Journal topic
Eur. J. Mineral., 32, 251–264, 2020
https://doi.org/10.5194/ejm-32-251-2020
Eur. J. Mineral., 32, 251–264, 2020
https://doi.org/10.5194/ejm-32-251-2020

Research article 23 Mar 2020

Research article | 23 Mar 2020

# Melting relations of anhydrous olivine-free pyroxenite Px1 at 2 GPa

Melting relations of anhydrous olivine-free pyroxenite Px1 at 2 GPa
Giulio Borghini and Patrizia Fumagalli Giulio Borghini and Patrizia Fumagalli
• Dipartimento di Scienze della Terra, via Botticelli 23, 20133 Milan, Italy

Correspondence: Patrizia Fumagalli (patrizia.fumagalli@unimi.it)

Abstract

The reaction between melt derived by mafic heterogeneities and peridotites in an upwelling mantle may form hybrid olivine-free pyroxenites. In order to evaluate the impact of these lithologies on the chemistry of primitive magmas and their ability to give rise to new mantle heterogeneities, we experimentally investigate the melting relations at 2 GPa of the model olivine-free pyroxenite Px1 (XMg=0.81, SiO2=52.9 wt %, Al2O3 = 11.3 wt %, CaO = 7.6 wt %). The subsolidus assemblage consists of clinopyroxene, orthopyroxene, and garnet. At 2 GPa, the solidus of Px1 is located between 1250 and 1280 C, at a temperature about 70 C lower than the solidus of fertile lherzolite. At increasing melt fraction, the sequence of mineral phase disappearance is garnet–clinopyroxene–orthopyroxene. Across the solidus, partial melting of Px1 is controlled by reaction garnet + clinopyroxene = liquid + orthopyroxene, and above 1300 C, once garnet is completely consumed, by reaction clinopyroxene + orthopyroxene = liquid. Orthopyroxene is the liquidus phase, and at 1480 C olivine-free pyroxenite Px1 is completely molten indicating a melting interval of about 200 C. Isobaric melt productivity is similar to garnet clinopyroxenites, and it is more than 3 times that of a fertile lherzolite at 1400 C. Px1 partial melts cover a wide range of XMg (0.57–0.84), with SiO2, Al2O3 and Na2O decreasing and Cr2O3 increasing with the degree of melting. CaO content in partial melts increases as long as clinopyroxene is involved in melting reactions and decreases after its exhaustion. At 2 GPa and for melting degrees higher than 10 %, Px1 produces MgO-rich basaltic andesites matching the composition of eclogitic melts in terms of silica and alkali contents but with significantly higher XMg values. These melts differ from those derived from lherzolites at 2 GPa by higher SiO2 and lower CaO contents. Their high silica activity makes them very reactive with mantle peridotite producing hybrid orthopyroxene-rich lithologies and residual websterites. Melt–rock reactions likely prevent direct extraction of melts produced by olivine-free pyroxenites.

1 Introduction

Several lines of evidence indicate that the upper mantle contains a significant fraction of mafic lithologies (e.g., Hofmann, 2007, and references therein), likely included to depth via subduction, which are expected to form eclogites at pressures above 2.0 GPa (Ringwood and Green, 1966; Allègre and Turcotte, 1986; Yasuda et al., 1994; Hirschmann and Stolper, 1996; Kogiso et al., 2004a). Even though volumetrically subordinated to ultramafic peridotites, they may play an important role in basalt generation because of their large contribution to mantle magma production as a result of their high melt productivity with respect to peridotites (e.g., Hirschmann and Stolper, 1996; Phipps Morgan, 2001; Kogiso et al., 2003; Pertermann and Hirschmann, 2003a, b). Many ocean island basalts (OIBs) have isotopic and geochemical signatures that require the partial melting of mafic components (e.g., Hofmann, 1997, 2007; Lassiter et al., 2000; Sobolev et al., 2005, 2007; Herzberg, 2011; Mallik and Dasgupta, 2012). Moreover, there is a growing consensus that some mid-ocean ridge basalts (MORBs) derive from a heterogeneous mantle source including peridotite mixed to olivine-poor pyroxenites (Lambart et al., 2012, 2013, 2016; Borghini et al., 2017; Lambart, 2017; Brunelli et al., 2018).

Crustal-derived mafic rocks represent low-solidus mantle lithologies and start melting at higher pressure than “dry” peridotites (e.g., Yasuda et al., 1994; Pertermann and Hirschmann, 2003a, b; Kogiso et al., 2004a; Kogiso and Hirschmann, 2006; Yaxley and Sobolev, 2007; Spandler et al., 2008). Their partial melts are expected to react with the surrounding peridotite either modifying the composition of the rising melts (Pilet et al., 2008; Mallik and Dasgupta, 2012, 2013, 2014) or creating new hybrid rocks, called secondary or stage 2 pyroxenites (e.g., Yaxley and Green, 1998; Sobolev et al., 2005, 2007; Herzberg, 2006, 2011; Lambart et al., 2012). Heterogeneous upwelling mantle is subject to continuous events of partial melting and melt–rock reactions that potentially replace the mafic components with a compositionally wide range of hybrid lithologies, including metasomatized peridotites and variably residual pyroxenites (e.g., Yaxley and Green, 1998; Spandler et al., 2008; Rosenthal et al., 2014, 2018). Petrological studies on ultramafic massifs have interpreted some pyroxenites embedded in mantle peridotite as natural examples of secondary pyroxenites, originated through high-pressure melt–peridotite reactions (i.e., Garrido and Bodinier, 1999; Bodinier et al., 2008; Gysi et al., 2011; Marchesi et al., 2013; Borghini et al., 2013, 2016, 2019; Montanini and Tribuzio, 2015).

A large number of experimental studies have been dedicated to partial melting of pyroxenites defining a large spectrum of partial melts compositions (e.g., Yaxley and Green, 1998; Kogiso and Hirschmann, 2001; Hirschmann et al., 2003; Pertermann and Hirschmann, 2003a; Kogiso et al., 2004a; Keshav et al., 2004; Médard et al., 2006; Sobolev et al., 2007; Lambart et al., 2009, 2013). These studies emphasized the existence of the garnet–pyroxene thermal divide, defined by the enstatite–Ca-Tschermak's pyroxene (En–CaTs) plane in the pseudoternary diagram forsterite–CaTs–quartz (Fo–CaTs–Qz) projected from diopside (Di) (e.g., Kogiso et al., 2004a; Lambart et al., 2013). The divide separates two fundamental types of pyroxenites: silica-excess (SE) pyroxenites plotting in the En–CaTs–Qz plane and silica-deficient (SD) pyroxenites contained in the En–Fo–CaTs triangle (e.g., Kogiso et al., 2004a; Lambart et al., 2013) Above 2 GPa, when garnet and pyroxenes are the main residual phases, it represents a thermal barrier controlling melting relations of pyroxenites. The most relevant effect is that at P>2 GPa SE and SD pyroxenites generate melts in the En–CaTs–Qz and En–Fo–CaTs triangle, respectively (Kogiso et al., 2004a).

Although several experimental works focused on melting relations in SD pyroxenites and eclogites (Lambart et al., 2013, and references therein), the melting behavior of hybrid olivine-free pyroxenites has been poorly evaluated. Recently, Borghini et al. (2017) have experimentally investigated an olivine-poor SD secondary pyroxenite concluding that during the partial melting of a heterogeneous peridotite–pyroxenite mantle source its involvement does not significantly impact on major element composition of primary basalts. In order to evaluate the role of olivine-free lithologies in the origin of Hawaiian OIBs, Sobolev et al. (2007) studied the melting behavior at 3.5 GPa of an olivine-free SE secondary pyroxenite, whose composition was modeled as product of reaction between eclogite-derived silica-rich melts and a peridotite. The composition of partial melts produced by this olivine-free SE pyroxenite allowed one to explain the unusually high NiO and SiO2 contents of most parental Hawaiian magmas giving rise to a quantitative model supporting the significant role of such lithology (Sobolev et al., 2005, 2007). Indeed, olivine-free rocks have been taken into consideration as a relevant mantle component in partial melting (Mallik and Dasgupta, 2012; Lambart et al., 2012, 2013; Lambart, 2017) or as a source for refertilizing mantle melts (e.g., Pearson and Nowell, 2004; Borghini et al., 2013, 2016; Tilhac et al., 2016, 2017; Varas-Reus et al., 2018). However, their melting behavior at shallower mantle levels (P<3.5 GPa) is currently not available. The knowledge of the composition of partial melts produced by hybrid SE pyroxenite will contribute to understand their implications on basalts chemistry as well as to investigate their interaction with peridotite within an upwelling heterogeneous mantle.

We present the results of partial melting experiments performed on the secondary-type SE pyroxenite Px1 previously studied by Sobolev et al. (2007). The major aim of our work is to depict the composition of melts produced by moderate to high degrees of melting of hybrid pyroxenite at 2 GPa. We discuss the fate of these pyroxenitic melts in the context of upwelling heterogeneous mantle as a function of potential temperature of mantle adiabat.

2 Experimental and analytical techniques

Px1 is a model olivine-free pyroxenite resulting from the reaction between high-Si eclogite-derived melt and peridotite (Sobolev et al., 2005, 2007). It is a synthetic sintered oxide mixture prepared by blending high purity oxides and carbonates at Australian National University and kindly provided by Gregory Yaxley.

In Fig. 1 the bulk composition of Px1 is compared with bulk compositions previously used in partial melting experiments at 2 GPa (Table 1). When compared to eclogites and MORB-like pyroxenites (SE pyroxenites), Px1 has significantly higher XMg [XMg = molar Mg/(Mg + Fetot) = 0.81] and SiO2 content coupled with relatively low Al2O3 and CaO contents (Fig. 1). This bulk composition diverges from the nominally “dry” SD pyroxenites in relation to much higher SiO2 content (Fig. 1). Moreover, in spite of similar XMg, Px1 has higher SiO2 and Al2O3 and lower CaO when compared with the clinopyroxenite OLCPX1 experimentally investigated by Kogiso and Hirschmann (2001) (Fig. 1).

Table 1Bulk compositions experimentally investigated at 2 GPa.

CIPW norm nepheline–olivine–hypersthene–diopside–feldspars (1) this study; (2) Hirschmann et al. (2003); (3) Pertermann and Hirschmann (2003a); (4) Keshav et al. (2004);
(5) Kogiso and Hirschmann (2001); (6) Wang et al. (2010); (7) and (8) Lambart et al. (2013).

Figure 1SiO2, Al2O3 and CaO vs. XMg= MgO/(MgO + FeOtot) diagrams showing the composition from this study (Px1) compared to compositions from previous experimental studies at 2 GPa. Silica-excess (SE) pyroxenites (red and orange symbols): olivine-free pyroxenite Px1 (This study); MORB-like pyroxenite G2 (Pertermann and Hisrchmann, 2003a); eclogite D96-25 (Wang et al., 2010). Silica-deficient (SD) pyroxenites (blue and black symbols): garnet pyroxenite MIX1G (Hirschmann et al., 2003); garnet clinopyroxenite 77SL-582 (Keshav et al., 2004); mixtures of peridotite and MORB KG1 (1:1) and KG2 (2:1) (Kogiso et al., 1998); olivine clinopyroxenite OLCPX1 (Kogiso and Hirschmann, 2001); garnet websterite M5-40 and garnet–olivine clinopyroxenite M7-16 (Lambart et al., 2013). The compositional field defined by MORB (Gale et al., 2013) and the MORB pyrolite (Green et al., 1979) are also reported.

Experiments were conducted at 2.0 GPa, and temperatures from 1250 to 1480 C, at the Laboratorio di Petrologia Sperimentale, Dipartimento di Scienze della Terra “Ardito Desio”, Università degli Studi di Milano. Experiments were carried out in an end-loaded piston cylinder using MgO–Pyrex-salt assemblies. Run durations range from 36 to 168 h (Table 2) following previous partial melting experiments (i.e., Kogiso and Hirschmann, 2001; Pertermann and Hirschmann, 2003a, b; Lambart et al., 2009; Borghini et al., 2017).

Table 2Experimental run conditions and products.

Sum of the squares of residuals for all elements calculated as the sum of the squares of the difference between model and calculated composition. opx, orthopyroxene; cpx, clinopyroxene; grt, garnet. Numbers in parentheses are propagated errors estimated by Monte Carlo simulations statistically treated as in Fumagalli et al. (2009).

Platinum capsules (outer diameter 3.0; length 7–8 mm) have been welded after being loaded with an inner graphite capsule containing approximately 20 mg of starting material. Graphite isolated the samples from the Pt capsule to avoid Fe loss (e.g., Kinzler, 1997; Walter, 1998). The graphite–Pt assembly keeps the oxygen fugacity below the graphite–C–O vapor buffer (e.g., Ulmer and Luth, 1991; Médard et al., 2008). A layer of vitreous carbon spheres (80–125 µm diameter) at the top of the capsule (less than 20 % wt % of the starting material) was used to extract a part of the partial melt (e.g., Pickering-Witter and Johnston, 2000; Wasylenki et al., 2003; Médard et al., 2006). A 0.5 mm thick hard corundum disk separated the thermocouple tip from the platinum capsule. In order to maintain anhydrous conditions (i) the graphite–Pt assembly loaded with the starting material was dried overnight in an oven at 250 C before being rapidly welded shut, and the whole assembly was kept in oven at about 200 C for several hours before running the experiments. Temperature was measured by S-type thermocouples and is considered to be accurate to ±5C. At an initial pressure of 0.25 GPa the sample was heated to 400 C for 10 min in order to soften the Pyrex; then, pressure was raised to the experimental value before reaching the desired temperature. Runs were terminated by turning off the power. Capsules were enclosed in epoxy, sectioned lengthwise, polished, and carbon-coated.

Run products were carefully characterized by backscattered electron (BSE) images and microanalyses using a JEOL JXA 8200 Superprobe equipped with five wavelength-dispersive spectrometers and one energy-dispersive spectrometer (EDS) at the Dipartimento di Scienze della Terra “Ardito Desio”, Università degli Studi di Milano. X-ray element maps further helped the textural and chemical examination of the experimental charges. Analyses on mineral phases were performed using 1 µm beam size and beam conditions of 15 kV and 5 nA. Counting time was 30 s for peak and 10 s for background. Whenever possible, in order to prevent alkali loss, we analyzed glass using a beam size of 5 µm, or 2–3 µm in experiments with very low melt fractions occurring as thin interstitial films.

3 Results

## 3.1 Phase assemblages and textures

Experimental details and run products are summarized in Table 2. At 2 GPa and 1250 C, pyroxenite Px1 is at subsolidus and the mineral assemblage is made of orthopyroxene, clinopyroxene, and garnet (Fig. S1a in the Supplement). Orthopyroxene occurs, in all runs, as rounded grains ranging from 5 to 20 µm in size. Clinopyroxene is smaller (2–10 µm) and generally shows polygonal crystals. Garnet is homogenously dispersed in the charges and forms irregular crystals (up to 50 µm) that include small rounded clinopyroxene and rarely orthopyroxene (Fig. 2). At 1280 C, the incipient melting is testified by the occurrence of very thin patches of glass interstitial to pyroxenes and garnet (Fig. 2a). Chemical analyses of glass in this low-T experiment are quite difficult, although few data have been collected within the carbon sphere layer at the top of the capsule (Fig. S1b). From 1300 to 1400 C, the amount of glass progressively increases and glass tends to form larger patches (5–15 µm) interstitial to residual minerals and concentrated within the carbon spheres layer (Fig. 2b, c). At 1350 C, garnet is completely exhausted and glass coexists with large rounded orthopyroxene (40–50 µm) and smaller clinopyroxene (5–10 µm) (Fig. 2c).

Figure 2Backscattered electron (BSE) images of representative textures of melting experiments on pyroxenite Px1. (a) Run Px1-5 (1280 C): the occurrence of very thin patches of glass interstitial to pyroxene and garnet indicates a very low degree of melting. (b) Run Px1-1 (1300 C): glass patches (5–15 µm) in equilibrium with residual clinopyroxene, orthopyroxene, and garnet. (c) Run Px1-4 (1350 C): large rounded orthopyroxene (40–50 µm) and smaller clinopyroxene (5–10 µm) coexisting with liquid mostly contained in the carbon sphere layer. (d) Run Px1-2 (1400 C): high-degree melting experiments with residual orthopyroxene and minor clinopyroxene at the bottom of the capsule and glass completely filling the carbon sphere layer.

At 1400 C, residual orthopyroxene and minor clinopyroxene are confined at the bottom of the capsule and glass completely fills the carbon sphere layer (Fig. 2d). At 1450 C, clinopyroxene disappears and a homogeneous glass coexists with coarse residual orthopyroxene (20–50 µm). At 1480 C, the pyroxenite Px1 is completely melted and the capsule contains glass and quenched minerals (Fig. S1c in the Supplement).

## 3.2 Liquid and mineral compositions

The compositions of glasses and minerals are reported in Table 3. At increasing temperature, MgO and Cr2O3 contents progressively increase and SiO2, Na2O and TiO2 abundances decrease (Fig. 3). At near solidus conditions (1280 C) glass is very high in SiO2 (SiO2 = 59.97 wt %). At increasing temperature, SiO2 progressively decreases until orthopyroxene is the only residual phase at 1450 C (Fig. 3). MgO regularly increases along the whole melting range from 3.97 to 18.94 wt % (Fig. 3). FeO content is relatively low at 1280 C, while starting from 1300 C it defines a rather flat trend varying from 6.31 to 7.10 wt % (Fig. 3). Al2O3 concentration slightly increases as long as garnet is a melting phase, and it progressively decreases once garnet is exhausted (T>1350C, Fig. 3). CaO abundance weakly increases up to 1400 C, as long as clinopyroxene is involved in the melting reactions, and at it decreases at a higher temperature once clinopyroxene is completely consumed (Fig. 3). Na2O and TiO2 behave as incompatible elements rapidly decreasing at increasing temperature, from 3.67 to 1.54 wt % and from 2.39 to 0.61 wt %, respectively (Fig. 3). K2O is very low in agreement with its low concentration in the bulk (Table 1); it reaches 0.21 wt % in experiment near the solidus and decreases with increasing degree of melting (Table 3).

Table 3Average compositions (wt %) of liquids and residual phases.

Numbers in parentheses correspond to 1σ standard deviations, given in terms of the least unit cited; e.g. 0.48 (8) and 54.31 (66) represent 0.48±0.08 and 54.31±0.66, respectively. Abbreviations are: gl glass, cpx clinopyroxene,
opx orthopyroxene, gnt garnet. Numbers of analyses are in parentheses. (*) CIPW norms: quartz/hypersthene/diopside/feldspars /olivine.

Figure 3Oxide concentrations (wt %) in experimental melts vs. temperature (C). When not visible, the error bar (1σ) is smaller than the symbol. Also reported are the limits of garnet and clinopyroxene stability, the blue and orange dashed lines, respectively.

In total alkali vs. SiO2 diagram melts produced by pyroxenite Px1 at 2.0 GPa are andesites, are at the lowest temperature investigated (1280 C), and shift to basaltic andesites (1300–1400 C) and basalts at very high degree of melting (Fig. 4).

Figure 4TAS (total alkali vs. silica) diagram showing the composition of Px1 partial melts compared to liquid compositions from different SE and SD pyroxenites experimentally derived at 2 GPa. Symbols and references are as in Fig. 1.

Orthopyroxene has an XMg average value of 0.83 at subsolidus conditions and, as expected, records a progressive XMg increase with temperature up to 0.90 at 1450 C (Table 3, Fig. 5a). Al2O3 content in orthopyroxene decreases across the solidus from 6.88 to 5.84 wt %; it increases as garnet disappears, at 1350 C but decreases again at a higher temperature (Table 3). The CaO abundance is rather high, as observed in previous pyroxenite melting experiments (e.g., Kogiso et al., 1998; Lambart et al., 2009; Borghini et al., 2017); it starts from 1.07 wt % at subsolidus and reaches 2.01 wt % at 1450 C (Table 3). TiO2 weakly decreases with temperature from 0.36 to 0.21 wt %, and Cr2O3 contents are always lower than 0.3 wt % (Table 3).

Figure 5Fe–Mg partitioning between glass and orthopyroxene (a), glass and clinopyroxene (b), and clinopyroxene and orthopyroxene (c). XMg= Mg/(Mg + Fetot). In (c) the gray field is defined by curves computed from the clinopyroxene–orthopyroxene thermobarometer of Brey and Köhler (1990) in the temperature range from 1250 to 1400 C, at a pressure of 2 GPa.

Subsolidus clinopyroxene shows an XMg value equal to 0.82 and very high Na2O content (Na2O= 2.32 wt %) (Table 3). As the melting degree increases, clinopyroxene displays a gradual XMg increase up to 0.88 at 1400 C (Fig. 5b) and a Na2O decrease down to 0.84 wt % (Table 3). Al2O3 content is rather constant and varies from 8.91 to 8.21 wt % (Table 3). Cr2O3 ranges from 0.28 and 0.43 wt % (Table 3). In glass-bearing runs, TiO2 content in clinopyroxene decreases at increasing temperature from 0.88 to 0.36 wt % (Table 3).

Garnet is characterized by an XMg increase from 0.74 in the subsolidus experiment to 0.82 at 1300 C, the last temperature at which it is stable (Table 3). With increasing temperature, garnet shows an increase of pyrope content coupled to a decrease in almandine molecule. CaO abundance varies in a narrow range from 5.01 to 5.72 wt % (Table 3). TiO2 content records the highest value in garnet at subsolidus and decreases with temperature, from 0.97 to 0.31 wt % (Table 3). Cr2O3 is low at subsolidus and reaches value of 0.44 wt % in glass-bearing experiment at 1300 C (Table 3).

## 3.3 Approach to equilibrium

Although the present set of experiments was not reversed, some observations strongly suggest that chemical equilibrium was closely approached. X-ray element maps revealed that minerals are compositionally homogeneous and chemically unzoned (Fig. S2). Systematic and consistent variations in mineral chemistry as a function of pressure and temperature conditions also support the attainment of equilibrium, as well as the coherent element partitioning. In particular, the Fe–Mg partitioning between clino- and orthopyroxene defined in our experiments is in good agreement with the partitioning computed using the thermobarometer of Brey and Köhler (1990) (Fig. 5c).

Mass balance calculations by a weighted least squares method (Table 2) provided phase abundances consistent with the melt fraction variations. Residual sums of squares lower than 1 are perfectly comparable to other experimental studies (i.e., Kogiso and Hirschmann, 2001; Pertermann and Hirschmann, 2003a, b; Lambart et al., 2009; Borghini et al., 2017) and indicate reasonable mass balances between analyzed phases and the starting bulk composition. Moreover, results of mass balance calculations indicate that Fe loss was very low (<3 %) in experiments below 1380 C, and it increases at a higher temperature up to 8 %, possibly due to fractures in graphite inner capsule towards the Pt outer capsule.

4 Discussion

## 4.1 Melting and phase relations

Glass and mineral abundances have been calculated by weighted least squares mass balance based on nine oxides: SiO2, TiO2, Al2O3, Cr2O3, FeO, MgO, CaO, Na2O, and K2O (Table 2). Error propagation was carried out by Monte Carlo simulations. Detailed explanation of mass balance calculations is reported in Fumagalli et al. (2009). In Fig. 6 we illustrate the variation of phase abundances as a function of temperature. At 1250 C, glass is absent and Px1 is a garnet websterite formed by clinopyroxene (51.1±4.5 wt %), orthopyroxene (30.1±4.2 wt %), and garnet (18.8±2.2 wt %). Orthopyroxene is stable along the whole melting interval with modal amounts increasing from 30.1 to 34.6±2.2 wt %, from subsolidus condition up to melt fraction of 19.4±5.6 wt % at 1300 C (Table 2 and Fig. 6). This indicates that orthopyroxene is a product of melting reaction as long as garnet is present in the residue.

Figure 6Phase abundances in experimental charges calculated by weighted least squares mass balance as a function of temperature (C). CPX: clinopyroxene, OPX: orthopyroxene, GRT: garnet.

Clinopyroxene is the dominant phase in pyroxenite Px1 at subsolidus. It is largely consumed by the melting reaction and completely exhausted at 1450 C at a melt fraction of 84.7±4.5 wt % (Table 2; Fig. 6). Garnet is the first phase to disappear from the residue at a temperature lower than 1350 C and a melt fraction lower than 33.8±3.2 wt % (Table 2; Fig. 6). With increasing melt fraction, the sequence of mineral phase disappearance is garnet–clinopyroxene–orthopyroxene.

Melting reactions for Px1 at 2 GPa are derived from mass balance calculations, fitting modal abundances of residual phases vs. melt fractions by least-squares (Baker and Stolper, 1994). In the range of 1250–1300 C, the partial melting of Px1 is controlled by following reaction:

$\begin{array}{}\text{(1)}& \begin{array}{rl}\mathrm{0.58}\phantom{\rule{0.25em}{0ex}}\phantom{\rule{0.25em}{0ex}}\text{garnet}& +\phantom{\rule{0.25em}{0ex}}\phantom{\rule{0.25em}{0ex}}\mathrm{0.64}\phantom{\rule{0.25em}{0ex}}\phantom{\rule{0.25em}{0ex}}\text{clinopyroxene}\phantom{\rule{0.25em}{0ex}}\phantom{\rule{0.25em}{0ex}}=\phantom{\rule{0.25em}{0ex}}\phantom{\rule{0.25em}{0ex}}\mathrm{1}\phantom{\rule{0.25em}{0ex}}\phantom{\rule{0.25em}{0ex}}\text{liquid}\\ & +\phantom{\rule{0.25em}{0ex}}\phantom{\rule{0.25em}{0ex}}\mathrm{0.22}\phantom{\rule{0.25em}{0ex}}\phantom{\rule{0.25em}{0ex}}\text{orthopyroxene}.\end{array}\end{array}$

At 1350 C garnet is completely consumed, the orthopyroxene becomes a reactant, and in the range 1350–1400 C the melting reaction is

$\begin{array}{}\text{(2)}& \begin{array}{rl}\mathrm{0.92}\phantom{\rule{0.25em}{0ex}}\phantom{\rule{0.25em}{0ex}}\text{clinopyroxene}& +\phantom{\rule{0.25em}{0ex}}\phantom{\rule{0.25em}{0ex}}\mathrm{0.08}\phantom{\rule{0.25em}{0ex}}\phantom{\rule{0.25em}{0ex}}\text{orthopyroxene}\\ & =\phantom{\rule{0.25em}{0ex}}\phantom{\rule{0.25em}{0ex}}\mathrm{1}\phantom{\rule{0.25em}{0ex}}\phantom{\rule{0.25em}{0ex}}\text{liquid}.\end{array}\end{array}$

At 1450 C clinopyroxene is exhausted; orthopyroxene is the liquidus phase and at 1480 C Px1 is completely molten.

At 2 GPa, Px1 melting interval is about 200 C, which is similar to the melting interval documented for other pyroxenites and eclogites (Pertermann and Hirschmann, 2003b; Keshav et al., 2004). Experiments performed at P=3.5 GPa (Sobolev et al., 2007) indicated that orthopyroxene is not present in the subsolidus assemblage, presumably due to the higher solubility of enstatite component in clinopyroxene at increasing pressure. However, it represents a product of melting reaction for low degrees of partial melting and it is consumed at high degrees of melting up to the liquidus (Sobolev et al., 2007).

Melting reactions 1 and 2 differ from those observed in olivine-free SD garnet pyroxenites because spinel is stable, with or without garnet, at subsolidus conditions and a low degree of melting (Hirschmann et al., 2003; Keshav et al., 2004). Moreover, in the SD pyroxenites orthopyroxene appears as a product of reaction clinopyroxene + spinel = liquid + orthopyroxene only at a high degree of melting (Keshav et al., 2004). Melting relations experimentally derived for SE MORB-like pyroxenite G2 at 3 GPa indicated that garnet and clinopyroxene strongly contribute to melt formation at near solidus, together with rutile and quartz that quickly disappear after very low melting degree (Pertermann and Hirschmann, 2003a). At 2–3 GPa, clinopyroxene is on the liquidus of the SE pyroxenite G2 and orthopyroxene is never stable either as a subsolidus or as a residual phase (Pertermann and Hirschmann, 2003a, b).

## 4.2 Melt productivity at 2 GPa

The solidus of olivine-free pyroxenite Px1 at 2 GPa is located between 1250 and 1280 C. In Fig. 7 we show melt fractions of this study, derived by mass balance calculations, as a function of temperature compared with previous partial melting experiments at 2 GPa on other pyroxenites (Kogiso et al., 1998; Hirschmann et al., 2003; Keshav et al., 2004; Lambart et al., 2013), eclogites (Pertermann and Hirschmann, 2003b; Wang et al., 2010), and lherzolites (Hirose and Kushiro, 1993). Experimental data on Px1 and most of all the other compositions show melt fraction vs. temperature relations that are rather straight or weakly concave upwards. As a result we assume a linear isobaric melt productivity (dF/dT)P and quantify it as (ΔF∕ΔT)P = [(FT2${F}_{T\mathrm{1}}\right)/\left({T}_{\mathrm{2}}-{T}_{\mathrm{1}}\right)$]P, where T1 and T2 are minimum and maximum experimental temperature, respectively. Px1 presents a melt fraction vs. temperature trend rather comparable with other pyroxenites and eclogites (Fig. 7). In particular Px1 has a (ΔF∕ΔT)P= 0.45, which is slightly lower than the value of 0.53 determined for basaltic pyroxenite G2 (Pertermann and Hirschmann, 2003b). Furthermore, eclogites display similar isobaric melt productivity but shifted towards lower temperatures than pyroxenites, in agreement with their more fertile compositions in terms of XMg and alkali contents (e.g., Kogiso et al., 2004a; Lambart et al., 2016). On the other hand, experiments on garnet pyroxenite at 2 GPa (Keshav et al., 2004) provide a rather high ($\mathrm{\Delta }F/\mathrm{\Delta }T{\right)}_{\mathrm{P}}=\mathrm{0.78}$.

Figure 7Temperature vs. melt fraction determined for pyroxenite Px1 (this work) compared to those from other experimental studies on dry SE and SD pyroxenites, eclogites, and peridotites at 2 GPa. Symbols and references are as in Fig. 1. Melt fractions of a highly fertile lherzolite (HK66) and fertile lherzolite (KLB-1) experimentally derived at 2 GPa (Hirose and Kushiro, 1993) are also shown for comparison. “MELT-PX” refers to the melt fraction curve (from 5 % melting up to clinopyroxene disappearance) computed for composition Px1 using the parameterization proposed by Lambart et al. (2016).

Using the empirical parameterization proposed by Lambart et al. (2016), we computed the melt fraction vs. temperature relation for composition Px1 from 5 % of melting up to clinopyroxene disappearance (red dashed line in Fig. 7). Compared to our experiments, the model gives a slightly steeper isobaric melt productivity, with ($\mathrm{\Delta }F/\mathrm{\Delta }T{\right)}_{\mathrm{P}}=\mathrm{0.56}$. At fixed melt fraction, the slightly higher temperatures of the model, as compared with the experimentally derived melt fraction vs. temperature relation, are within the standard error of the parameterization (±30, Lambart et al., 2016).

In comparison, melt fractions obtained in experiments on lherzolites yield lower values of (dF/dT)P (Fig. 7). In the range 1375–1400 C, pyroxenite Px1 produces a melt amount that is more than 3 times the amount potentially extracted from the fertile lherzolite KLB-1. In keeping with the steeper (dF/dT)P of pyroxenite, the difference in isobaric melt production between Px1 and peridotite increases with temperature (Fig. 7).

## 4.3 Composition of pyroxenite-derived melts at 2 GPa and their role in upwelling mantle

In Fig. 8, the compositions of melts produced by pyroxenite Px1 are projected from diopside (Di) in the pseudo-ternary diagram Fo–CaTs–Qz and compared with the compositions of partial melts obtained in melting experiments on peridotites and pyroxenites at 2 GPa. All the compositions of Px1 partial melts, as well as the Px1 bulk, plot on the right side of the CaTs–En join, together with the other SE MORB–pyroxenites G2 (Pertermann and Hirschmann, 2003a) and D95-25 (Wang et al., 2010). In agreement with the presence of the thermal divide at 2 GPa (e.g., Kogiso et al., 2004a; Lambart et al., 2013), the SD pyroxenites and peridotites produce melt compositions plotting on the left side of the CaTs–En join (Fig. 8). In order to evaluate the effect of pressure, the partial melts reported for the same bulk composition Px1 at 3.5 GPa (Sobolev et al., 2007) are considered. Although up to moderate melting degree melt compositions at 3.5 GPa are well comparable with those at 2 GPa, at increasing melt fractions they deviate towards the quartz apex (Fig. 8). This is presumably related to the fact that, at high pressure (3.5 GPa), orthopyroxene is not involved in melting reactions until high degrees of melting are reached (Sobolev et al., 2007).

Figure 8Molar projections from diopside [Di] into the pseudoternary diagram forsterite–Ca-Tschermak–quartz (Fo–CaTs–Qz) (O'Hara, 1972) of melts produced by experiments on Px1 at 2 GPa (this study) and 3.5 GPa (Sobolev et al., 2007). The melt compositions reported in previous experimental studies on other pyroxenites, eclogites, and peridotites are also plotted. Symbols and references are as in Fig. 7. Larger symbols represent the starting bulk compositions.

In Fig. 9 the compositions of partial melts derived from Px1 are compared with experimental results for different pyroxenites, eclogites, and peridotites at 2 GPa. Although major element oxides (Al2O3, Na2O, TiO2 and Cr2O3, Fig. 9) present very similar abundances in all bulk compositions, partial melts of Px1 show higher SiO2 and slightly lower CaO. Interestingly, the Px1 partial melts, although very similar to eclogitic melts (Pertermann and Hirschmann, 2003a; Wang et al., 2010), present significantly higher XMg values. At 2 GPa, liquids produced by eclogites display XMg lower than 0.60, whereas Px1 melts vary within a range of higher XMg value (XMg=0.57–0.81) (Fig. 9). On the other hand, for moderate to high degree of melting, Px1 partial melts have XMg similar to peridotite-derived melts but with higher SiO2 contents (Fig. 9).

Figure 9Compositions (wt %) of Px1 partial melts from this study compared with those of experimental melts in SE and SD pyroxenites, eclogites, and peridotites at 2.0 GPa. Symbols and references are as in Fig. 7.

In order to discuss the implications of melting of olivine-free hybrid pyroxenite Px1, we simulated the evolution of an upwelling heterogeneous mantle at 2 GPa, using the parameterization of Lambart et al. (2016). The model allows one to distinguish the contribution of melting of pyroxenite Px1 and fertile lherzolite during the decompressional evolution of a mixed pyroxenite–peridotite mantle source, taking into account the thermodynamics of heterogeneous veined mantle (Phipps Morgan, 2001). We assumed potential temperatures from 1300 to 1550 C, which represent the potential temperatures for ambient mantle below oceanic ridges and plume settings (e.g., Herzberg et al., 2007). We considered heterogeneous mantle portions made of fertile lherzolite hosting pyroxenite Px1 in different mass fraction, i.e., 0.05, 0.02 and 0.5.

Although geochemical and physical models point to pyroxenite abundance in an upwelling mantle at oceanic ridge and plume settings mostly limited to 4 %–10 %, and rarely up to 20 % (e.g., Hirschmann and Stolper, 1996; Pertermann and Hirschmann, 2003b; Lambart et al., 2009; Shorttle and Maclennan, 2011; Shorttle et al., 2014; Brown and Lesher, 2014; Lambart, 2017), secondary-type pyroxenites (as Px1) could be locally more abundant in the mantle. This is because the reaction between eclogite-derived melt and peridotite is able to readily produce a large volume of orthopyroxene-bearing lithologies at the expense of peridotite (Wang et al., 2019). Pyroxenite-rich mantle outcrops documented in orogenic (e.g., Gysi et al., 2011; Hidas et al., 2013) and ophiolitic massifs (e.g., Borghini et al., 2013, 2016; Basch et al., 2019) support this view. However, hybrid rocks have major element composition more refractory with respect to eclogites, often assumed as proxies of the enriched mantle components. Therefore, the geochemical signature that secondary type pyroxenites could transfer to aggregated melts is more diluted (Lambart et al., 2009; Borghini et al., 2017), and the difference in density with the ambient peridotite is significantly reduced (e.g., Schutt and Lesher, 2006).

For a mantle adiabat with a potential temperatures of 1350–1550 C, at 2 GPa both lherzolite and pyroxenite Px1 encounter partial melting. Calculations indicate that pyroxenite Px1 is able to produce melt fractions up to 4 times those produced by the associate lherzolite (Fig. S3). However, in spite of a much higher melt productivity, assuming a pyroxenite mass fraction of 5 %, Px1 modestly contributes to the whole melt fraction. On the contrary, for mantle source containing 50 % of Px1, the contribution to the melt production coming from the pyroxenite component increases up to about 80 % of the whole liquid (Fig. S3). According to the chemical data summarized in Fig. 9, the composition of melts produced by such heterogeneous sources should be basalts with higher SiO2 and slightly lower CaO contents than partial melt produced by peridotite at the same PT conditions.

We computed the activity of SiO2 (aSiO2) of partial melts from Px1 and KLB-1 using MELTS supplemental calculator (Ghiorso and Sack, 1995; Asimow and Ghiorso, 1998) in order to make inferences on the fate of these aggregated melts at lithospheric mantle depths. Px1 partial melts are quartz- or hypersthene-normative liquids (Table 3) with high aSiO2 that decreases from 0.59 to 0.44 as the melting degree increases. At similar conditions, lherzolite KLB-1 produces melt with aSiO2 of 0.37 and 0.41 at 1375 and 1425 C, respectively. Lambart et al. (2012) have investigated the reaction between pyroxenite-derived melt and peridotite by impregnation experiments at 1 and 1.5 GPa combined with thermodynamic calculations. They argued that such interaction results in clinopyroxene-rich product coexisting with olivine or orthopyroxene as a function of aSiO2 of reacting melts. Using impregnating melts with a rather high aSiO2 (e.g., 0.44), they found that melt–peridotite reaction results in olivine dissolution and orthopyroxene crystallization.

We expect therefore that aggregated melts produced by Px1–lherzolite source should inherit high SiO2 activities, even if Px1 moderately contributes to melt production of the whole mantle source. In spite of their relatively high XMg, making them rather similar to peridotite-derived melts (Fig. 9), they are expected to be reactive with ambient mantle peridotite. This could likely imply that they cannot be extracted from the mantle without a significant chemical modification via melt–peridotite reaction that would prevent the transfer of their geochemical signature even in terms of trace elements. According to their high SiO2 activity, the infiltration within shallower mantle peridotite of mixed melts produced by a Px1-bearing mantle source would lead to melt–rock reaction and melt consumption by crystallization with the formation of websteritic rocks (Lambart et al., 2012). However, the capability of pyroxenite-derived melt to directly participate to basalt production depends not only on chemical features but also on physical parameters, such as the length scale of pyroxenite (e.g., Kogiso et al., 2004b; Liu and Liang, 2017) and the porosity (i.e., degree of melting) of the surrounding peridotite (Lambart et al., 2012). Indeed, a large volume of pyroxenite and high porosity of the melting peridotite would favor extraction of these melts. However, the extent to which these parameters allow melt extraction from such heterogeneous mantle source is poorly constrained and still under debate.

For mantle adiabat with a potential temperature lower than 1350 C, according to the model results, mantle peridotite is subsolidus or in a state of incipient melting (F<2 %). Our experiments indicate that pyroxenite Px1 starts melting between 1250 and 1280 C with melt fraction increasing rapidly with temperature (Fig. 6). Partial melts derived from Px1 at T<1350C have very high silica contents (SiO2 = 55–59 wt %) and silica activity (aSiO2=0.52–0.59); therefore, they are expected to react with subsolidus mantle peridotite to produce orthopyroxene-rich lithologies (e.g., Yaxley and Green, 1998; Lambart et al., 2012). Mallik and Dasgupta (2012) experimentally demonstrated that the melts resulting from the interaction between MORB–eclogite partial melts and subsolidus peridotite follow similar chemical evolution of OIBs and some MORBs, from tholeiitic to alkalic melts (Michael et al., 2003; Standish et al., 2008). Partial melts of Px1 are closer to the thermal divide than the eclogitic melts considered by Mallik and Dasgupta (2012), suggesting that a similar geochemical evolution is expected, even for minor melt–rock interaction. However, the reaction between subsolidus peridotite and silica-rich melts likely leads to local freezing (e.g., Lambart et al., 2012; Rosenthal et al., 2014) that prevents direct extraction of these melts. Partial melting of olivine-free pyroxenite embedded into subsolidus peridotite would produce an orthopyroxene-rich reaction zone and residual websterites.

The results of this study strongly support the hypothesis that hybrid mantle heterogeneities such as Px1 may contribute to refertilization of the Earth's mantle. Starting from a deep peridotite-dominated mantle enclosing eclogites or pyroxenites, mantle refertilization results from a complex series of processes (e.g., Spandler et al., 2008; Rosenthal et al., 2018). Mantle heterogeneities undergo dynamic and polybaric transformation mostly driven by multiple episodes of partial melting and interactions with the surrounding mantle.

Data availability
Data availability.

All data derived from this research are presented in the enclosed tables and figures.

Supplement
Supplement.

Author contributions
Author contributions.

All authors contributed to the experimental strategy, result interpretations, and manuscript preparation.

Competing interests
Competing interests.

The authors declare that they have no conflict of interest.

Acknowledgements
Acknowledgements.

The authors are greatly thankful to Gregory Yaxley for providing the starting material Px1. Andrea Risplendente is thanked for technical assistance during the work at the electron microprobe.

Financial support
Financial support.

The research has been supported by the Italian Ministry of Education, University and Research (MIUR) (grant no. PRIN-2015C5LN35) through the project “Melt rock reaction and melt migration in the MORB mantle through combined natural and experimental studies”.

Review statement
Review statement.

This paper was edited by Didier Laporte and reviewed by Gordana Garapic and one anonymous referee.

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