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Article

Ancient Melt Depletion and Metasomatic History of the Subduction Zone Mantle: Osmium Isotope Evidence of Peridotites from the Yap Trench, Western Pacific

by
Ling Chen
1,2,
Limei Tang
1,2,*,
Xiaohu Li
1,2,
Jie Zhang
1,2,*,
Wei Wang
1,2,
Zhenggang Li
1,2,
Hao Wang
1,2,
Xichang Wu
1,2 and
Fengyou Chu
1,2
1
Key Laboratory of Submarine Geosciences, State Oceanic Administration, Hangzhou 310012, China
2
Second Institute of Oceanography, Ministry of Natural Resources, Hangzhou 310012, China
*
Authors to whom correspondence should be addressed.
Minerals 2019, 9(12), 717; https://doi.org/10.3390/min9120717
Submission received: 16 September 2019 / Revised: 14 November 2019 / Accepted: 18 November 2019 / Published: 20 November 2019
(This article belongs to the Section Mineral Geochemistry and Geochronology)
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Abstract

:
Highly depleted peridotites from the Yap Trench in the western Pacific Ocean have been studied for Re-Os elements and Re-Os isotopes. These peridotites have a low Re-Os content and variable 187Os/188Os ratios (0.12043–0.14867). The highest 187Os/188Os ratio is far higher than that of the primitive upper mantle and the lowest 187Os/188Os ratio is comparable to the most unradiogenic 187Os/188Os ratio (0.11933) discovered in subduction zone peridotites. The suprachondritic 187Os/188Os ratios of the Yap Trench peridotites results from modification of the mantle wedge by slab-derived fluid and melt. This is consistent with the observation that high 187Os/188Os ratios generally occur in oceanic peridotites with low Os content (<2 ppb) since Os may be reduced during late processes such as fluid alteration and melt refertilization. The sub-chondritic 187Os/188Os ratios of the Yap Trench peridotites correspond to a Re depletion age of 0.24–1.16 billion years, which means that these peridotites represent old mantle residue of ancient melting events. This ancient melting, combined with probable back-arc melting and forearc melting during subduction initiation, indicates that the Yap Trench mantle has a complex evolutionary history. The amount of old mantle residue in the oceanic asthenosphere was underestimated because the 187Os/188Os ratio in mantle peridotites is elevated during late processes. Therefore, old depleted mantle fragments may contribute substantially to the chemical heterogeneity of the oceanic mantle.

1. Introduction

As 187Re decays to 187Os with a half-life of about 42 billion years (Ga) [1], the 187Os/188Os ratios of basaltic rock and mantle residue diverges. Therefore, the 187Re–187Os system in mantle-derived rock is widely used for detecting mantle melting and post-melting processes, which are essential for constraining the geochemical evolution of the oceanic mantle. During mantle melting, Os behaves as a compatible element, whereas Re is a moderately incompatible element with a bulk partition coefficient similar to that of Al [2,3]. Thus, the residual peridotites will be depleted in Re and evolve to sub-chondritic 187Os/188Os. In contrast, Re-enriched basaltic rock will develop highly suprachondritic 187Os/188Os [3,4,5]. For example, mid-ocean ridge basalts generally have higher 87Os/188Os ratios (0.125–0.23) relative to abyssal peridotites (0.12–0.13) [6]. In addition, the 187Os/188Os ratio in seawater (~1) is much higher than that in the bulk Earth (~0.127) [7]; therefore, apart from mantle melting, the secondary processes also play an important role in shaping the Os isotope composition of the melting residue, resulting in suprachondritic 187Os/188Os ratios. However, unradiogenic 187Os/188Os ratios are widely reported in abyssal peridotites from mid-ocean ridges [8,9,10,11,12]; these peridotites were thought to be inherited from ancient mantle melting events given an oldest depleted age of ~2 Ga [10]. This means that instead of being obscured by secondary processes, ancient melting signatures can survive on long timescales in the oceanic upper mantle. Additional evidence for ancient melting in the oceanic mantle was presented by peridotite mantle xenoliths from oceanic islands, which indicates that mantle plumes also contain components from an ancient recycled lithospheric mantle [13]. With respect to the subduction zone, unradiogenic 187Os/188Os ratios were frequently found in ophiolites and interpreted as representative of the ancient oceanic lithosphere [14,15,16]. By contrast, ancient melting evidence in peridotites from modern subduction zones is relatively scarce; this is probably due to the influence of slab-derived fluids or melts, as revealed by the peridotite xenoliths from convergent plate margins [17]. However, serpentinized peridotites collected from the Izu–Bonin–Mariana forearc have unradiogenic 187Os/188Os ratios that provide a model age of 1.2 Ga, which suggests that ancient depleted mantle can be preserved in modern subduction zones even though it has undergone strong metasomatism [18]. These observations indicate that instead of being homogenized by convective stirring chemical heterogeneities in oceanic mantle occur in different tectonic environments. Mantle peridotites from subduction zones mostly have experienced complex melting histories and were modified by slab-derived materials, which makes it difficult to constrain the primary signature of the asthenosphere. The Re-Os isotope system can provide unique perspective into both the nature of melt extraction and the influence of post-melting processes. In this paper, the Re-Os isotopes of peridotites from the Yap subduction zone were studied to constrain the effect of subduction-related modification and the nature of asthenospheric mantle.

2. Materials and Methods

2.1. Geological Setting

The Yap Trench is located at the junction of the Philippine Sea Plate, the Pacific Plate, and the Caroline Plate (Figure 1). The Mariana Trench, the Palau Trench, and the Caroline Ridge are adjacent to the Yap Trench from the north, southwest, and east, respectively. Along the Yap Trench, the Pacific and Caroline plates subduct below the Philippine Sea Plate at an estimated rate of 0 to 6 mm/year [19]. The Yap Trench is one of the deepest trenches on Earth, with a deepest water depth of 8527 m [20]. The subduction processes, magmatism, and tectonic activity of the Yap Trench have been studied to investigate the dynamic mechanisms and mantle evolution of the Yap subduction system [20,21,22,23,24,25,26,27]. The results have shown that the Yap Trench has some features in common with other subduction zones in the western Pacific, such as a trench–arc–basin system and a great axial depth [22,23]. Moreover, some characteristics of the Yap Trench are distinct from other trenches, for example: a very short distance between the trench axis and the island arc (~50 km), an intersection with the Mariana Trench at a nearly perpendicular angle, a collision with the Caroline Ridge (ESE–WNW trending) from the east, a notable lack of arc volcanism [28,29], little seismicity, and a lack of deep earthquakes [23].
There are complex tectonic morphostructures in the subducting Caroline Plate, such as the Caroline Ridge, the West Caroline Rise, the Sorol Trough, and numerous horsts and grabens [20,25,30,31], thus the tectonic erosion of the overlying plate may be enhanced. As a result, more slab-derived materials were transported into the mantle wedge. In addition, asthenospheric mantle underneath the Philippine Sea Plate is inferred to flow outward through the subducting slab along the southern Mariana–Yap–Palau Trench [32]. These features indicate that the upper mantle beneath the Yap Trench system may have experienced complex evolutionary history, which may have a significant influence on the geochemistry of mantle-derived rocks. Hawkins and Batiza (1977) [29] have shown that the basement of the Yap arc is composed of ultramafic to mafic metamorphic rock. The peridotites and volcanic rocks from the north Yap Escarpment and the Yap Trench were interpreted as subduction-related rocks [24,26]. By contrast, a complex evolutionary history including mantle melting at the initial stage of subduction was proposed to explain the highly depleted Yap Trench peridotites [27].

2.2. Samples and Analytical Methods

Peridotite samples in this study were collected from the northern and southern parts of the Yap Trench using the Chinese manned submersible, Jiaolong (Figure 1). Six samples from the northern Yap Trench were collected during cruise DY125-37 on Dive 112. Two samples from the southern Yap Trench were collected during cruise DY125-38 on Dive 149. Petrographic characteristics and elemental data from the northern Yap Trench samples have been reported by Chen et al. (2019) [27]. In this study, we report new Re-Os elements and Re-Os isotope composition of the Yap Trench peridotites and new major and trace element compositions of the samples from the southern Yap Trench. All of the Yap Trench samples have experienced varying degrees of seafloor weathering and serpentinization. Based on the content of loss on ignition (LOI), the calculated degree of serpentinization is 71.9–78.1% (Serp% = 100 × LOI/PM (H2O), PM (H2O) = 0.18%; PM: primitive mantle) [33]. The surfaces of the peridotite samples were cut off to remove any obvious alteration materials. Then, the selected samples were crushed in agate mortars to powders of 200 mesh size for analysis.
The whole-rock major and trace element analysis was performed at Wuhan Sample Solution Analytical Technology Co., Ltd., Wuhan, China. The major elements were analyzed by X-ray fluorescence (XRF); the analytical precision was better than ±2–5%. Whole-rock trace element analysis was conducted using an Agilent 7700e inductively coupled plasma mass spectrometry (ICP-MS) at Wuhan Sample Solution Analytical Technology Co., Ltd., Wuhan, China. The detailed sample-digesting procedure was as follows: (1) sample powder (200 mesh) was placed in an oven at 105 °C for drying for 12 h; (2) 50 mg of sample powder was accurately weighed and placed in a Teflon bomb; (3) 1 mL HNO3 and 1 mL HF were slowly added into the Teflon bomb; (4) the Teflon bomb was put in a stainless steel pressure jacket and heated to 190 °C in an oven for >24 h; (5) after cooling, the Teflon bomb was opened, placed on a hotplate at 140 °C and evaporated to incipient dryness; 1 mL HNO3 was then added, and the sample was evaporated to dryness again; (6) 1 mL of HNO3, 1 mL of Milli-Q water, and 1 mL of internal standard solution of 1 ppm In were added, and the Teflon bomb was resealed and placed in the oven at 190 °C for >12 h; (7) finally, the solution was transferred to a polyethylene bottle and diluted to 100 g through the addition of 2% HNO3.
Re-Os element and isotope compositions were performed at the State Key Laboratory of Isotope Geochemistry, Guangzhou Institute of Geochemistry, Chinese Academy of Sciences in Guangzhou, China. The Carius tube digestion technique was used for Re-Os chemistry [34]. About 0.5–2 g of each powdered sample was digested and equilibrated with 185Re- and 190Os-enriched spikes in reverse aqua regia (7.5 mL concentrated HNO3 + 2.5 mL concentrated HCl) for 24 h at 240 °C in sealed Carius tubes. Os was extracted by solvent extraction into CCl4 and back-extracted into concentrated HBr, with subsequent cleanup by microdistillation. The Re fraction was separated and purified using anion column chromatography.
Mass spectrometry procedures for the Os are given in Li et al. (2015a) [34]. Os was loaded onto Pt filaments and measured as OsO3 ions via negative-thermal ionization mass spectrometry (N-TIMS, Thermo Fisher Scientific, Waltham, MA, USA) using the electron multiplier mode on a Thermo-Finnigan Triton. Repeated analyses of the Os standard solution (Merck Chemical AA standard solution) yield a mean 187Os/188Os value of 0.12042 ± 0.00027 (2 SD, n = 6) for the period of analysis. These values are in good agreement with a value of 0.12022 ± 0.00020 (2 SD, n = 14) measured on the same mass spectrometer in Faraday cup mode [35].
The Re mass fraction was analyzed using inductively coupled plasma mass spectrometry (Thermo Elemental X2 Series, Thermo Fisher Scientific, Waltham, MA, USA). A conventional low-volume quartz impact bead spray chamber with a Peltier cooled (3 °C) and a 0.4 mL min−1 borosilicate nebulizer (MicroMist GE) was used in the determinations. Ion lens settings, nebulizer gas flow rate, and torch position were optimized daily using a 10 ng mL−1 tuning In–Ce mixture standard solution in order to obtain high instrumental sensitivity and low oxide production levels. A peristaltic pump was not used, as free aspiration of the nebulizer provided better signal stability. The details of the measurements are given in Li et al. (2014) [36]. Total procedural blanks were 0.45 ± 0.04 pg (1σ, n = 3) with an 187Os/188Os ratio of 0.284 ± 0.025 (1σ, n = 3) on average for Os and 5.1 ± 0.9 pg (1σ, n = 3) for Re. All data were corrected for the procedural blank for each analytical batch. Blank contributions were generally insignificant. The average values of the Re-Os isotope for basaltic reference material BIR-1 are in good agreement with published data [37].

3. Results

3.1. Major and Trace Elements

Whole-rock major and trace elements of the studied peridotites are presented in Table 1. Major elements of the Yap Trench peridotites are generally plotted along a composition trend defined by the abyssal peridotites and the forearc mantle peridotites (Figure 2). The Yap Trench peridotites and the peridotites from the Izu–Bonin–Mariana (IBM) forearc have higher MgO contents and lower Al2O3 and CaO contents than those of the abyssal peridotites (Figure 2b,c). Compared with the IBM forearc mantle peridotites, the Yap Trench peridotites have extremely low CaO and relatively lower Al2O3. In the Al2O3/SiO2 versus MgO/SiO2 diagram (Figure 2d), the oceanic peridotites define a trend parallel to the terrestrial array, and the forearc mantle peridotites are plotted on the high MgO/SiO2 and low Al2O3/SiO2 ends. Two samples from the southern part of the Yap Trench have the most extreme compositions within the Yap Trench peridotites, which correspond to the most depleted and most fertile ends of the composition trend, respectively (Figure 2).
The Yap Trench peridotites show light rare earth element (LREE)-rich patterns in the chondrite-normalized diagram (Figure 3a). Sample JL149-S27-1 from the southern Yap Trench has a heavy rare earth element (HREE) content comparable to the average value of abyssal peridotites, while other samples have HREE contents similar to that of peridotites from the IBM forearc, which is plotted outside the HREE field of the abyssal peridotites. In the trace elements spider diagram (Figure 3b), the Yap Trench peridotites show a positive peak in Ba, U, and Sr with respect to the adjacent elements. In contrast, Ti shows negative anomalies in samples from the northern Yap Trench.

3.2. Re-Os Isotopes

Compositions of Re-Os elements and Re-Os isotopes are listed in Table 2. The Re content in Yap Trench peridotites has a narrow range of 0.06–0.24 ppb, which is slightly higher than that of the peridotite xenoliths from subduction zones [17] but is lower than the value of most abyssal peridotites (Figure 4a). Nearly all peridotites from the Yap Trench have an Os content of less than 1.5 ppb (0.30–1.26) and are plotted in the low Os end of the fields of both abyssal and subduction zone peridotites (Figure 4b); the exception is sample JL149-S03-1, which has a high Os content (4.18 ppb). The 187Os/188Os ratios of the Yap Trench peridotites vary over a wide range (0.12043–0.14867), with the highest value comparable to that of the dunite from mid-ocean ridge [44] and the lowest value comparable to the most unradiogenic Os isotope (0.11933) discovered in subduction zone peridotites [45] (Figure 4b). The most unradiogenic 187Os/188Os ratio occurs in sample JL149-S03-1, which has the lowest Al2O3 and CaO content and a relatively low rare earth element (REE) content among the Yap Trench peridotites. There are no obvious correlations between Os and 187Os/188Os of the oceanic peridotites; however, anomalously radiogenic values are limited to samples with Os content less than 2 ppb (Figure 4b). In general, the oceanic peridotites show a positive correlation between Al2O3 and 187Os/188Os, which represents a melt depletion trend. Some Yap Trench peridotites, however, show a trend that intersects with melt depletion trend, which is characterized by an increase in 187Os/188Os with a constant Al2O3 (Figure 5).

4. Discussion

4.1. Seawater and Fluid Alteration

As residues of mantle melting, peridotites are commonly used to detect information on the oceanic upper mantle beneath a mid-ocean ridge and subduction zone [27,38,39,47,48]. Unfortunately, most oceanic peridotites have been modified by secondary alteration processes such as serpentinization and sea-floor contamination [49,50,51], which results in ambiguity when discussing the deep mantle processes. The Yap Trench peridotites have high LOI (12.38–14.06) and show elevated concentrations of fluid mobile elements—such as U, Pb, and Sr—which represents characteristics resulting from serpentinization and seawater alteration of oceanic peridotites [38,48,51] and is consistent with the presence of serpentine, observed petrographically [27]; however, these modifications are generally thought to be restricted in elements that are highly mobile in fluid [38]. Most major elements seems unaffected by alteration processes, which is supported by the general correlations between major elements (Figure 2) and by the observation that the peridotites do not deviate significantly from the “terrestrial array” [41] in the Al2O3/SiO2–MgO/SiO2 diagram (Figure 2d). The slope of the trend defined by the Yap Trench peridotites is close to that of the terrestrial array, indicating that Al2O3 is not significantly modified by secondary processes.
Previous studies have suggested that the Re in peridotites is potentially elevated by alteration processes [7,9,52,53]; however, the Yap Trench peridotites have relatively lower Re values (0.06–0.24 ppb) compared to the value of the primitive mantle (0.34 ppb) and the abyssal peridotites (Figure 4a), implying that most of the Re was removed from the mantle and that there was no significant addition of Re to the peridotites after melting. As a compatible element, the Os content in the mantle will increase with the increase in the degree of mantle melting. The Yap Trench peridotites are characterized by high MgO and low Al2O3, CaO, and HREE content, indicating a high mantle melting degree. Thus, the highly depleted Yap Trench peridotites should have high Os content, which is inconsistent with the observation that most of them have lower Os values than abyssal peridotites do (1–5 ppb) (Figure 4b). This contrast indicates that Os in peridotites should have been affected by processes other than mantle melting. It has been suggested that mantle Os may be partly lost during seawater alteration [7], leading to lower Os concentrations in abyssal peridotites compared to orogenic lherzolites [4,54]. During the alteration processes in oxidizing conditions, sulfides—which are a major Os carrier in peridotites [54]—are not as stable as they are in less oxidizing regimes and may therefore be oxidized to sulfates [55]. In addition, Os will behave as a moderately incompatible element during alteration, which could possibly promote its mobility [4]. Considering that the Yap Trench peridotites have experienced varying degrees of seafloor weathering and serpentinization, it can be inferred that the low Os content and high Re/Os ratio in the depleted Yap Trench peridotites were partly affected by seawater alteration, at least for the three samples with Os content lower than 0.5 ppb and Re/Os content higher than 0.2 (Figure 4 and Figure 6).
Researchers have long debated whether seawater alteration could increase the radiogenic Os isotopes of oceanic peridotites [7,10,12,17,45,56]. Even though seawater has over six orders of magnitude less Os than peridotite, it is possible to significantly modify the Os isotopic composition of peridotites via seawater alteration because the 187Os/188Os in seawater is much higher than that in mantle (~1 compared to ~0.127 for the bulk Earth), which largely reduces the amount of added water needed to modify the Os isotopic composition in peridotites [7]. Modification of the 187Os/188Os ratio by the hydrothermal alteration and seafloor weathering of peridotites has been reported in several studies [7,17,44]. Some oceanic peridotites contain cracks filled with MnO2 or are covered by MnO2 rinds, which generally contain high concentrations (up to 3 ppb) of radiogenic Os [57]); thus, they may significantly increase the 187Os/188Os ratio of the peridotites [4,7,44,58,59]. There are several studies, however, suggest that the difference in 187Os/188Os ratio between weathered rims and fresh interiors of abyssal peridotites is small [10] and that the Os isotopic compositions in peridotites mainly record the information of high temperature mantle processes [12,18].
The Yap Trench peridotites have a wide range of 187Os/188Os ratios (0.12043–0.14867) and the highly radiogenic 187Os/188Os ratios seem to be affected by seawater alteration. Because there is no correlation between 187Os/188Os and the U (fluid mobile element) of the Yap Trench peridotites (Figure 7), alteration may not be the only process that account for the increasing of the 187Os/188Os ratio. However, samples with the most radiogenic Os have the highest U content and demonstrate significantly altered appearances in hand specimens (Dive 112-S04-1) (Figure 2b in Chen et al., 2019 [27]) and high LREE enrichment in REE patterns (Figure 3a), suggesting that the significant increase of radiogenic Os should be related to secondary alteration. Apart from alteration by seawater, peridotites from subduction zones also can be affected by slab-derived water-rich fluids; therefore, the recent addition of radiogenic Os from subducted oceanic crust and sediments may play a role in elevating the radiogenic Os content of the two highly altered samples [17,60,61]. This is supported by the subduction component addition trend in the 187Os/188Os vs. Al2O3 diagram (Figure 5), which is consistent with the addition of a component with high radiogenic Os and low A12O3 to the depleted mantle, as Al is sparingly soluble in the slab-derived water-rich fluids [62]. Modification of Os isotope compositions in the other six Yap Trench samples cannot be excluded because two of them have suprachondritic 187Os/188Os ratios; however, these samples show generally positive correlations in the 187Os/188Os vs. Al2O3 diagrams (Figure 5), indicating that alteration disturbance in Re-Os isotope systematics of these samples is not as strong as the two highly altered samples.

4.2. Melt Refertilization

Melt refertilization is very common in oceanic peridotites, leading to the enrichment of LREEs and other highly incompatible elements observed in abyssal peridotites [48,63] and peridotites from subduction zones [45]. The Yap Trench peridotites also show evidence of interaction between slab-derived melts and mantle wedges [27]. As the half-life of the 187Re decays to 187Os is about 42 billion years [1], there is significant divergence in 187Os/188Os ratios between basalts (0.125–0.23) and depleted mantle residue (0.12–0.13) [6]. However, Os concentration in basalts are two orders of magnitude lower than that of the mantle peridotites; thus, the Os isotopes of mantle peridotites are thought to be insensitive to late processes related to basaltic melts. Whereas in subduction zones, evidence for recycling of radiogenic Os from the subducted slabs to the mantle wedge have been widely reported [8,16]. The high halogen (i.e., Cl and F) contents and oxygen fugacities of the slab-released fluids or melts may convert Os into a mobile element in subduction zone environments [16,64]. Even though it is difficult to distinguish the contribution of fluids and melts in controlling Os isotopes, the highly radiogenic 187Os/188Os ratios in peridotites that sample the mantle wedge did confirm the disturbance of Os isotopes by slab-derived components [17,60,61,65,66].
The positive correlation between 187Os/188Os ratios and high field-strength elements (Nb and Zr) suggests that melt refertilization should play a role in increasing the radioactive Os isotopic composition of the Yap Trench peridotites (Figure 8). Melt refertilization has a negligible effect on the Os isotopic compositions of peridotites except when there is a high melt/rock ratio and low Os content in peridotites [12,16]. Some dunites from the Southwest Indian Ridge have highly radiogenic 187Os/188Os, which may be related to the high melt/rock ratio of the melt channels [44]. Additionally, low Os contents and radiogenic 187Os/188Os were also observed in ophiolite peridotites affected by penetrating melts under high melt/rock ratios [67]. As shown in Figure 4b, mantle peridotites can be divided into two groups; one group are characterized by low Os concentrations (<2 ppb) and variable Os isotopic compositions due to the occurrence of highly radiogenic 187Os/188Os ratios; another group are characterized by higher Os concentrations (>2 ppb) and unradiogenic 187Os/188Os ratios. Peridotites with extremely high 187Os/188Os ratios (>0.145) [12,44] generally have Os contents lower than 0.5 ppb (Figure 4b) implying that the primary unradiogenic Os should have been removed from the peridotites if melt refertilization did affect the Os isotope composition. Therefore, the Yap Trench peridotites should have been affected by penetrating melts under high melt/rock ratios, this is reasonable because tectonic erosion was enhanced by subducting of the Caroline ridge, thus more slab-derived melts were transported into the mantle wedge. During this process, the primary sulfides with unradiogenic Os were dissolved by the penetrating melts and secondary sulfides with radiogenic Os were segregated from the melts into mantle peridotites.

4.3. Ancient Melting Event

Studies of major and trace elements of peridotites have inferred that there may be old mantle fragments present in the oceanic asthenosphere [48,68], which has been confirmed by unradiogenic 187Os/188Os ratios recorded in abyssal peridotite [8,9,10,11,69], ophiolite peridotite [70,71], and forearc mantle peridotite [18]. This suggests that ancient melting events are ubiquitously recorded in the oceanic mantle. Nevertheless, when Os isotopes are considered, it should be ensured that they have not been significantly disturbed by secondary processes such as fluid alteration and melt refertilization. The correlation between Al2O3 content and the 187Os/188Os ratio is a useful proxy to evaluate whether the peridotites preserve magmatic information. Here, Al2O3 instead of Re/Os is used because rhenium is more likely to be affected by late processes than aluminum is. The positive correlation between Al2O3 and the 187Os/188Os ratio in peridotites was widely observed in orogenic peridotites [52], abyssal peridotites [10], and forearc mantle peridotites [18], and was thought to indicate that the peridotites are inherited from one or more melting events [11].
Previous sections have shown that the Os isotope in the Yap Trench peridotites have been modified by fluid alteration and melt refertilization, especially for three samples with high 187Os/188Os ratios that obviously deviate from the general trend of the oceanic peridotites (Figure 5). The other five samples show positive correlation between Al2O3 and 187Os/188Os ratio, implying that to some extent these samples preserve the signature of the melting events. However, compositional trend of these samples has a higher slope than that of the trend defined by the abyssal peridotites (Figure 5), which means that, for a given Al2O3, the subduction-related peridotites are shifted on average to a higher 187Os/188Os ratio. These features are consistent with the modification of the peridotites by late processes. Considering that the radiogenic Os will be increased by late processes, low 187Os/188Os ratios in the peridotite are more likely to record the true melting history. It is documented that the 187Os/188Os composition of the convecting upper mantle is related to both the melting degree and the melting age of the mantle [11]. Low 187Os/188Os ratios (sub-chondritic) in peridotites are indicative of a long-term evolution in a low Re-Os environment. Thus, the most unradiogenic Os isotopic composition of sample JL149-S03-1 may indicate that the peridotite is inherited from ancient melting events. The age of the melting event can be estimated by calculating the Re-depletion age (TRD), which assumes that all Re is extracted from the mantle during partial melting [72]. The TRD age represents the minimum ages of melt extraction because, in most cases, it is unlikely for all the Re to be removed from the mantle after melting. Thus, the TRD ages are closer to the true melting age in highly depleted peridotites than in less depleted peridotites. The TRD values (relative to chondrite) for the studied Yap Trench peridotites were calculated following the equation and parameters from Shirey and Walker (1998) [2] and Pearson et al. (2002) [46]. The results show that the melt extraction age is 0.24–1.16 Ga for the four unradiogenic (sub-chondritic) samples (Table 2). The wide range of the depletion age requires mantles with different evolution histories to be juxtaposed within the forearc mantle section. The maximum age (1.16 Ga) of the Yap Trench sample is comparable to the oldest age (0.82–1.23 Ga) that has been recorded in the IBM forearc mantle peridotites [18]. The beginning of the Yap subduction system was contemporaneous with and part of the formation of the IBM arc–trench system around 51–40 Ma [20,73,74], which means that, similar to the IBM forearc mantle [18], there may be episodic melting events in the Yap forearc mantle. This is supported by the observation that the oldest age occurs in the most depleted sample (JL149-S03-1), because a single melting event such as melting during the initiation of subduction [27] cannot account for the highly depleted peridotites with unradiogenic Os isotopes. It is documented that the asthenospheric mantle beneath the Philippine Sea Plate (PSP) has invaded into the forearc area of the southern Mariana Trench due to the shrinking of the PSP [32]. This large-scale asthenospheric flow may also have an impact on the Yap Trench, which is located to the south of the Mariana Trench, where slab gaps were inferred to induce mantle outflow from the shrinking PSP [32]. Thus, the Yap Trench peridotites may represent a residual mantle that experienced episodic melting events, including Proterozoic ancient mantle melting, back-arc mantle melting beneath the PSP, and mantle melting induced by forearc spreading at the earliest stage of subduction initiation [27].

4.4. Os Isotopic Heterogeneity in the Oceanic Asthenosphere

The wide range of the 187Os/188Os ratio in the Yap Trench peridotites indicates that the mantle wedge is heterogeneous in its Os isotopic composition. Peridotites from the southern Yap Trench plot in both the most depleted and fertile ends of the array of the studied samples (Figure 5), which reflects the coexistence of fertile mantle domains with relatively radiogenic 187Os/188Os ratios and refractory domains with unradiogenic 187Os/188Os ratios. The heterogeneity of the Os isotopic composition is inherited from both asthenospheric heterogeneity and lithospheric heterogeneity, which are mainly reflected by unradiogenic (sub-chondritic) and radiogenic (super-chondritic) Os isotopic composition, respectively. Lithospheric heterogeneity is more common and easier to identify than asthenospheric heterogeneity because the addition of radiogenic Os can be achieved by most late processes, and, meanwhile, the primary asthenospheric signals (unradiogenic Os) were blurred; therefore, the unradiogenic Os in the oceanic asthenosphere is underestimated based on the observations of oceanic peridotites, and the age of melt depletion reflected by 187Os/188Os ratios should be older than estimated.
As modification by late processes, including melt refertilization and fluid alteration, are common features in oceanic peridotites, the identification of asthenospheric heterogeneity is very important to establish the evolution history of the convecting upper mantle. A variety of studies have suggested that the asthenospheric mantle is heterogeneous in Os isotopes and that these heterogeneities can survive on long timescales (several billion years) in the convecting upper mantle [8,9,10,11,12,18]. A depleted mantle with unradiogenic Os making a great contribution to the heterogeneity of the asthenosphere indicates that the old mantle fragment is widespread in the asthenospheric mantle and was not homogenized by the convective stirring. This may be related to the contrast in density between the highly depleted and fertile mantle. The refractory old mantle fragment has a lower density [75,76] than the fertile mantle does and will therefore float above the “normal” asthenosphere, leading to high stability resisting mantle convection. The late processes may mask the primary mantle information and make it difficult to identify the ancient melting residue; thus, the amount of old mantle fragment is underestimated in the oceanic convecting mantle. Similar old mantle peridotites are also presented beneath the IBM forearc [18]. Therefore, the old depleted mantle domain, as a material that contrasts with isotopically enriched components such as recycled oceanic crust, may make a significant contribution to the chemical heterogeneity of the oceanic mantle.

5. Conclusions

The highly depleted Yap Trench peridotites are rich in LREEs and highly incompatible elements, implying that they were affected by late processes such as fluid alteration and melt refertilization. During these late processes, Os may become mobile and be removed from the mantle, leading to extremely low Os content in the depleted Yap Trench peridotites. Fluid alteration and melt refertilization also have increased the 187Os/188Os ratios of the mantle, resulting in a wide range of 187Os/188Os ratios (0.12043–0.14867, from sub-chondritic to suprachondritic) for the Yap Trench peridotites. As the 187Os/188Os ratio will be increased during late processes, the lowest 187Os/188Os ratio in the Yap Trench peridotites corresponds to a youngest Re-depletion age of 1.16 Ga (relative to chondrite), which undoubtedly indicates an ancient melting event. This Proterozoic ancient melting, combined with probable back-arc mantle melting beneath the Philippine Sea Plate and forearc mantle melting during the earliest stage of subduction initiation, indicates that the Yap Trench mantle has a complex evolutionary history.
The discovery of mantle with a low 187Os/188Os ratio in the subduction zone suggests that the amount and distribution area of old mantle fragment is underestimated in the oceanic mantle, which is probably due to the addition of radiogenic Os isotopes to the mantle during late processes. The refractory old mantle fragment has a lower density than the normal mantle does and will therefore float above the asthenosphere. Such fragments can be preserved in the convecting upper mantle for several billion years, which can make a great contribution to the heterogeneity of the oceanic asthenospheric mantle.

Author Contributions

L.C. and L.T. conceived and designed the concept of this study; L.C. and J.Z. wrote the original manuscript; X.L., W.W., Z.L., H.W., X.W. and F.C. have substantially revised the original manuscript.

Funding

This research was jointly funded by the Scientific Research Fund of the Second Institute of Oceanography, MNR (grant No. QNYC1901); the National Basic Research Program (973 Program) of China (grant No. 2015CB755905); the National Natural Science Foundation of China (grant No. 41706041; 41976072; 41706044; 91628301); the Natural Science Foundation of Zhejiang province, China (grant no. LQY18D060002); and the “13th Five-Year Plan” for Resources and Environment Projects of the China Ocean Mineral R&D Association (COMRA) (grant No. DY135-G2-1-01; DY135-N1-1-01).

Acknowledgments

We are grateful to two anonymous reviewers for their constructive comments.

Conflicts of Interest

The authors declare no conflict of interest.

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Minerals 09 00717 g001 550
Figure 1. Bathymetry and tectonic features of the studied area. Red box shows the location of the Yap Trench. Sampling locations (red circles) for Dive 112 (northern Yap Trench) and JL 149 (southern Yap Trench) are shown.
Figure 1. Bathymetry and tectonic features of the studied area. Red box shows the location of the Yap Trench. Sampling locations (red circles) for Dive 112 (northern Yap Trench) and JL 149 (southern Yap Trench) are shown.
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Figure 2. Plots of MgO versus (a) SiO2 and (b) Al2O3, (c) CaO versus Al2O3, and (d) Al2O3/SiO2 versus MgO/SiO2 of the studied Yap Trench peridotites (stars). Samples from the southern Yap Trench are shown by stars with green border. Concentrations have been recalculated to 100% on a loss on ignition (LOI)-free basis. The abyssal peridotites [38] and peridotites from the Izu–Bonin–Mariana forearc [39,40] are shown for comparison. The thick gray line in (d) represents the terrestrial array [41].
Figure 2. Plots of MgO versus (a) SiO2 and (b) Al2O3, (c) CaO versus Al2O3, and (d) Al2O3/SiO2 versus MgO/SiO2 of the studied Yap Trench peridotites (stars). Samples from the southern Yap Trench are shown by stars with green border. Concentrations have been recalculated to 100% on a loss on ignition (LOI)-free basis. The abyssal peridotites [38] and peridotites from the Izu–Bonin–Mariana forearc [39,40] are shown for comparison. The thick gray line in (d) represents the terrestrial array [41].
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Figure 3. (a) Chondrite-normalized rare earth element patterns and (b) a trace element spider diagram of the Yap Trench peridotites. JL149 samples are from the southern Yap Trench. Chondrite values are from Anders and Grevesse (1989) [42]. Fields for the abyssal peridotites [38] and the Izu–Bonin–Mariana forearc peridotites [39] are shown for comparison. Data for the depleted mantle (DM) are from Workman and Hart (2005) [43].
Figure 3. (a) Chondrite-normalized rare earth element patterns and (b) a trace element spider diagram of the Yap Trench peridotites. JL149 samples are from the southern Yap Trench. Chondrite values are from Anders and Grevesse (1989) [42]. Fields for the abyssal peridotites [38] and the Izu–Bonin–Mariana forearc peridotites [39] are shown for comparison. Data for the depleted mantle (DM) are from Workman and Hart (2005) [43].
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Figure 4. Plots of 187Os/188Os versus the (a) Re and (b) Os content of the Yap Trench peridotites. D, H, and L represent dunite, harzburgite, and lherzolite, respectively. The abyssal peridotites [7,9,10,11,12,44], the peridotite xenoliths from subduction zones [17], and the Izu–Bonin–Mariana forearc peridotites [18] are shown for comparison.
Figure 4. Plots of 187Os/188Os versus the (a) Re and (b) Os content of the Yap Trench peridotites. D, H, and L represent dunite, harzburgite, and lherzolite, respectively. The abyssal peridotites [7,9,10,11,12,44], the peridotite xenoliths from subduction zones [17], and the Izu–Bonin–Mariana forearc peridotites [18] are shown for comparison.
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Figure 5. Plot of 187Os/188Os versus Al2O3 content of the Yap Trench peridotites. Data sources are the same as in Figure 4. Samples from the southern Yap Trench are shown by stars with green border. The cyan field shows the general trend of typical oceanic peridotites. Solid arrows show the melt depletion trends for abyssal peridotites. Dashed arrows show the subduction component addition trend for the Yap Trench peridotites.
Figure 5. Plot of 187Os/188Os versus Al2O3 content of the Yap Trench peridotites. Data sources are the same as in Figure 4. Samples from the southern Yap Trench are shown by stars with green border. The cyan field shows the general trend of typical oceanic peridotites. Solid arrows show the melt depletion trends for abyssal peridotites. Dashed arrows show the subduction component addition trend for the Yap Trench peridotites.
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Figure 6. Plot of Re/Os versus Al2O3 content of the Yap Trench peridotites. Data sources are the same as in Figure 4.
Figure 6. Plot of Re/Os versus Al2O3 content of the Yap Trench peridotites. Data sources are the same as in Figure 4.
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Figure 7. Plot of 187Os/188Os versus U content of the Yap Trench peridotites. Data sources are the same as in Figure 4.
Figure 7. Plot of 187Os/188Os versus U content of the Yap Trench peridotites. Data sources are the same as in Figure 4.
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Figure 8. Plot of 187Os/188Os versus high field-strength elements (HFSE) (Zr and Nb) content of the Yap Trench peridotites. Correlation lines are drawn by linear fit.
Figure 8. Plot of 187Os/188Os versus high field-strength elements (HFSE) (Zr and Nb) content of the Yap Trench peridotites. Correlation lines are drawn by linear fit.
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Table
Table 1. Major element (wt. %) and trace element (ppm) concentrations in the bulk-rock peridotites.
Table 1. Major element (wt. %) and trace element (ppm) concentrations in the bulk-rock peridotites.
StationDive112-S04Dive112-S05Dive112-S0838III-Yap-JL149-S2738III-Yap-JL149-S03
Longitude138°29’46” E138°29’38” E138°28’44” E137°32’53” E137°33’14” E
Latitude9°51’56” N9°51’57” N9°52’8” N8°3’21” N8°3’18” N
Sample IDDive112-S04-1*Dive112-S04-2*Dive112-S05-1*Dive112-S05-2*Dive112-S08-1*Dive112-S08-2*38III-Yap-JL149-S27-138III-Yap-JL149-S03-1
Major element (wt. %)
SiO244.9644.9545.8145.7245.9546.1546.1245.59
TiO20.010.01----0.04-
Al2O30.310.330.640.650.360.471.620.08
TFe2O38.969.017.697.677.57.538.769.02
MnO0.150.150.090.090.060.060.120.11
MgO44.3844.4444.9844.6645.4645.3742.9744.67
CaO0.070.060.050.050.040.040.320.06
Na2O0.060.070.030.030.020.020.150.26
K2O0.010.010.01--0.010.020.01
P2O50.040.040.020.020.010.010.010.03
Sum98.9499.0599.3298.8999.499.66100.1299.85
LOI13.1613.3414.0613.7312.951312.3812.98
Trace element (ppm)
Sc3.893.816.16.076.06 9.283.83
Ti34.3732.577.076.245.71 --
V31.6631.6934.0832.534.65 39.2823.5
Cr21962466328030112763 25642639
Co97.6597.6172.9571.7988.73 95.16101.01
Ni22442212224722072305 21082133
Cu5.845.682.962.691.01 9.531.39
Zn48.8949.5936.1134.9543.85 40.5933.44
Cs0.00150.0010.00370.00420.0029 0.04770.0094
Rb0.08070.0670.10690.10590.0908 0.53240.1775
Ba1.53461.60850.68620.58940.597 2.26078.6628
Th0.020.01970.00080.00080.0024 0.0340.002
U0.88590.88360.65510.68560.5293 0.06650.7195
Nb0.18110.16930.0190.02170.0076 0.0360.0085
Ta0.00720.00650.01460.01350.0063 0.0110.0014
La0.17280.18440.04040.03760.0268 0.09820.0335
Ce0.31220.30130.02650.02390.0189 0.28950.0313
Pb0.09870.09130.17560.18160.3971 0.21690.0339
Pr0.03750.03430.0080.00850.0043 0.0360.0063
Sr4.724.512.392.351.55 4.556.12
Nd0.12470.13580.04430.04160.0193 0.14780.0436
Zr1.51741.82690.35240.52590.4541 1.23210.0702
Hf0.01350.02130.00830.01190.013 0.04870.0017
Sm0.0230.02690.00640.00870.0045 0.05990.0165
Eu0.00920.00930.0070.00520.0017 0.03140.0018
Gd0.03230.020.01380.01440.0032 0.10880.0065
Tb0.00490.00450.00220.0020.0006 0.05050.0003
Dy0.02650.02790.01250.01060.0025 0.14240.0054
Ho0.00640.0080.00370.00270.0009 0.03540.003
Er0.02420.01860.01380.01120.0045 0.11350.0067
Tm0.0030.00370.00220.00170.0008 0.02010.0018
Y0.21750.20570.17450.19570.0646 0.96210.1281
Yb0.02840.0290.01650.01390.0069 0.13360.0109
Lu0.0060.00630.00240.00260.0019 0.04880.0017
*: Major and trace element data from Chen et al. (2019) [27]. LOI: Loss on ignition. Major element concentrations have been recalculated on an LOI-free basis.
Table
Table 2. Re-Os element concentration and Re-Os isotope compositions of the Yap Trench peridotites
Table 2. Re-Os element concentration and Re-Os isotope compositions of the Yap Trench peridotites
Sample IDRe (ppb)2SEOs (ppb)2SE187Os/188Os2SE187Re/188Os2SETRD (Ga)
Dive112-s04-10.0955 0.0135 0.3327 0.0009 0.14867 0.00045 1.38558 0.19593 -
Dive112-s04-20.0870 0.0154 0.3705 0.0004 0.14707 0.00022 1.13424 0.20080 -
Dive112-s08-10.0835 0.0065 0.8909 0.0021 0.12542 0.00023 0.45125 0.03528 0.46
Dive112-s08-20.1060 0.0134 0.3023 0.0005 0.13189 0.00028 1.68912 0.21369 -
Dive112-S05-10.0855 0.0126 1.1081 0.0019 0.12702 0.00025 0.37162 0.05489 0.24
Dive112-S05-20.0642 0.0063 1.2622 0.0041 0.12641 0.00020 0.24505 0.02405 0.32
38III-Yap-JL149-S27-10.1595 0.0098 0.9054 0.0026 0.13198 0.00025 0.84898 0.05236 -
38III-Yap-JL149-S03-10.2399 0.0109 4.1797 0.0315 0.12043 0.00019 0.27608 0.01273 1.16
BIR-1a (reference material)0.6719 0.0147 0.3615 0.0007 0.13335 0.00022 8.95680 0.19633 -
TRD: Time of rhenium depletion age, calculated as: 1/λ*ln [(187Os/188Oschondrite –187Os/188Ossample)/187Re/188Oschondrite + 1] [2]. Calculating parameters are from Pearson et al. (2002) [46]. SE: Standard Error.

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Chen, L.; Tang, L.; Li, X.; Zhang, J.; Wang, W.; Li, Z.; Wang, H.; Wu, X.; Chu, F. Ancient Melt Depletion and Metasomatic History of the Subduction Zone Mantle: Osmium Isotope Evidence of Peridotites from the Yap Trench, Western Pacific. Minerals 2019, 9, 717. https://doi.org/10.3390/min9120717

AMA Style

Chen L, Tang L, Li X, Zhang J, Wang W, Li Z, Wang H, Wu X, Chu F. Ancient Melt Depletion and Metasomatic History of the Subduction Zone Mantle: Osmium Isotope Evidence of Peridotites from the Yap Trench, Western Pacific. Minerals. 2019; 9(12):717. https://doi.org/10.3390/min9120717

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Chen, Ling, Limei Tang, Xiaohu Li, Jie Zhang, Wei Wang, Zhenggang Li, Hao Wang, Xichang Wu, and Fengyou Chu. 2019. "Ancient Melt Depletion and Metasomatic History of the Subduction Zone Mantle: Osmium Isotope Evidence of Peridotites from the Yap Trench, Western Pacific" Minerals 9, no. 12: 717. https://doi.org/10.3390/min9120717

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