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Article

Dynamic Metasomatism Experiments Investigating the Interaction between Migrating Potassic Melt and Garnet Peridotite

by
Stephen F. Foley
* and
Maik Pertermann
Department of Earth and Environmental Sciences, Macquarie University, North Ryde, NSW 2109, Australia
*
Author to whom correspondence should be addressed.
Geosciences 2021, 11(10), 432; https://doi.org/10.3390/geosciences11100432
Submission received: 21 September 2021 / Revised: 12 October 2021 / Accepted: 15 October 2021 / Published: 18 October 2021
(This article belongs to the Section Geochemistry)
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Abstract

:
Dynamic metasomatism experiments were performed by reacting a lamproite melt with garnet peridotite by drawing melt through the peridotite into a vitreous carbon melt trap, ensuring the flow of melt through the peridotite and facilitating analysis of the melt. Pressure (2–3 GPa) and temperature (1050–1125 °C) conditions were chosen where the lamproite was molten but the peridotite was not. Phlogopite was formed and garnet and orthopyroxene reacted out, resulting in phlogopite wehrlite (2 GPa) and phlogopite harzburgite (3 GPa). Phlogopites in the peridotite have higher Mg/(Mg + Fe) and Cr2O3 and lower TiO2 than in the lamproite due to buffering by peridotite minerals, with Cr2O3 from the elimination of garnet. Compositional trends in phlogopites in the peridotite are similar to those in natural garnet peridotite xenoliths in kimberlites. Changes in melt composition resulting from the reaction show decreased TiO2 and increased Cr2O3 and Mg/(Mg + Fe). The loss of phlogopite components during migration through the peridotite results in low K2O/Na2O and K/Al in melts, indicating that chemical characteristics of lamproites are lost through reaction with peridotite so that emerging melts would be less extreme in composition. This indicates that lamproites are unlikely to be derived from a source rich in peridotite, and more likely originate in a source dominated by phlogopite-rich hydrous pyroxenites. Phlogopites from an experiment in which lamproite and peridotite were intimately mixed before the experiment did not produce the same phlogopite compositions, showing that care must be taken in the design of reaction experiments.

1. Introduction

The xenolith record from the cratonic mantle lithosphere shows that much of the lower lithosphere was originally strongly depleted in melt components and subsequently re-enriched, a process that was titled stealth metasomatism [1]. This re-enrichment may re-introduce clinopyroxene and garnet into harzburgites [2,3] or may lead to the crystallization of hydrous minerals including mica and amphiboles [4,5]. These are Mg-rich where they occur in peridotites because they are buffered by the Mg# (100Mg/(Mg + Fe)) of the modally dominant olivine and pyroxenes, but may have more Fe-rich compositions where they are deposited as discrete rock types in channels from fractionating, flowing melts.
Although the products of reactions between metasomatic agents and peridotites are well documented from a plethora of xenoliths, the nature of the metasomatic agent remains contentious because most reactions have gone to completion, or the melts or fluids have moved on. Initial debates about whether fluids or melts were involved in these reactions have settled in favour of melts [6,7], but the composition of the melts is not well understood. In many cases, the reaction produces enrichment in Fe and Ti and is generally attributed to melts related to earlier incarnations of the host kimberlite [8,9], which leads to rocks of the PIC (phlogopite-ilmenite-clinopyroxene) group. In contrast, the abundance of phlogopite in MARID-type (mica-amphibole-rutile-ilmenite-diopside) enrichments leads to the conclusion that the melts were rich in potassium, with most favouring a lamproitic or orangeitic composition [10,11].
The origin of orangeites (formerly Group II kimberlites; [12]) is the subject of renewed debate as these are more potassic than kimberlites, occur in the same craton as most MARID xenoliths, and are suggested by some to be the carbonate-rich equivalent of lamproites [13]. Interactions of more than one type of potassic melt with peridotite may thus be relevant to the formation of hydrous minerals during re-enrichment.
We refer to the process of re-enrichment by reaction with passing melts as dynamic metasomatism, deliberately choosing the qualifier “dynamic” to emphasize that reactions are not static, but involve the flow of melt through the peridotite, with reaction products incorporating chemical components from both the melt and the host rock. In the case of crystallization in channels, dynamic metasomatism also occurs at the initial margins of veins and dykes, as seen, for example, in Ligurian peridotites [14], whereas later crystallization in the centre of veins may simply correspond to igneous fractionation from a moving melt. The process of dynamic metasomatism has almost universally been studied in natural rocks but has received little attention in high-pressure experiments. Odling [15,16] tested reactions between depleted peridotites and fluids and kimberlitic melts, finding mica and amphibole to be products of reaction with kimberlitic melt [16], whereas abundant alkali amphibole and less phlogopite were produced from reactions with a water-rich COH fluid [15]. These experiments used long capsules and a temperature gradient to drive melt migration. Here, we investigate reactions between peridotite and a lamproitic melt—another commonly invoked metasomatic agent—using a melt trap to draw the melt through the peridotite.
The purpose of this investigation is twofold: (i) to characterize the mineralogical products of the reaction between peridotite and a passing potassic melt, and (ii) to assess the modification of the composition of the migrating melt. Here, we use a leucite lamproite as the migrating melt, which may be more common at shallower levels of the continental lithosphere, and may represent the more evolved products of fractionation of olivine lamproites [17].

2. Materials and Methods

2.1. Experimental Design

To ensure reaction between peridotite and a migrating melt, the experiments were designed to contain an alkaline melt (lamproite) at one end of the capsule, peridotite in the middle, and a vitreous carbon melt trap at the other end of the capsule (Figure 1). The primary function of the melt trap is to facilitate movement of melt through the peridotite, which works due to the pore space within the trap initially offering a lower pressure than in the rest of the capsule. Experiments were conducted with the melt trap at the top of the capsule so that melt movement had to occur against gravity. The ratio of vitreous carbon trap to silicate charge was kept low (0.035–0.046) to allow complete filling of the pore space with melt and subsequent equilibration of the melt: this allows equilibration of the melt within 24 h [18], circumventing issues with the attainment of equilibrium [19,20,21], which only occurs when the pore space in the trap is too large [18]. All experiments in this study were run for 24 h or more. A similar constellation of three layers was used for basalt/peridotite experiments, but with a larger melt trap that was not intended to collect melts for analysis [22,23].
Graphite-lined Pt capsules were used to limit the loss of iron during the experiments: the Pt capsules had an inner diameter of 3.6 mm and the graphite liners had an inner diameter of 1.9–2.0 mm. Water was added to the charge, then the capsule was welded shut whilst cooled below 0 °C in an iced brass block. After welding, capsules were checked for leaks by heating at 110 °C for >30 min and re-weighing. The amount of water was ≈10 wt% for the lamproite and ≈3 wt% for the whole charge; this amount of water ensures that the lamproite is molten under the P-T conditions of the experiments [24]. One experiment (G141, 3 GPa, 1100 °C) was run with the peridotite and lamproite intimately mixed before the experiment to compare results with those of the layered configuration. This should produce similar mineral assemblages to the reaction zone, but in which minerals are easier to identify [25,26].
Experiments were conducted at 2 and 3 GPa in standard piston-cylinder apparatuses at the University of Göttingen as part of the Diploma thesis of M. Pertermann [27]. Boron nitride was used for sample sleeves and NaCl as pressure medium apart from the 1250 °C experiment at 3 GPa, for which BaCO3 was used as the melting point of NaCl was exceeded. Temperature was controlled to within ±1 °C by an 818P Eurotherm controller and Pt/Pt90Rh10 thermocouples and run durations varied between 24 and 132 h. After experiments, capsules were cut lengthwise with a WS22 wire saw and the resulting halves and thin sample discs were mounted in epoxy and polished with diamond paste. Details of experiments are listed in Table 1.

2.2. Starting Materials and Analytical Methods

The alkaline melt is a natural lamproite from Gaussberg, eastern Antarctica, chosen because of its suitable composition and because phase relations at these pressures are known from previous studies [24,28]. The peridotite is a natural garnet lherzolite from Jagersfontein, South Africa, which has was also used previously in experiments, commonly as mineral separates. Compositions of the rocks and the constituent minerals of the peridotite are given in Table 2.
The melt trap consisted of 60–80 µm grains of vitreous carbon (Deutsche Carbone AG, Frankfurt) and was used in preference to diamond aggregates for the melt trap since it simplifies polishing of experimental charges and quenched melts. Trace element analysis shows that the only major contaminant in the vitreous carbon is Zr (1340 ppm) with minimal amounts of Ba (18 ppm) and Rb (4.7 ppm).
The lamproite is a glassy pillow rim sample (4891-3) of the Gaussberg lamproite with a composition close to the range given by Sheraton and Cundari ([29] Table 2). The sample was crushed and ground under acetone in an agate mortar; the resulting grain size was mostly 20–30 µm with a maximum of 50 µm. Previous experiments [24] show that at 2 GPa and 1125 °C the lamproite should be completely molten, whilst at 2 GPa and 1050 °C and at 3 GPa and 1100 °C phlogopite coexists with a large amount of melt, ensuring adequate reaction with the peridotite.
The modal mineral composition of the J4 garnet lherzolite was estimated by XRD analysis to be 65% olivine, 15% orthopyroxene, 10% clinopyroxene and 15% garnet. The resulting calculated bulk composition of the rock and the mineral analyses are given in Table 2.
Electron microprobe analyses of run products were obtained at Heidelberg (Cameca SX-51, Cameca, Paris, France), Utrecht (JEOL JXA 8600 Superprobe, JEOL, Tokyo, Japan) and Macquarie (Cameca SX100, Cameca, Paris, France) Universities using standard analytical procedures (15 kV, 10–20 nA) calibrated on a variety of natural and synthetic mineral standards. For phlogopites and quenched melts, the beam was defocused to 10–15 µm whereas for all other minerals a focused beam (1–2 µm) was used.

3. Results

3.1. Phases Present in Experimental Products

Experiments were conducted at 2 and 3 GPa, two temperatures at each pressure and a time series of three experiments was conducted at 3 GPa and 1100 °C with durations of 24, 58 and 132 h. A summary of experimental run conditions, ratios of starting materials and experimental products is given in Table 1. Experiment G141 with the peridotite and lamproite intimately mixed produced olivine, Cpx, Phl and melt, the same assemblage as in the experiments with layered run charges, but mineral compositions differed (see below).
Inspection of the polished sections showed that the layering of the run charges remained essentially intact and the dimensions of the original lamproite and peridotite remained constant. Abundant quench phlogopite formed in the lamproite sections, where phlogopite also occurred as idiomorphic primary platelets up to 50 × 50 µm. No melts or continuous pathways could be identified in the peridotite section, but phlogopite occurred as interstitial patches up to 100 µm in length and 50 µm wide. Minerals adjacent to the phlogopites in the peridotite section were rounded and/or embayed, indicating reaction with a melt and deposition of the phlogopite in the interstices (Figure 2). All minerals in the peridotite showed thin rims with modified compositions due to reaction with passing melt: these rims were too thin for microprobe analysis (Figure 2).
In both experiments at 2 GPa, run products contained olivine, Cpx, Phl and melt, but no Opx or garnet could be found, whereas at 3 GPa and 1100 °C olivine, Opx, minor Cpx, Phl and melt formed. The time-series experiments showed the same run products regardless of duration.

3.2. Mineral Compositions

3.2.1. Phlogopite

Phlogopites were analysed in the remains of the lamproite section, in the peridotite close to the lamproite section and in the peridotite close to the melt trap in order to establish any systematic compositional variation across the profile of the peridotite section. Two compositional groups could be identified; one in the lamproite section with high TiO2 and low Cr2O3 (Table 3), and the other in the peridotite section with lower TiO2 and higher Cr2O3. No systematic variation could be recognized for phlogopites in the peridotite section (Figure 3) and so these are summarized in unison in Table 3. Phlogopites in the time series comparison (G138, 24 h; G131, 58 h; G137, 132 h) showed only small compositional differences with no consistent trend: phlogopite from the shortest and longest time-series runs were most similar, whereas those in the experiment with intermediate duration had a higher Al2O3 and lower Cr2O3, which may be attributable to the higher proportion of lamproite in the capsule imparting stronger lamproite characteristics.
In the 2 GPa experiments, phlogopites in the higher temperature experiment (1125 °C vs. 1050 °C) have slightly higher TiO2 (7.0 vs. 5.1 wt%) and lower Cr2O3 (0.07 vs. 0.17 wt%), emphasizing the polarization between mineral compositions in the lamproite and peridotite sections. Phlogopite did not occur at 2 GPa and 1125 °C in the liquidus experiments of [24], presumably due to a higher content of fluid components in those experiments. Phlogopites in the peridotite sections are distinct from those in the lamproite section, with higher Cr2O3 (≈1.7 vs. ≤0.2 wt%), Al2O3 (15–16 vs. <12 wt%) and Na2O (0.60–0.74 vs. 0.12–0.16 wt%) and lower TiO2 (1.0–1.3 vs. >5 wt%; Figure 3). The Mg# is buffered by the peridotite minerals at 90.4–91.8, in contrast to those in the lamproite section, which are more variable (Figure 3) and characteristic of those in magmatic lamproites [17]. The distinction between phlogopites in the peridotite reaction zone and the lamproite section for experiment G131 at 3 GPa, 1100 °C (Figure 4) is not as sharp as in Figure 3. This is most likely due to the higher proportion of lamproite relative to peridotite (i.e., melt/rock ratio is higher) in the experiment (Table 1), as the higher temperature did not have this effect in other experiments.

3.2.2. Other Silicate Minerals

All silicate minerals display compositional changes compared to the mineral composition of the starting materials: the values listed in Table 4 are averages of points analysed as line scans as for the phlogopites in Figure 3, with the low standard deviations indicating relatively uniform compositions. Clinopyroxenes are diopsides with Mg# 88–91, Cr2O3 between 0.85 and 1.37 wt%, Al2O3 between 2.6 and 3.5 wt%, and Na2O 0.6 to 1.6 wt%. Orthopyroxenes have Mg# 88.6–90.2, Cr2O3 between 0.24 and 0.59 wt%, Al2O3 between 1.2 and 2.0 wt%, and Na2O 0.17–0.19 wt%.
In the shortest run of the time series, Opx has higher Al2O3 and Cr2O3 contents (1.6 vs. 1.3 wt% and 0.5 vs. 0.2 wt%) and lower FeO contents (7.2 vs. 7.7 wt%) near the carbon trap, which may reflect less reaction with the percolating melt. Olivine displays uniform composition throughout the peridotite layer, with Mg# ranging from 88.5 to 91.1.

3.3. Melt Compositions

The quenched melts were analysed in the residual lamproite melt and in the melt traps (Table 5); only in one high-temperature experiment was interstitial melt found in the peridotite section. However, the analysis of the melts in the residual lamproite was complicated by the occurrence of abundant quench crystals, mainly phlogopite. The discrepancy in the total from 100% is principally due to H2O, but minor CO2 may have been generated from the graphite capsule; the concentration of water was not determined independently.
Melt compositions in the extraction traps were not of uniform composition, but displayed a compositional range, varying with each melt pool analysed, possibly reflecting different extents of melt mixing along paths with different degrees of interaction rather than inhomogeneity of analyses. Glass in the melt trap is quench-free, eliminating the possibility that the variation is due to quenching modification of the melt composition. The individual analyses span a wide range of SiO2, and the behaviour of Al2O3 and K2O as a function of the SiO2 content for experiment G128 (2 GPa, 1125 °C) is shown in Figure 5; this behaviour is representative for all other experiments. The major elements seem to be largely unaffected by the different time scales of the experiments, except for Ti, Na, K and Ba. All these elements are more enriched in the extraction trap of the longer duration experiment, indicating either slower diffusion processes for them, or they reacted more during migration through the peridotite. This is especially the case for Ba, for which the concentration is nearly twice as high in the longer duration experiment than in the shorter experiment.
In most experiments the melts in the extraction traps have a significantly higher Mg# than the residual lamproite melt (averages 74.6 vs. 66.4), lower K2O/Na2O (averages 2.7 vs. 6.3) and also lower BaO, K2O/Na2O and K/Al ratios (averages 0.50 vs. 0.80). This reflects the uptake of K2O and Ba in phlogopites that grew in the peridotite and the buffering of the Mg# by the peridotite minerals because the volume of the peridotite greatly exceeds that of the reacting melt. The compositions of melts in the residue of the lamproite section are much less variable than melts in the carbon traps, particularly in terms of Mg# (Figure 6b). Examples of compositional parameters are shown in Figure 6.

4. Discussion

4.1. Reaction Experiment Design

Reaction experiments have been used increasingly over the last ten years to study hybridization reactions between melts and rocks they pass through, mostly peridotites. One of two methods are usually used: either (i) two rocks (or powdered rocks) are placed in capsules as separate blocks or cylinders with a sharp boundary between them similar to the layered configuration used here (“reaction experiments” using the terminology of Wang and Foley [30]; or (ii) the two powdered rocks are intimately mixed in different proportions (“mixed experiments” in {30]). Layered experiments have been used to assess hybridization by a variety of melts from clastic sedimentary or carbonate-rich through basalt to granite [22,23,31,32,33,34,35,36,37]. A similar array of melts has been studied with the mixing of the two reactant rocks [38,39,40,41], but few studies have used both methods to compare them. Of these, the experiments of [30] compared mineral compositions using the two methods, concluding that they were the same and that the homogenized mixtures were, therefore, useful to study minerals in thin reaction layers in layered experiments where the formation of new minerals had created a barrier to melt flow.
Experiment G141 was conducted with a homogenized mixture of lamproite and garnet lherzolite in the same ratio as the layered experiment (Table 1) in order to compare results to those from experiments with the layered run charges. This experiment was also run at the same pressure and temperature as the time series experiments. In Figure 7, the compositions of the phlogopites from this experiment are compared to those in layered experiment G131, which had the most similar experiment duration (58 vs. 72 h). Figure 7 shows that the phlogopites from the experiment with the homogenised starting materials are distinct from those in both the peridotite layer and the lamproite residue from Experiment G131: they have low TiO2 resembling those in the peridotite layer, but high SiO2 characteristic of those in the lamproite residue. The difference to earlier experimental studies in which similar mineral compositions were found in layered and mixed experiments lies in the inclusion of the carbon melt trap, which has effectively removed the melt components from the reacting system, creating a “flow-through” scenario: the phlogopites in the peridotite layer mimick the reaction products from a flowing melt that is no longer present in the system.
The use of melt traps has had a chequered history since its introduction to separate fluids and melts from rock matrices to optimize chemical analysis [20,42,43]. Tests have shown that the melt compositions in traps may correspond to melts in equilibrium at lower pressures than the nominal experimental pressure due to the initial pore space in the traps [19], but that this can be circumvented by ensuring that the volume of the pore space in the trap is exceeded by the volume of melt, facilitating continued chemical communication and thus equilibrium [44]. However, the extraction traps in our experiments were included to serve as a suction pump to assure sufficient reaction of the lamproite melt during complete passage through the peridotite section, rather than to assess equilibrium melt compositions. Nevertheless, the melt compositions in the melt traps may approach equilibrium, as the volume of the pore space is estimated to be only 1–1.5% of the original volume of lamproite melt in the whole experiment. The melt compositions in the melt traps are modified from the original lamproite by reaction with the peridotite and may include components of the peridotite that were dissolved, rather than melted out, at temperatures below the peridotite solidus.

4.2. Melt Compositions before and after Reaction with Peridotite

The time-series experiments G138 (24 h), G131 (58 h) and G137 (132 h) had similar proportions of lamproite, peridotite and carbon traps in the starting materials and the melt compositions in the traps are broadly similar but show some significant inhomogeneities between melt pools. Baker and Stolper [20] noted that the SiO2 content of melt in the extraction trap decreased in experiments with long durations, whereas the Al2O3 content increased. This could be the result of initial high-SiO2 melt entering the trap first, followed by equilibration with a later melt from the rest of the run charge. This may indicate that the equilibrium concentrations of mobile elements such as alkalis or Ti should lie at the high end of the compositional variations displayed by the individual melt trap analyses (Figure 6). Ti, Na, K and Ba contents in melts in the melt trap increase with experimental duration, probably due to more extensive reaction during migration through the peridotite. In the shortest run of the time series, Opx has higher Al2O3 and Cr2O3 and lower FeO contents close to the carbon trap, which may be caused by the reaction with the percolating melt not having progressed as far as in the longer duration experiments.
The main differences in melt compositions at either side of the peridotite section are that the melt in the melt traps, which is modified by reaction with peridotite, has higher Mg#, Al2O3, Cr2O3 and Na2O but lower K2O and BaO. These reacted melts have less variable compositions than residual melts in the former lamproite section: this may be a function of quench modification in the larger areas of the latter, whereas melts quench well to glass in the melt trap. The higher and consistent Mg# is a result of buffering by the peridotite minerals, which are volumetrically dominant in the experiments. Peridotite minerals with Mg# ≈90 seek to impose an equilibrium Mg# of 70–73 on coexisting melts: the Mg# of the lamproite flowing in is slightly lower than this and is reduced further by the formation of high-Mg# phlogopite. The peridotite, therefore, removes Fe from the melt, forming the thin Fe-rich rims seen in BSE images (Figure 2) and the resultant melt in the melt trap has a higher and consistent Mg# (Figure 6b). If the melt/rock ratio were lower (corresponding to lower temperatures close to the lamproite solidus), this process would induce freezing of the melt and thus stoppage of the metasomatic process [44]. The lower contents of K2O and BaO in the melt are due to the formation of metasomatic phlogopite, whereas the increase in Al2O3 and Cr2O3 is caused by the removal of garnet through reaction with the melt.
No phosphorus-bearing mineral was found in the experiments, but the concentration of ca. 0.6 wt% in melts in the extraction traps indicates dilution by a factor of two compared to the original leucite lamproite. This degree of dilution of phosphorus may mean that the contribution of peridotite to the melt is relatively high.

4.3. Applications to Mantle Metasomatism

4.3.1. Composition of Phlogopites Formed by Melt/Rock Reaction

The main aim of this study was to assess whether the phlogopites in cratonic garnet peridotites were formed by reaction with a passing potassic silicate melt. The phlogopites in the lamproite section reflect magmatic crystallization from the lamproite melt, whereas the phlogopites occurring interstitially in the peridotite are the product of a reaction between melt and peridotite as the melt moves through the garnet peridotite and into the extraction trap. This is formed by the reaction of lamproitic melt primarily with garnet: the garnet reacts with the alkali- and water-rich melt and the high Cr2O3 content of the garnet (Table 2) is incorporated into the newly formed phlogopite. This conclusion is backed up by the observation that the interstitial phlogopite is xenomorphic (Figure 2) and has a much higher Cr2O3 content than the original lamproite (0.03 wt%; Table 2). At 2 GPa, the reaction also consumes Opx, whereas at 3 GPa Opx survives, indicating increased stability of Opx towards higher pressures, as is typical in peridotites [45].
Phlogopites in cratonic peridotites have been studied for several decades. Carswell [46] defined primary-textured micas as being single large crystals that have regular boundaries with silicate and oxide minerals, whereas secondary-textured micas usually form reaction rims around other silicate minerals, particularly orthopyroxene and garnet, and often occur as veinlets in the peridotite. Delaney et al. [4] showed that the compositions of these phlogopites show lower TiO2 and higher Cr2O3 contents in later minerals, as judged by textures, and interpreted the high Cr2O3 micas to be the products of metasomatism by K- and H2O-rich fluids in which the garnet reacts with the fluid (or melt). Later studies of other localities confirmed the higher Cr2O3 contents but found that the behaviour of TiO2 was inconsistent, often also increasing in late micas (Figure 8; [47,48,49,50]). Micas in kelyphitic rims around garnets have particularly high Cr2O3, extending up to 3 wt% in examples from ilmenite-rutile-phlogopite-sulphide series xenoliths despite lower concentrations of <0.75 wt% in primary-textured micas [51].
Erlank et al. [5] describe the metasomatic progression from garnet peridotites (GP), through garnet phlogopite peridotites (GPP) and phlogopite peridotites (PP) to phlogopite K-richterite peridotites (PKP), resulting from increasing metasomatic alteration by alkali-, volatile- and incompatible element-rich fluids, which were re-interpreted as melts by [6]. The experimental results presented here are the equivalent of phlogopite peridotite, where metasomatic alteration has removed the garnet completely.
The phlogopites occurring interstitially in the current experiments have similar trends of decreasing TiO2 and increasing Cr2O3 relative to phlogopites in the lamproite section and plot towards the upper end of Cr2O3 contents of secondary-textured micas in the natural peridotites (Figure 8). They may be equivalent to those in kelyphitic rims, but garnet was completely replaced by phlogopites under these experimental conditions, as a result of the relatively high temperature and low pressure [54]. Rapid breakdown of garnet is facilitated by the presence of the melt, which has been shown to react 100 µm in 2 days at 1050 °C [55], a distance exceeding the grain size of the garnets in our starting materials.

4.3.2. Reactivity of Different Alkaline Melts with Peridotite

There are a range of melts that may be involved in the metasomatic process when they infiltrate peridotites, and these melts should produce different mineralogical assemblages. Current summaries of metasomatic types in peridotites of the Kaapvaal Craton in South Africa recognize principally two types of phlogopite-bearing assemblages, known as MARID (mica-amphibole-rutile-ilmenite-diopside) and PIC (phlogopite-ilmenite-clinoproxene) [9,53], although other minor types (e.g., IRPS; [51]) may have been neglected. Candidates for melt types for cratonic processes include kimberlite, orangeite (formerly Group II kimberlite), lamproite, as well as carbonate-rich melts such as carbonatites and carbonated silicate melts with <30 wt% SiO2 that are recognized as potential metasomatic agents from high-pressure experiments more than from natural rocks [56,57].
The formation of PIC and MARID xenolith suites has been assigned to interaction with kimberlites and orangeite melts, respectively [9]. However, orangeites and lamproites may be related, although the exact relationship is currently uncertain. Some refer to them as carbonate-rich lamproites [13,58], a Kaapvaal equivalent of carbonate-poor lamproites elsewhere that have been shown to originate in reduced source regions where carbonate would not be stable [24,59]. This mode of origin also occurs in eastern Zambia [60].
Few studies that produced phlogopites from the reaction between melts and peridotite are available for comparison with our experimental results. Odling [16] reacted kimberlite melts (25 wt% SiO2, 5.9 wt% CO2, 6.5 wt% H2O) with harzburgite in experiments with a temperature gradient, finding interstitial phlogopite and glass coexisting with olivine+Cpx+Sp at high temperatures, which transitioned to Ol+Cpx+Phl and were joined by orthopyroxene and finally K-richterite at a lower temperature. Shatskiy et al. [53] studied the interaction of a synthetic potassic carbonatite (0% SiO2, 35–44 wt% CO2, 8.1–11.6 wt% H2O, 0–4.9 wt% Na2O) mixed at different proportions with peridotite, finding K-richterite in addition to phlogopite and carbonates, but only if Na2O-bearing carbonatite melts were used. Other experiments using dry carbonatite or carbonated silicate melts and peridotite did not produce phlogopite [37].
Shatskiy et al. [53] confirmed the observation that Cr2O3 in phlogopite is highest where garnet was consumed, implying a similar interpretation for the natural phlogopites of [4] but involving a carbonatite melt in contrast to our CO2-free lamproite melt. K-richterite was found as a product of reaction with kimberlite [16] and carbonatite [53] but not in our experiments with lamproitic melt, which is noteworthy since K-richterite occurs in lamproites but not in kimberlites or carbonatites. The phlogopites in all three studies of reaction experiments are enriched in Cr2O3 (Figure 8; Odling’s single analysis had 1.51 wt%), whereas there is a small but distinct difference in TiO2. Those in the current experiments have 1.07–1.26 wt % TiO2, presumably due to the high TiO2 in the lamproite, whereas those resulting from reaction with carbonatite have an average of 0.61 wt% and with kimberlite 0.21 wt%. This difference, together with any inclusions of Cr-spinel or especially carbonates, as in the experiments of [53], may prove critical in deciding which melt type drove the metasomatic reactions in natural rocks.

4.3.3. Compositional Evolution of the Reacting Melt

A principal difference between the current experimental design and other experiments on metasomatic reactions is the inclusion of the carbon melt trap at the far end of the capsules in which melt compositions were analyzed. Although intended primarily to assist the flow of the melt through the peridotite, this melt trap collected the evolved melt. Initial melts entering the trap may have been artificially high in SiO2, corresponding to a lower effective pressure because of the initial pore space in the trap [19]. After it was filled, the time series experiments how that the melt composition changed to approach the correct composition, with Ti, Na, K and Ba needing longer to reach equilibrium because of exchange reactions with the peridotite. Melts in the trap were inhomogeneous, varying between different pools that had experienced different paths through the peridotite (Figure 5).
The compositions of melts in the trap show increased Mg# and lower BaO contents, K2O/Na2O and K/Al ratios relative to the initial lamproite melt composition (Figure 6) because of the loss of chemical components to phlogopite during melt/rock reaction. The Mg# would remain buffered at high values as long as melt percolates along grain boundaries rather than flowing through coated channels.
The experiments could also be seen to represent an advanced stage of melting of phlogopite and K-richterite-bearing hydrous pyroxenite vein [18], from which the melt infiltrates the peridotite wall-rock and partially dissolves it [61]. At this advanced state of melting when phlogopite remains the only stable phase in the vein assemblage, the experiments confirm predictions [44] that the melt will dissolve mainly garnet and orthopyroxene. The melt in the carbon trap would then represent melt that moves on to higher levels of the lithosphere in the case of percolation along grain boundaries. This shows that the vein/wall-rock reaction is not a matter of simple dissolution of minerals, because phlogopite forms during the reaction, involving the dissolution of olivine. This would deplete the melt in K2O and BaO, which does not correspond to the extreme enrichment in K2O and BaO in lamproites [17]. However, this may be explained by the movement of melt through coated channels initially produced by high melt flow rates: lamproitic melt compositions are consistent with the melting of K-richterite-bearing rocks, which produce a large melt fraction with little rise in temperature above the solidus [18]. Following initial infiltration and reaction with wall rocks, melts with high K2O/Na2O will be channeled in the little-modified form to higher levels. The current experiments indicate that at lower rates of melt infiltration, alkaline melts with lower K2O/Na2O may evolve through melt/rock reactions.

5. Conclusions

Flow-through experiments reproducing the reaction of migrating lamproitic melt and peridotite wall rocks were conducted with a vitreous carbon melt trap at the opposite end of the experimental capsule to the lamproitic melt to assist the migration of the melt. This set-up also allowed chemical analysis of the melt after reaction with the peridotite, which showed increased Mg#, decreased K2O/Na2O and decreased K/Al ratios relative to the unreacted lamproite melt. The melts in the traps show that lamproitic melts lose the chemical characteristics of lamproites through this reaction, indicating that lamproites are unlikely to be derived from a peridotite source, but more likely a source dominated by phlogopite-rich hydrous pyroxenites.
Reactions in the peridotite removed orthopyroxene and garnet and deposited phlogopite by an incongruent reaction of melt with olivine and orthopyroxene. The phlogopites formed mimic the compositions of those seen in peridotite xenoliths, with increased Cr2O3 derived from the garnets.

Author Contributions

Conceptualisation, S.F.F.; formal analysis, S.F.F. and M.P.; investigation, M.P. and S.F.F.; data curation, S.F.F.; writing—original draft preparation, S.F.F. and M.P.; writing—review and editing, S.F.F.; project administration, S.F.F.; funding acquisition, S.F.F. All authors have read and agreed to the published version of the manuscript.

Funding

This research was funded by the Deutsche Forschungsgemeinschaft Grant Fo 181-3 and Australian Research Council Grant FL180100134 to S. Foley.

Institutional Review Board Statement

Not applicable.

Informed Consent Statement

Not applicable.

Data Availability Statement

Not applicable.

Acknowledgments

This paper is based on the Diploma (M.Sc.) thesis of M.P. [27]. John Sheraton and Gerhard Brey supplied the lamproite and peridotite samples used in the experiments. We thank Michael Förster, Chunfei Chen and Isra Ezad for their comments on the manuscript.

Conflicts of Interest

The authors declare no conflict of interest.

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Figure 1. Capsule design for dynamic metasomatism experiments. Lamproite loaded below peridotite as separate layers so that melt must flow against gravity, drawn through by suction of the vitreous carbon melt trap, present at 3.5–4.5% of the volume of the silicate charge. Inner graphite capsule prevents iron loss to outer sealed Pt capsule.
Figure 1. Capsule design for dynamic metasomatism experiments. Lamproite loaded below peridotite as separate layers so that melt must flow against gravity, drawn through by suction of the vitreous carbon melt trap, present at 3.5–4.5% of the volume of the silicate charge. Inner graphite capsule prevents iron loss to outer sealed Pt capsule.
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Figure 2. Back-scattered electron image of the peridotite section after Experiment G128 at 2 GPa and 1125 °C (Ol + Cpx + Phl). Compositionally homogeneous xenomorphic phlogopite crystallizes interstitially between olivine and clinopyroxene. Olivine shows rounded and embayed grains indicating reaction (Melt + olivine => Phl) and light, Fe-rich rims due to approaching equilibrium of Mg# with the infiltrating melt.
Figure 2. Back-scattered electron image of the peridotite section after Experiment G128 at 2 GPa and 1125 °C (Ol + Cpx + Phl). Compositionally homogeneous xenomorphic phlogopite crystallizes interstitially between olivine and clinopyroxene. Olivine shows rounded and embayed grains indicating reaction (Melt + olivine => Phl) and light, Fe-rich rims due to approaching equilibrium of Mg# with the infiltrating melt.
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Figure 3. Traverse of phlogopite compositions in lamproite and peridotite sections of Experiment G132 (2 GPa, 1050 °C), plotted at approximately equal intervals from bottom to top of capsule (left to right). Peridotite section indicated by grey background. New phlogopites grown in the peridotite have higher Mg# and Cr2O3 as well as lower TiO2 than those crystallizing as a liquidus phase in the lamproite and show consistent compositions throughout the peridotite section.
Figure 3. Traverse of phlogopite compositions in lamproite and peridotite sections of Experiment G132 (2 GPa, 1050 °C), plotted at approximately equal intervals from bottom to top of capsule (left to right). Peridotite section indicated by grey background. New phlogopites grown in the peridotite have higher Mg# and Cr2O3 as well as lower TiO2 than those crystallizing as a liquidus phase in the lamproite and show consistent compositions throughout the peridotite section.
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Figure 4. Traverse of phlogopite compositions in lamproite and peridotite sections of Experiment G131 (3 GPa, 1100 °C), plotted from bottom to top of capsule (left to right). Trends are similar to those in Figure 3 but the lamproite characteristics are beginning to dominate the Mg# at the start of the peridotite section, probably due to the higher proportion of lamproite in this experiment.
Figure 4. Traverse of phlogopite compositions in lamproite and peridotite sections of Experiment G131 (3 GPa, 1100 °C), plotted from bottom to top of capsule (left to right). Trends are similar to those in Figure 3 but the lamproite characteristics are beginning to dominate the Mg# at the start of the peridotite section, probably due to the higher proportion of lamproite in this experiment.
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Figure 5. Melt compositions in the melt traps from Experiment G128 (2 GPa, 1125 °C). SiO2, Al2O3 and K2O contents show variation, probably due to different path lengths through the peridotite.
Figure 5. Melt compositions in the melt traps from Experiment G128 (2 GPa, 1125 °C). SiO2, Al2O3 and K2O contents show variation, probably due to different path lengths through the peridotite.
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Figure 6. Comparison of melt compositions in melt traps (squares) with melts in the residual lamproite section (diamonds): each symbol is the average for one experiment and colours indicate same experiments (see key). Changes across the peridotite reaction column show similar trends to phlogopites due to buffering of the melt Mg# by the peridotite (middle) and the uptake of TiO2 but release of Cr2O3 in the metasomatic reaction (a). The growth of phlogopite in the peridotite also results in lower BaO and near-constant Mg# (b), and in lower K2O, hence lower K/Al and K2O/Na2O (c).
Figure 6. Comparison of melt compositions in melt traps (squares) with melts in the residual lamproite section (diamonds): each symbol is the average for one experiment and colours indicate same experiments (see key). Changes across the peridotite reaction column show similar trends to phlogopites due to buffering of the melt Mg# by the peridotite (middle) and the uptake of TiO2 but release of Cr2O3 in the metasomatic reaction (a). The growth of phlogopite in the peridotite also results in lower BaO and near-constant Mg# (b), and in lower K2O, hence lower K/Al and K2O/Na2O (c).
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Figure 7. Comparison of phlogopite compositions in layered experiment G131 (green squares) to those in homogenized experiment G141 (both experiments were conducted at 3 GPa, 1100 °C). This shows that minerals from experiments in which lamproite and peridotite are mixed before the experiment (G141) are not equivalent to reaction products in the peridotite section of layered runs.
Figure 7. Comparison of phlogopite compositions in layered experiment G131 (green squares) to those in homogenized experiment G141 (both experiments were conducted at 3 GPa, 1100 °C). This shows that minerals from experiments in which lamproite and peridotite are mixed before the experiment (G141) are not equivalent to reaction products in the peridotite section of layered runs.
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Figure 8. Comparison of phlogopites in peridotite (green squares) and lamproite (yellow squares) sections of the current experiments with phlogopites in natural mantle rocks. Data sources: Metasomatised Kaapvaal peridotites [4,50]; Lashaine peridotites [47]; Jagersfontein peridotites (1 = primary, 2 = secondary; [50]); IRPS suite [51]; Bultfontein peridotite close to vein, and polymict breccias [48]; MARID and PIC xenoliths [52]; experiments reacting carbonate-silicate melt with peridotite (“cbt reaction expts”; [53]).
Figure 8. Comparison of phlogopites in peridotite (green squares) and lamproite (yellow squares) sections of the current experiments with phlogopites in natural mantle rocks. Data sources: Metasomatised Kaapvaal peridotites [4,50]; Lashaine peridotites [47]; Jagersfontein peridotites (1 = primary, 2 = secondary; [50]); IRPS suite [51]; Bultfontein peridotite close to vein, and polymict breccias [48]; MARID and PIC xenoliths [52]; experiments reacting carbonate-silicate melt with peridotite (“cbt reaction expts”; [53]).
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Table
Table 1. Experimental details for dynamic metasomatism experiments.
Table 1. Experimental details for dynamic metasomatism experiments.
Experiment LabelPressure GPaTemperature °CDuration
Hours		Ratio
Peridotite/
Lamproite a		Ratio Trap/
Silicate Charge b		Phases Present c
G13221050723.290.043OL + CPX + PHL + L
G12821125722.520.039OL + CPX + PHL + L
G13831100243.150.046OL + CPX + OPX + PHL + L
G13131100582.570.043OL + CPX + OPX + PHL + L
G137311001323.180.044OL + CPX + OPX + PHL + L
G13931250243.190.041OL + (SP) + L
G141 *31100723.190.036OL + (CPX) + OPX + PHL + L
a = weight ratio peridotite/lamproite in capsule; b = weight ratio of carbon extraction trap to total silicate mix; c = phases present in peridotite section after experiment; * = peridotite and lamproite intimately mixed before experiment.
Table
Table 2. Compositions of starting materials: lamproite and peridotite and its constituent minerals.
Table 2. Compositions of starting materials: lamproite and peridotite and its constituent minerals.
Starting Material 65%15%10%10%Average
GaussbergJ4J4J4J4J4Garnet
LamproitePeridotiteOlivineOpxCpxGrtLherzolite
SiO251.144.8840.857.5855.1442.145.98
TiO23.30.180.030.230.490.780.09
Al2O310.282.560.040.982.8920.931.57
MgO7.0840.8948.9833.9418.1121.5143.46
FeO6.088.569.946.084.057.816.91
CaO4.032.190.071.0215.654.251.16
Na2O1.80.30.030.322.250.110.16
K2O12.460.010.010.010.030.010.12
Cr2O30.030.340.030.210.822.020.32
MnO0.080.130.110.120.130.280.11
NiO0.010.230.36 0.29
BaO0.55
P2O51.37
H2O1.17
Sum99.34100.27100.4100.4999.5699.8100.17
Mg#67.4989.4989.7890.8788.8583.0891.81
Table
Table 3. Phlogopite compositions in dynamic metasomatism experiments.
Table 3. Phlogopite compositions in dynamic metasomatism experiments.
ExptG132 G132 G128 G128
P (GPa)2 2 2 2
T (°C)1050 1050 1125 1125
Duration (h)72 72 72 72
LocationResidual interstitial in Residual interstitial in
melts.d.peridotites.d.melts.d.peridotites.d.
SiO240.290.1239.70.2739.730.2438.720.51
TiO25.140.431.20.086.980.371.260.11
Al2O311.860.114.70.2811.490.2715.990.43
MgO20.120.3623.20.1717.980.2222.40.25
FeO6.190.223.70.147.420.23.680.09
CaO0.030.050.00.020.050.030.030.02
Na2O0.120.020.60.030.160.030.740.04
K2O9.980.119.40.169.810.169.320.09
Cr2O30.170.071.70.210.070.021.670.2
MnO0.050.030.00.020.050.030.050.03
NiO0.080.030.20.040.040.020.140.07
BaO0.290.040.20.060.350.030.220.06
Sum94.32 94.58 94.13 94.22
Mg#85.3 91.8 81.2 91.6
n5 14 5 8
ExptG138 G138 G131 G131
P (GPa)3 3 3 3
T (°C)1100 1100 1100 1100
Duration (h)24 24 58 58
LocationResidual interstitial in Residual interstitial in
melts.d.peridotites.d.melts.d.peridotites.d.
SiO240.970.8439.310.5340.970.3839.220.19
TiO22.560.621.120.244.670.431.190.22
Al2O313.970.5815.270.3411.840.1514.30.26
MgO23.150.4723.520.5720.080.3322.530.3
FeO5.090.24.470.225.70.214.280.56
CaO0.040.020.030.030.190.250.020.02
Na2O0.280.070.420.070.110.020.280.11
K2O8.780.238.540.2610.060.229.880.09
Cr2O30.560.381.390.260.180.031.250.23
MnO 0.030.010.030.02
NiO0.10.060.180.040.040.030.130.07
BaO0.360.090.40.080.310.060.390.09
Sum95.86 94.65 94.18 93.5
Mg#89.0 90.4 86.3 90.4
n8 11 5 12
ExptG137 G137
P (GPa)3 3
T (°C)1100 1100
Duration (h)132 132
LocationResidual interstitial in
melts.d.peridotites.d.
SiO239.361.0939.850.93
TiO23.10.491.070.56
Al2O313.760.4315.10.53
MgO23.030.3423.890.42
FeO4.410.214.210.14
CaO0.020.010.020.02
Na2O0.140.020.240.04
K2O9.090.228.910.2
Cr2O30.680.131.410.42
MnO
NiO0.080.030.160.03
BaO0.280.080.30.06
Sum93.95 95.16
Mg#90.3 91.0
n6 16
Table
Table 4. Compositions of peridotite minerals in dynamic metasomatism experiments.
Table 4. Compositions of peridotite minerals in dynamic metasomatism experiments.
ExptG132 G128 G138 G131 G137
P (GPa)2 2 2 3 3
T (°C)1050 1125 1100 1100 1100
Duration (h)72 72 24 58 132
MineralCPXs.d.CPXs.d.CPXs.d.CPXs.d.CPXs.d.
SiO253.060.5353.91.1154.320.4853.860.2653.930.65
TiO20.280.030.50.120.150.050.170.030.330.18
Al2O33.150.523.50.72.610.183.060.232.670.45
MgO17.740.2818.00.5618.830.3118.380.417.721.01
FeO3.080.163.80.393.440.373.370.094.181.09
CaO20.480.2717.31.718.570.318.330.3519.050.45
Na2O0.620.041.60.640.980.121.110.141.280.27
K2O0.010.010.00.020.020.010.010.010.030.01
Cr2O31.290.151.00.161.330.461.370.150.850.65
MnO0.120.020.10.03 0.120.03
NiO0.040.020.10.010.050.030.040.020.040.05
Sum99.87 99.72 100.3 99.82 100.08
Mg#91.1 89.4 90.7 90.7 88.3
n9 28 18 12 16
ExptG132 G128 G138 G131 G137
P (GPa)2 2 3 3 3
T (°C)1050 1125 1100 1100 1100
Duration (h)72 72 24 58 132
MineralOLs.d.OLs.d.OLs.d.OLs.d.OLs.d.
SiO240.450.1740.320.1941.610.5840.640.1241.380.23
TiO20.020.010.030.020.030.020.010.010.030.02
Al2O30.020.010.030.010.060.060.040.010.020.02
MgO48.850.2248.840.1948.740.3648.80.2249.020.28
FeO10.380.2710.310.210.770.4510.430.2911.310.37
CaO0.090.010.110.030.110.020.080.010.080.02
Na2O0.010.010.010.010.020.020.010.010.020.02
K2O00000.030.0500.0100
Cr2O30.040.010.060.010.090.080.060.010.070.04
MnO0.160.040.140.03 0.150.02
NiO0.350.050.360.040.260.040.380.030.290.05
Sum100.37 100.21 101.72 100.6 102.22
Mg#89.3 89.4 89.0 89.3 88.5
n12 19 14 9 6
ExptG139 G138 G131 G137
P (GPa)3 3 3 3
T (°C)1250 1100 1100 1100
Duration (h)24 24 58 132
MineralOLs.d.OPXs.d.OPXs.d.OPXs.d.
SiO240.630.3557.580.5256.40.5857.140.93
TiO20.020.020.190.060.130.030.180.06
Al2O30.030.011.410.572.010.531.220.37
MgO50.430.5632.939533.130.3933.480.75
FeO8.810.417.541.246.390.427.350.87
CaO0.120.021.360.231.210.061.130.08
Na2O0.010.010.190.080.170.050.170.07
K2O0.010.020.010.040.010.0110.07
Cr2O30.210.070.30.360.590.280.240.16
MnO 0.150.03
NiO0.170.090.060.030.120.020.070.04
Sum100.44 101.57 100.31 101.984
Mg#91.1 88.6 90.2 89.0
n21 12 10 23
Table
Table 5. Melt compositions in dynamic metasomatism experiments.
Table 5. Melt compositions in dynamic metasomatism experiments.
ExptG132 G132 G128 G128
P (GPa)2 2 2 2
T (°C)1050 1050 1125 1125
Duration (h)72 72 72 72
Residual Melt Residual Melt
melts.d.traps.d.melts.d.traps.d.
SiO256.332.1452.492.9255.540.3048.632.42
TiO22.980.261.240.252.410.131.320.21
Al2O310.100.1514.961.2010.620.0915.441.04
MgO3.612.408.212.183.140.768.571.44
FeO5.580.645.211.014.790.175.890.59
CaO4.180.394.962.052.090.118.522.99
Na2O1.570.282.220.461.930.153.000.67
K2O7.590.265.821.0411.200.183.930.84
Cr2O30.010.020.090.040.010.010.090.04
MnO0.100.030.120.060.090.020.150.07
NiO0.010.020.030.040.010.010.020.03
BaO0.650.060.130.060.660.050.070.04
P2O52.280.300.390.251.660.080.390.09
Sum94.98 95.87 94.16 96.01
Mg#53.5 73.7 53.8 72.2
n8 23 7 23
ExptG138 G138 G131 G131
P (GPa)3 3 3 3
T (°C)1100 1100 1100 1100
Duration (h)24 24 58 58
Residual Melt Residual Melt
melts.d.traps.d.melts.d.traps.d.
SiO241.751.8944.581.9252.011.5343.682.74
TiO23.240.932.080.323.020.212.090.48
Al2O312.231.4410.341.2510.210.4010.201.88
MgO16.365.6113.922.835.452.3713.282.96
FeO6.852.258.671.395.390.598.591.41
CaO5.412.917.371.553.730.617.163.12
Na2O0.750.352.150.602.080.331.740.47
K2O6.672.234.720.978.610.285.711.74
Cr2O30.030.040.110.060.020.020.120.14
MnO0.000.000.00 0.120.010.180.06
NiO0.070.050.020.030.020.020.040.04
BaO0.470.210.320.180.630.070.410.16
P2O50.090.100.600.302.010.331.540.69
Sum93.90 94.89 93.30 94.76
Mg#81.0 74.1 64.3 73.4
n11 11 9 23
ExptG137 G139 G139 G139
P (GPa)3 3 3 3
T (°C)1100 1250 1250 1250
Duration (h)132 24 24 24
Melt Residual interstital in Melt
traps.d.melts.d.peridotites.d.traps.d.
SiO242.701.8949.060.8151.030.4050.462.28
TiO22.630.231.870.071.830.101.470.22
Al2O310.010.849.600.139.800.2110.820.89
MgO14.072.2714.762.0211.961.7613.233.71
FeO9.111.196.800.186.830.385.651.09
CaO5.821.855.881.387.511.326.461.17
Na2O2.640.870.600.080.530.091.250.39
K2O6.101.324.620.434.320.345.271.13
Cr2O30.060.060.410.090.380.080.390.13
MnO0.000.000.000.000.000.000.000.00
NiO0.030.040.010.020.010.020.030.05
BaO0.540.170.310.050.330.060.370.10
P2O50.560.700.570.060.540.080.480.15
Sum94.27 94.50 95.07 95.88
Mg#73.4 79.5 75.7 80.7
n14 10 12 11
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Foley, S.F.; Pertermann, M. Dynamic Metasomatism Experiments Investigating the Interaction between Migrating Potassic Melt and Garnet Peridotite. Geosciences 2021, 11, 432. https://doi.org/10.3390/geosciences11100432

AMA Style

Foley SF, Pertermann M. Dynamic Metasomatism Experiments Investigating the Interaction between Migrating Potassic Melt and Garnet Peridotite. Geosciences. 2021; 11(10):432. https://doi.org/10.3390/geosciences11100432

Chicago/Turabian Style

Foley, Stephen F., and Maik Pertermann. 2021. "Dynamic Metasomatism Experiments Investigating the Interaction between Migrating Potassic Melt and Garnet Peridotite" Geosciences 11, no. 10: 432. https://doi.org/10.3390/geosciences11100432

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