaction of carbonate-bearing melt and CO2 fluid with cohenite, crystallization of graphite takes place. This process is accompanied by the melt enrichment in FeO:
Fe3C + Lcarb-sil → Lcarb-sil + FeOin melt + C0
When iron carbide is totally consumed, redox Reaction (7) is discontinued, and, in the central part of the reaction volume, large graphite crystals with inclusions of cohenite are formed. After finishing of this redox interaction, the smoothing of fO2 gradients in the samples occurs, with overall fO2 values close to CCO buffer. The interaction of iron oxides dissolved in the carbonate–silicate melt with CO2 fluid, released via decarbonation, results in a partial oxidation of Fe2+ to Fe3+ and the melt saturation with elemental carbon and crystallization of graphite:
FeOin melt + CO2 → Fe3O4 in melt + C0

4.1.2. Carbide–Oxide–Carbonate System (“Mixture”-Type experiments)

Based on a detailed study of experimental samples and data of previous studies [55,56], we conclude that the main processes of carbide–oxide–carbonate interaction at the lowest temperatures (1100∓1200 °C) include: (i) decarbonation resulting in the release of a CO2-dominated fluid and the formation of garnet and orthopyroxene (Reactions (1) and (9)); and (ii) the subsequent redox interaction between iron carbide and the resulting fluid (Reaction (10)):
2(Mg,Ca)CO3 + 2SiO2 → (Mg,Ca)2Si2O6 + 2CO2
3Fe3C + 5CO2 → 6FeOin silicates, oxides + FeFe2O4 + 8C0
Decarbonation plays a key role in the phase formation processes in the carbide–oxide–carbonate system. It should be noted that the temperatures of partial and complete decarbonation of the cohenite-involving system are in good agreement with ones in the (Mg,Ca)CO3–SiO2–Al2O3–FeO system at similar pressures [51]. In the experiments, decarbonation reactions occurred at 1100 °C, whereas according to Knoche co-authors [53], decarbonation with formation of pure pyrope at 6.3 GPa can proceed at temperatures higher than 1400 °C. Using the calculation results [54] and experimental data [53] for reconstructing the decarbonation curve of a produced solid solution of Alm70Prp20Grs10 garnet, typical of carbonated eclogites EC1, we found that at 6.3 GPa decarbonation started at about 1100 °C (Figure 7).
We found that the redox interaction (Reaction (10)) leads to: (i) oxidation of cohenite to magnetite (separate phase) and FeO (in silicates and oxides), which is accompanied by carbon extraction and graphite crystallization; and (ii) reduction of CO2 fluid by cohenite to C0 (graphite). Therefore, if Reactions (2), (9), and (10) proceed simultaneously, an assemblage of Fe-rich silicates, graphite, and magnetite forms. According to Mössbauer spectroscopy, all ferric iron formed during cohenite oxidation is included in magnetite. It should be noted that decarbonation of the system at these temperatures is complete, but initial oxides partially remain in the reaction volume. Given the initial proportions of SiO2, Al2O3, MgCO3, and CaMg(CO3)2, the absence of carbonates among final phases indicates that there was a redox interaction between magnesite and iron carbide, which is confirmed by the presence of ferropericlase in the reaction volume:
2/3Fe3C + MgCO3 → 3(Mg,Fe)O + 5/3C0
The performed experiments indicate that complete decarbonation of the system (Reactions (1) and (9)), redox interaction between CO2-fluid and iron carbide (Reaction (12)), and partial melting occur in a temperature range of 1300∓1500 °C:
3Fe3C + 3CO2 → 6FeOin silicates + 3Fe–Cmelt + 5C0
The redox interaction (Reaction (12)) leads to the formation of elemental carbon (graphite ± diamond growth), a Fe–C melt, and also FeO that does not form an independent phase, but is included in silicates (garnet and orthopyroxene). In this case, new portions of a CO2-fluid formed at subsequent stages of experiments are involved the redox interaction with a Fe–C melt:
3Fe–Cmelt + 3CO2 → 6FeOin silicates + 4C0
Reactions (12) and (13) lead to complete oxidation of cohenite and a Fe–C melt, which results in the formation of an assemblage of Fe-rich garnet, Fe-rich orthopyroxene, and graphite as well as in diamond growth on seed crystals (1500 °C). All ferric iron formed in these reactions is concentrated in garnet.
A set of phases produced in the experiments at 1100∓1300 °C (Fe2+-bearing silicates, magnetite, and graphite) designates ƒO2 values close to the C–CO and wüstite–magnetite (WM) buffer equilibria. In this temperature range, ƒO2 values characteristic of the WM buffer are within the stability field of elemental carbon. A Fe2+,Fe3+-garnet + graphite assemblage produced at higher temperatures does not contain phase-markers of redox conditions, but, given Fe2+ and Fe3+ proportions in garnet, its oxygen fugacity values may be estimated as close to the WM buffer and definitely not higher than CCO one (this upper ƒO2 limit is set by outer graphite capsules).

4.2. Reconstruction of Elemental Carbon Formation Processes

One of the key issues addressed in modern studies on diamond formation in nature is the problem of a carbon source in the processes of mantle diamond formation. Potential carbon sources include C–O–H–N fluid species, carbonates (carbonate-bearing melts), carbides, and metal–carbon melts [2,12,27,32,57,58,59]. Most of these hypotheses are confirmed by experiments [60,61,62,63,64]. It should be noted that experimental studies of the role of iron carbides in natural diamond formation are now very rare. In this section, we propose potential mechanisms for the formation of graphite and diamond growth in a course of carbide–oxide–carbonate interaction.

Graphite Formation and Diamond Growth from Carbon of Carbide and Carbonate

Reconstruction of the processes of phase formation in the carbide–oxide–carbonate system revealed the characteristic features of graphite formation and diamond growth in carbon-producing processes in relatively low- (1100∓1200 °C) and high-temperature (1300∓1500 °C) experiments. Crystallization of metastable graphite occurs in the entire temperature range, and diamond growth on seed crystals is observed at a temperature of 1500 °C. It should be noted that a carbon source in this system is not only carbide but also carbonate. At relatively low temperatures, graphite forms due to simultaneous realization of the decarbonation reactions (Reactions (1) and (9)) and the redox interaction between a CO2-dominated fluid and iron carbide (Reaction (2)). This redox interaction may be considered as a basis for reconstruction of the mechanism of graphite formation in a temperature range of 1100∓1200 °C. The formation of graphite from carbon of carbide occurs during oxidation of cohenite by the fluid to FeO and Fe2O3 (in form of magnetite, silicates, and oxides) and is due to accompanying extraction of carbon from Fe3C. Oxidation of the cohenite is accompanied by a corresponding reduction of CO2 to C0, leading to crystallization of metastable graphite, the source of which is carbonate. We suppose that the most likely environment for graphite formation by this mechanism is the CO2-dominated fluid.
At higher temperatures, the formation of metastable graphite was found to occur both via the described mechanisms and via the redox interaction between the CO2-dominated fluid and a predominantly metal melt (Fe–C), according to Reaction (13). Under these conditions, the formation of metastable graphite (1300∓1500 °C) and diamond growth on seed crystals (1500 °C) occur due to complete oxidation of a Fe–C melt by the fluid, which is accompanied by the formation of Fe2+,Fe3+-bearing silicates and, correspondingly, due to reduction of the CO2-dominated fluid to C0. We suppose that media for graphite crystallization and diamond growth via this mechanism are both CO2-dominated fluid and Fe–C melt, and both carbide and carbonate acted as carbon sources.
One of the potential reasons for crystallization of graphite in the P,T-field of diamond stability is the inhibitory effect of impurities present in the melt, e.g., oxygen and nitrogen adsorbed on the starting reagents. Investigation of diamond crystallization in metal–carbon systems in the presence of impurities demonstrated that ~0.48 wt % H2O or ~0.1 wt % nitrogen in a Fe–Ni–C melt was sufficient for the formation of metastable graphite in the thermodynamic stability field of diamond [44,65].

4.3. Scenarios of the Cohenite–Fluid Interaction in the Presence of Silicates in Natural Deep Mantle Environments

The experimental results as well as data of thermodynamic calculations indicate that oxygen fugacity values in the lithospheric mantle at depths of about 250 km correspond to those of the iron–wüstite buffer [3,5,6,7,8]. The content of metallic iron spread to a metal-saturated mantle at depths of ~250 km is estimated to be ~0.1∓0.2 wt % (1400 ppm) [6,7]. Previous studies [4,9,10] demonstrated that at bulk carbon concentrations corresponding to undepleted mantle conditions (300∓800 ppm C), iron is most likely included in carbides (Fe3C and Fe7C3).
An interaction between cohenite and CO2-fluid or carbonate–silicate melts very likely occurs under lithospheric mantle conditions where it may be considered as one of the potential C0-producing processes [38] as well as a potential mechanism of Fe2+,3+-bearing garnet formation. In addition, the processes of graphite or diamond formation by carbon extraction from carbide are accompanied by the generation of a predominantly metal melt at temperatures substantially lower than cohenite melting temperatures. During subduction of crustal material to great depths, highly reduced phases may interact with an oxidized slab that is a source of carbonates and CO2 fluid. Under subduction conditions, the most typical reactions are decarbonation processes occurring during the interaction between carbonate material and mantle oxides or silicates. However, subducted Mg–Ca carbonates can be stable up to lower mantle depths [32,59,66]. As shown in studies [45,54,67] the presence of iron can significantly reduce the temperature of decarbonation onset and trigger the formation of CO2 fluid and Fe-rich silicates. It should be noted, that phase assemblages of highly ferrous silicates are definitely not representative as mantle rock-forming minerals, they can only demonstrate micro-volumes of mantle, which are in direct contact with carbide. Results of the present study regarding Fe-rich silicates can be useful in a course of reconstruction of the very complex processes of natural rock formation, especially subduction-related or metasomatic.
We suppose that experimentally reproduced decarbonation processes involving carbide or a predominantly metal melt together with accompanying graphite- or diamond-producing redox reactions may occur locally in natural environments, under conditions of oxidized material subduction in a metal-saturated mantle.

5. Conclusions

(1) It was experimentally demonstrated that carbide–oxide–carbonate interaction led to decarbonation, with the formation of Fe,Mg,Ca-garnet and CO2 fluid, and graphite or diamond-producing redox reactions, involving iron carbide, mantle oxidized fluids, melts, carbonates, Mg,Fe silicates and oxides.
(2) Carbide–oxid–carbonate interaction realized in the experiments with ƒO2-gradient at 7.5 GPa and 1250–1350 °C resulted in the crystallization of magnesiowüstite + garnet + graphite ± cohenite assemblage. Graphite under reduced conditions was produced through the redox interactions of carbide with carbonate or CO2, and, under the oxidized conditions, as a result of the redox reaction of magnesiowüstite and CO2. At 1450–1650 °C, carbide–oxide–carbonate interactions resulted in the formation of Fe3+-magnesiowüstite + Fe3+-garnet + graphite assemblage as well as generation of Fe2+,3+-rich carbonate–silicate melt. This melt, saturated with carbon, acted as a medium of graphite crystallization and diamond growth on seeds.
(3) The experiments without ƒO2-gradient at 6.3 GPa demonstrated that carbide–oxide–carbonate interaction was accompanied by decarbonation reactions with the formation of Fe,Mg,Ca-silicates and CO2 fluid as well as by carbon-producing redox reactions between the CO2 fluid and cohenite. These processes resulted in the formation of Fe2+,Fe3+,Mg-silicate + magnetite + graphite assemblages (1100∓1200 °C) and Fe3+-bearing garnet + orthopyroxene + graphite (± diamond growth) (1300∓1500 °C).
(4) Potential mechanisms for crystallization of graphite or diamond during the carbide–oxide–carbonate interaction are oxidation of cohenite by CO2 fluid or carbonate–silicate melt to FeO and Fe2O3, which is accompanied by carbon extraction from Fe3C and corresponding reduction of CO2 or carbonate component of the melt to C0.

Author Contributions

Conceptualization, Y.B. (Yuliya Bataleva) and Y.P.; Data curation, Y.B. (Yuliya Bataleva) and Y.P.; Formal analysis, Y.B. (Yuliya Bataleva), I.N. and O.B.; Investigation, Y.B. (Yuliya Bataleva), Y.P. and Y.B. (Yuri Borzdov); Methodology, Y.B. (Yuri Borzdov); Visualization, Y.B. (Yuliya Bataleva); Writing—original draft, Y.B. (Yuliya Bataleva); Writing—review & editing, Y.B. (Yuliya Bataleva) and Y.P.

Funding

This work was supported by the Russian Foundation for Basic Research (project No. 16-35-60024) and a State Assignment (project No. 0330-2016-0007) and the Russian Science Foundation (grant No. 16-17-10041).

Acknowledgments

The authors express their sincere thanks to the in-house Editor, the guest Academic Editor, and three anonymous Reviewers for helpful and constructive reviews. The authors thank S. Ovchinnikov for his assistance in implementation of Mössbauer spectroscopy measurements and A. Moskalev for his assistance in the work preparation.

Conflicts of Interest

The authors declare no conflict of interest.

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Minerals 08 00522 g001 550
Figure 1. Schemes of carbide–oxide–carbonate interaction after “sandwich-type” experiments (Fe3C-Al2O3-SiO2-(Mg,Ca)CO3 system, P = 7.5 GPa): (a) initial ampoule assembly (before experiments); (b) samples after experiments at 1250–1350 °C, t = 30 h; and (c) samples after experiments at 1450–1650 °C, t = 8–20 h. Grt, garnet; Coh, cohenite; Mws, magnesiowustite; Fsp, ferrospinel; Gr, graphite; L, carbonate–silicate melt; Dm, diamond seeds.
Figure 1. Schemes of carbide–oxide–carbonate interaction after “sandwich-type” experiments (Fe3C-Al2O3-SiO2-(Mg,Ca)CO3 system, P = 7.5 GPa): (a) initial ampoule assembly (before experiments); (b) samples after experiments at 1250–1350 °C, t = 30 h; and (c) samples after experiments at 1450–1650 °C, t = 8–20 h. Grt, garnet; Coh, cohenite; Mws, magnesiowustite; Fsp, ferrospinel; Gr, graphite; L, carbonate–silicate melt; Dm, diamond seeds.
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Figure 2. SEM-micrographs (BSE-regime) of polished fragments of the samples (”sandwich”-type experiments, 7.5 GPa): (a) cohenite, magnesiowustite, garnet and graphite assemblage (reduced part of the sample, 1250 °C); (b) large graphite crystal with inclusions of cohenite and magnesiowustite, in a garnet + magnesiowustite + graphite aggregate (1550 °C); (c): growth patterns at (111) face of the diamond seed (1350 °C); (d) garnet and graphite in the quenched carbonate–silicate melt (1550 °C); (e) garnet in the quenched carbonate–silicate melt, at the contact with magnesiowustite + garnet + graphite polycrystalline aggregate (1450 °C); and (f) garnet, graphite and ferrospinel crystals in the quenched carbonate–silicate melt (1550 °C); Grt, garnet; Coh, cohenite; Mws, magnesiowüstite; Fsp, ferrospinel; Gr, graphite; Lcarb-sil, carbonate–silicate melt.
Figure 2. SEM-micrographs (BSE-regime) of polished fragments of the samples (”sandwich”-type experiments, 7.5 GPa): (a) cohenite, magnesiowustite, garnet and graphite assemblage (reduced part of the sample, 1250 °C); (b) large graphite crystal with inclusions of cohenite and magnesiowustite, in a garnet + magnesiowustite + graphite aggregate (1550 °C); (c): growth patterns at (111) face of the diamond seed (1350 °C); (d) garnet and graphite in the quenched carbonate–silicate melt (1550 °C); (e) garnet in the quenched carbonate–silicate melt, at the contact with magnesiowustite + garnet + graphite polycrystalline aggregate (1450 °C); and (f) garnet, graphite and ferrospinel crystals in the quenched carbonate–silicate melt (1550 °C); Grt, garnet; Coh, cohenite; Mws, magnesiowüstite; Fsp, ferrospinel; Gr, graphite; Lcarb-sil, carbonate–silicate melt.
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Figure 3. Temperature dependence of FeO content in silicate and oxide phases: (a) “sandwich”-type experiments, P = 7.5 GPa; and (b) “mixture”-type experiments, P = 6.3 GPa.
Figure 3. Temperature dependence of FeO content in silicate and oxide phases: (a) “sandwich”-type experiments, P = 7.5 GPa; and (b) “mixture”-type experiments, P = 6.3 GPa.
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Figure 4. Room-temperature Mössbauer spectra: (a) spectra of different zones of samples after “sandwich”-type experiments at 7.5 GPa, T = 1550 °C ((1) quenched carbonate–silicate melt; and (2) polycrystalline garnet aggregate with quenched melt in interstices); and (b,c) spectra of garnets and orthopyroxenes after “mixture”-type experiments at 6.3 GPa, T = 1400 and 1500 °C, respectively; Grt, garnet; Opx, orthopyroxene.
Figure 4. Room-temperature Mössbauer spectra: (a) spectra of different zones of samples after “sandwich”-type experiments at 7.5 GPa, T = 1550 °C ((1) quenched carbonate–silicate melt; and (2) polycrystalline garnet aggregate with quenched melt in interstices); and (b,c) spectra of garnets and orthopyroxenes after “mixture”-type experiments at 6.3 GPa, T = 1400 and 1500 °C, respectively; Grt, garnet; Opx, orthopyroxene.
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Figure 5. Schemes of carbide–oxide–carbonate interaction in the “mixture-type” experiments (Fe3C–Al2O3–SiO2–(Mg,Ca)CO3 system, P = 6.3 GPa): (a) initial ampoule assembly (before experiments); (b) samples after experiments at 1100–1200 °C, t = 30–40 h; and (c) samples after experiments at 1300–1500 °C, t = 20 h. Grt, garnet; Coh, cohenite; Mgt, magnetite; Opx, orthopyroxene; Fe-Opx, Fe-rich orthopyroxene; Gr, graphite; Fe3+-Grt, garnet, enriched with trivalent iron, Fpc, ferropericlase.
Figure 5. Schemes of carbide–oxide–carbonate interaction in the “mixture-type” experiments (Fe3C–Al2O3–SiO2–(Mg,Ca)CO3 system, P = 6.3 GPa): (a) initial ampoule assembly (before experiments); (b) samples after experiments at 1100–1200 °C, t = 30–40 h; and (c) samples after experiments at 1300–1500 °C, t = 20 h. Grt, garnet; Coh, cohenite; Mgt, magnetite; Opx, orthopyroxene; Fe-Opx, Fe-rich orthopyroxene; Gr, graphite; Fe3+-Grt, garnet, enriched with trivalent iron, Fpc, ferropericlase.
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Figure 6. SEM-micrographs (BSE-regime) of polished fragments of the samples (“mixture”-type experiments, Fe3C–Al2O3–SiO2–(Mg,Ca)CO3 system, P = 6.3 GPa): (a) polycrystalline aggregate of newly-formed garnet, orthopyroxene, magnetite and graphite and recrystallized cohenite and corundum (1100 °C); (b) zoned garnet crystals with magnetite + graphite in the interstitials (1300 °C); and (c) graphite + Fe-rich orthopyroxene assemblage in polycrystalline garnet aggregate (1500 °C). Grt, garnet; Opx, orthopyroxene; Cor, corundum; Co, coesite; Mgt, magnetite; Opx, orthopyroxene; Gr, graphite; Fe-Opx, Fe-rich orthopyroxene; Fpc, ferropericlase.
Figure 6. SEM-micrographs (BSE-regime) of polished fragments of the samples (“mixture”-type experiments, Fe3C–Al2O3–SiO2–(Mg,Ca)CO3 system, P = 6.3 GPa): (a) polycrystalline aggregate of newly-formed garnet, orthopyroxene, magnetite and graphite and recrystallized cohenite and corundum (1100 °C); (b) zoned garnet crystals with magnetite + graphite in the interstitials (1300 °C); and (c) graphite + Fe-rich orthopyroxene assemblage in polycrystalline garnet aggregate (1500 °C). Grt, garnet; Opx, orthopyroxene; Cor, corundum; Co, coesite; Mgt, magnetite; Opx, orthopyroxene; Gr, graphite; Fe-Opx, Fe-rich orthopyroxene; Fpc, ferropericlase.
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Figure 7. P,T-diagram with experimental results of the carbide–oxide–carbonate interaction “sandwich”-type (circles) and “mixture”-type (rhombs) experiments, with experimentally determined or calculated decarbonation curves [52,53,54]. Color of symbols denotes variations in Fe-bearing phases. Calculated shift of Reactions (1) and (2), which results in Reaction (3), are shown according to EC1 garnet compositions [54]. Co, coesite; Dol, dolomite; Di, diopside; Ms, magnesite; En, enstatite; Ky, kyanite; Prp, pyrope; Grs, grossular.
Figure 7. P,T-diagram with experimental results of the carbide–oxide–carbonate interaction “sandwich”-type (circles) and “mixture”-type (rhombs) experiments, with experimentally determined or calculated decarbonation curves [52,53,54]. Color of symbols denotes variations in Fe-bearing phases. Calculated shift of Reactions (1) and (2), which results in Reaction (3), are shown according to EC1 garnet compositions [54]. Co, coesite; Dol, dolomite; Di, diopside; Ms, magnesite; En, enstatite; Ky, kyanite; Prp, pyrope; Grs, grossular.
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Table
Table 1. Mass proportions of starting materials.
Table 1. Mass proportions of starting materials.
Experimental SeriesP, GPaStarting Materials, mg
Fe3CSiO2Al2O3MgCO3CaMg(CO3)2
“Mixture-type”6.324.629.516.811.02.8
“Sandwich-type”7.572.233.718.937.89.5
Table
Table 2. Bulk compositions of the carbide–oxide–carbonate systems.
Table 2. Bulk compositions of the carbide–oxide–carbonate systems.
Experimental SeriesP, GPaMass Concentrations, wt %Molar Concentrations, mol %
SiAlFeMgCaCOSiAlFeMgCaCO
“Mixture-type”6.315.610.126.14.51.54.637.612.88.610.74.30.98.754.0
“Sandwich-type”7.58.65.536.77.42.57.032.37.44.915.87.41.514.248.8
Table
Table 3. Results of experiments in the carbide–oxide–carbonate systems at 6.3 and 7.5 GPa.
Table 3. Results of experiments in the carbide–oxide–carbonate systems at 6.3 and 7.5 GPa.
Run NP, GPaT, °Ct, hFinal PhasesDiamond Growth on Seeds
”Mixture-type” experiments
CG-016.3110040Grt, Opx, Mgt, Cor, Co, Fpc, Gr-
CG-026.3120030Grt, Opx, Mgt, Cor, Co, Fpc, Gr-
CG-036.3130020Grt, Opx, Gr, Mgt-
CG-046.3140020Grt, Opx, Gr-
CG-056.3150020Grt, Opx, Gr+
”Sandwich-type” experiments
ST-017.5125030Coh, Grt, Mws, Gr+
ST-027.5135020Coh, Grt, Mws, Gr+
ST-037.5145020Grt, Mws, Fsp, Gr, Lcarb-sil+
ST-047.5155020Grt, Mws, Fsp, Gr, Lcarb-sil+
ST-057.516508Grt, Mws, Fsp, Gr, Lcarb-sil+
Grt, garnet, Opx, orthopyroxene, Mgt, magnetite, Fpc, ferropericlase, Coh, cohenite, Cor, corundum, Fe–Cmelt, metal–carbon melt, Co, coesite, Gr, graphite, Fsp, ferrospinel, Mws, magnesiowüstite, Lcarb-sil, carbonate–silicate melt.
Table
Table 4. Average compositions of silicates and oxides in the carbide–oxide–carbonate system (“sandwich-type” experiments) at 7.5 GPa, according to microprobe analysis.
Table 4. Average compositions of silicates and oxides in the carbide–oxide–carbonate system (“sandwich-type” experiments) at 7.5 GPa, according to microprobe analysis.
Run NT, °CPhaseNAMass Concentrations, wt %
SiO2Al2O3FeOFeO *Fe2O3 *MgOCaOTotal
ST-011250Grt P1441.6 (7)23.1 (5)8.9 (8)9-16.9 (5)9.5 (4)100.0
Mws P16--89.7 (7)8469.5 (8)0.33 (6)99.6
Grt C1540.9 (3)21.8 (1)13.4 (3)13-15.2 (3)8.5 (4)99.8
Mws C14--94.7 (3)95-4.6 (2)0.03 (1)99.4
ST-021350Grt P1742.3 (3)23.1 (3)10.3 (6)23-20.7 (7)3.3 (7)99.8
Mws P11--90.7 (5)8468.8 (5)0.03 (1)99.5
Grt C1441.0 (1)21.7 (1)13.2 (1)22-15.1 (2)8.6 (4)99.7
Mws C16--93.4 (9)93-5.8 (9)0.02 (0)99.3
ST-031450Grt1740.2 (4)22.5 (1)18.2 (3)14414.9 (6)3.57 (6)99.5
Mws14--89.9 (2)90-9.41 (6)0.04 (1)99.3
Fsp51.9 (1)47.9 (1)37.3 (2)30712.0 (1)-99.1
Lcarb-sil3011.0 (8)0.1 (1)36 (1)30616 (1)7 (1)70.1
ST-041550Grt2040.4 (4)21.4 (4)20.3 (2)16414.7 (2)2.5 (2)99.4
Mws15--91.7 (4)92-7.88 (1)0.03 (1)99.7
Fsp72.0 (1)48.5 (2)37.6 (3)31711.9 (6)-100.0
Lcarb-sil3112.8 (9)2.0 (4)43 (1)341011.5 (9)5 (1)74.2
ST-051650Grt2140.2 (3)21.3 (4)20.7 (3)16514.4 (2)3.0 (2)99.6
Mws16--91.2 (7)91-8.2 (2)0.03 (1)99.4
Fsp61.8 (1)53.0 (3)31.8 (3)27513.9 (9)-100.4
Lcarb-sil3015.0 (9)3.5 (7)42.7 (8)331011.0 (8)4.1 (9)76.3
Data were taken from the polished samples, coated with carbon. Grt, garnet, Mws, magnesiowustite, Fsp, ferrospinel, Lcarb-sil, carbonate–silicate melt, Fetot, total Fe2+ and Fe3+; NA, number of electron probe analyses. The values in parentheses are one sigma errors of the means reported as least units cited; P, peripheral zone; C, central zone; *, calculated according to Mössbauer spectroscopy data.
Table
Table 5. 57Fe Mössbauer data for silicates, carbonates, oxides and melts.
Table 5. 57Fe Mössbauer data for silicates, carbonates, oxides and melts.
Run NP, GPaT, °CSamplePhaseIron ValenceA, %Fe3+/∑Fe
ST-017.51250Central (reduced) partCohFe018-
MwsFe2+76-
GrtFe2+ (8)6-
Peripheral (oxidized) partMwsFe2+74-
Fe3+ (4)60.075
GrtFe2+ (8)20-
ST-047.51550Quenched carbonate–silicate meltCarb *Fe2+ (6)620.18 (in melt, bulk)
Mgt *Fe3+ (4)18
Fe2+ (8)5
Opx *Fe2+ (6)12
Grt *Fe2+ (8)4
Garnet aggregate with interstitial meltGrtFe2+ (8)550.23
Fe3+ (6)16
Carb *Fe2+ (6)120.14 (in melt, bulk)
Mgt *Fe3+ (4)4
Fe2+ (8)2
Opx *Fe2+ (6)11
CG-036.31300Bulk sampleGrtFe2+ (8)490.17
Fe3+ (6)10
OpxFe2+ (6)41-
CG-046.31400Bulk sampleGrtFe2+ (8)520.24
Fe3+ (6)16
OpxFe2+ (6)26-
CG-056.31500Bulk sampleGrtFe2+ (8)570.24
Fe3+ (6)18
OpxFe2+ (6)26-
A: (Area(Fe3+)/(Area(Fe2+) + Area(Fe3+)) × 100 (error = ±3) or (Area(Fe2+)/(Area(Fe2+) + Area(Fe3+)) × 100 (error = ±3). Number in parenthesis denotes coordination of iron. Grt, garnet, Coh, cohenite, Mws, magnesiowüstite, Mgt, magnetite, Opx, orthopyroxene, Carb, carbonate; *, quenched phase.
Table
Table 6. Average compositions of silicates and oxides in the carbide–oxide–carbonate system (“mixture-type” experiments) at 6.3 GPa, according to microprobe analysis.
Table 6. Average compositions of silicates and oxides in the carbide–oxide–carbonate system (“mixture-type” experiments) at 6.3 GPa, according to microprobe analysis.
Run NT, °CPhaseNAMass Concentrations, wt %
SiO2Al2O3FeOFeO *Fe2O3 *MgOCaOTotal
CG-011100Grt1440 (2)25 (3)17 (3)17 (3)-14 (3)4 (2)99.7
938.5 (5)21.3 (8)30 (3)30 (3)-6 (1)4 (2)100.1
Opx1250.7 (8)-33 (1)33 (1)-14.4 (8)0.7 (3)99.4
Mgt5--91.1 (2)20717.0 (2)-98.1
Fpc6--30.7 (9)31-68.4 (8)-99.1
CG-021200Grt1038.3 (1)18.8 (8)33.9 (1)3136.1 (9)2.5 (9)99.6
Opx1050.9 (6)0.4 (3)33 (1)--14.5 (8)0.6 (2)99.7
Mgt6--91.5 (2)20717.5 (1)-98.0
CG-031300GrtC1237.5 (1)22.5 (5)28.6 (8)2358.9 (6)2.1 (1)99.5
GrtR1639.0 (5)25.8 (4)16 (2)15 (2)~114 (1)4.2 (7)99.5
Opx149.4 (3)-40.4 (5)40-10.2 (5)-99.9
Mgt6--90.8 (2)20717.6 (2)-98.4
CG-041400Grt1538.6 (4)21.1 (6)28.7 (5)2279.4 (2)1.7 (4)99.5
Opx749.2 (3)-41.0 (7)41-9.2 (6)-99.5
CG-051500Grt1539.3 (4)21.1 (3)28 (1)22710.0 (6)1.7 (4)99.9
Opx1250 (1)0.4 (3)35.4 (7)--5.6 (5)7.5 (10)99.5
Data were taken from the polished samples, coated with carbon. Grt, garnet; Opx, orthopyroxene; Mgt, magnetite; Fpc, ferropericlase; C, center; R, rim; NA, number of electron probe analyses used to obtain the average compositions. The values in parentheses are one sigma errors of the means based on replicate electron microprobe analyses reported as least units cited. *, calculated according to Mössbauer spectroscopy data.

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Bataleva, Y.; Palyanov, Y.; Borzdov, Y.; Novoselov, I.; Bayukov, O. Graphite and Diamond Formation in the Carbide–Oxide–Carbonate Interactions (Experimental Modeling under Mantle P,T-Conditions). Minerals 2018, 8, 522. https://doi.org/10.3390/min8110522

AMA Style

Bataleva Y, Palyanov Y, Borzdov Y, Novoselov I, Bayukov O. Graphite and Diamond Formation in the Carbide–Oxide–Carbonate Interactions (Experimental Modeling under Mantle P,T-Conditions). Minerals. 2018; 8(11):522. https://doi.org/10.3390/min8110522

Chicago/Turabian Style

Bataleva, Yuliya, Yuri Palyanov, Yuri Borzdov, Ivan Novoselov, and Oleg Bayukov. 2018. "Graphite and Diamond Formation in the Carbide–Oxide–Carbonate Interactions (Experimental Modeling under Mantle P,T-Conditions)" Minerals 8, no. 11: 522. https://doi.org/10.3390/min8110522

APA Style

Bataleva, Y., Palyanov, Y., Borzdov, Y., Novoselov, I., & Bayukov, O. (2018). Graphite and Diamond Formation in the Carbide–Oxide–Carbonate Interactions (Experimental Modeling under Mantle P,T-Conditions). Minerals, 8(11), 522. https://doi.org/10.3390/min8110522

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