Jianite: Massive Dunite Solely Made of Virtually Pure Forsterite from Ji'an County, Jilin Province, Northeast China

: A rare massive yellowish-green serpentinized dunite, covering a minimum area up to ~50 m 2 , has been found in Ji ' an County, Jilin Province, Northeast China. It contains primary olivine and secondary serpentine (antigorite) and brucite. Other primary minerals like orthopyroxene, clinopyroxene, and aluminum-rich phase (such as garnet, spinel, and plagioclase), frequently appearing in ultramafic rocks, have not been identified. The olivine is essentially pure forsterite, with an Mg# (100 × Mg/(Mg + Fe)) of ~99.6–99.7. Due to these distinct features, we especially name the protolith of this dunite as jianite ( 集安岩 ). The forsterite grains range up to ~2 mm, show clear equilibrium textures such as nearly straight grain boundaries and ~120° dihedral angles at their triple junctions, and display no intragranular or intergranular composition variations. They are extensively ruptured and hydrated (i.e., serpentinized), with the fractures (and the grain boundaries as well) filled by fine-grained antigorite (ideally Mg 6 (Si 4 O 10 )(OH) 8 ) and brucite (ideally Mg(OH) 2 ). These secondary phases are also extremely poor in Fe, indicating a good chemical equilibrium with the forsterite. The serpentinization reaction may have proceeded as forsterite + fluid = antigorite + brucite at temperatures of ~425(25) °C and at relatively low but undetermined pressures. The fluid was likely a B-rich, but Si-poor dilute aqueous fluid, as implied by the trace element characteristics and water-related infrared features of the forsterites in equilibrium. The petrogenesis of the jianite is presently unclear.


Introduction
The ultramafic peridotitic upper mantle generally consists of olivine (Ol; (Mg,Fe)2SiO4), orthopyroxene, clinopyroxene, and an aluminous phase (plagioclase, spinel or garnet, depending on pressure). As it partially melts to generate basaltic magmas, it gradually turns into harzburgite and dunite, with the former containing olivine, orthopyroxene, and the aluminous phase (small amount), and the latter containing olivine and the aluminous phase (trace amount). Subject to the interior thermal state of the Earth, this partial melting process seldom goes beyond the elimination of orthopyroxene, so that a residual dunite is rarely generated [1,2]. Indeed, mantle xenoliths brought up by kimberlites and alkaline basalts are usually lherzolite and harzburgite [3][4][5] and only sparsely dunite [6,7].
As the partial melting process progresses, the constituent phases of the peridotite alter their compositions and become more refractory. High-P experiments and field observations suggest that the Mg# (100 × Mg/(Mg + Fe)) of the residual olivine increases from a typical mantle value of ~89 to ~95 [2,3,8,9], and the Cr# (100 × Cr/(Cr + Al)) of the residual spinel sharply increases from ~20 to over 80 [2,10,11]. Further, the magmas derived from this partial melting process are incapable of crystallizing at shallow depths more refractory olivine (with Mg# higher than that of the corresponding residual olivine in the source regions) due to the Fe-Mg partitioning equilibrium [12,13]. Consequently, natural olivine with Mg# > 96 is not typical for any igneous rocks in general [14]. Natural olivine crystals with nearly pure forsteritic composition (with Mg# > 96) were sometimes found as phenocrysts in some basalts and kimberlites [15,16], as inclusions in chromites from some podiform chromitite [17], and as one of the metamorphic minerals in the contact zone between an igneous rock and a carbonate rock [18][19][20]. Their genesis has been attributed to some special processes such as subsurface oxidation, subsolidus re-equilibration, and interaction with carbonates [14]. Additionally, narrow pseudomorphic olivine rims with Mg# > 96 were occasionally found surrounding primary olivine grains (Mg# = ~89-92) in some serpentinites, with their genesis ascribed to the serpentinization or deserpentinization reaction [21][22][23].
Here, we report a massive serpentinized dunite (occupying an area of at least up to ~50 m 2 ) from Ji'an County, Jilin Province, Northeast China. The protolith of this rock contains virtually pure forsterite (i.e., Mg# = ~100), which coexist with no other primary mantle phase. This type of lithology is extremely rare and has not been well characterized so far.

Sampling Location and Analytical Methods
The sampling area lies to the east of the Songliao depression and consists of four major tectonic terranes, the Ji-Hei orogenic belt, the Longgang block, the Liao-Ji Proterozoic rift zone, and the Langlin block ( Figure 1).

Figure 1.
Geological map of the sample-collecting area (after Qin et al. [24]; Zhou et al. [25]). The exact sample-collecting location is indicated by the white star (latitude N41°20'18", longitude E125°39'). The insert shows the major tectonic terranes in a much larger area. T-L fault refers to the Tancheng-Lujiang fault.
The rock documented here exposes in the Mayihe formation of the Ji'an group, which locates in the Liao-Ji Proterozoic rift zone. The Mayihe formation, a boron-bearing sequence with a deposition age of ~2126-1940 Ma [26], contains various altered felsic and granitic rocks, dolomitic marble, serpentinized olivine marble, and boron-and iron-bearing serpentinite, and amphibolite [24,27]. It has been proposed that some metavolcanic rocks of the Ji'an group formed at ~2189-2156 Ma and experienced an amphibolite facies metamorphic event at ~1881-1870 Ma [24]. Existing petrochemical and geochemical analyses of the altered volcanic rocks show the characteristics of the calc-alkali volcanic rocks of island arc, indicating the possible involvement of an ancient subduction process [28]. Recently, some ultra-basic rock blocks were found in the metamorphic sedimentary rocks of the Ji'an group [25].
The discovered outcrop of the serpentinized dunite locates near Jiayi Village, Caiyuan Town, Ji'an County, Jilin Province. The exposed body, with a yellowish weathered surface, is ~10-15 m long, ~4-5 m wide, and ~3-4 m high ( Figure 2). The rock contains olivine, serpentine (Serp), and brucite (Brc), and shows varying degrees of serpentinization. The relatively dark neighboring rock (Figure 2b) is of similar lithology but presumably has a different bulk composition (to be reported elsewhere). A large number of specimens were collected from the serpentinized dunite. Here, we have arbitrarily selected and subsequently processed four samples (JAY01, JAY02, JAY03, and JAY04) to investigate the basic petrological and mineralogical features. was coupled to a COMPexPro 102 laser-ablation system with a 193 nm ArF-excimer laser [31]. Helium was served as the carrier gas to enhance the transport efficiency of the ablated material. Each analysis comprised ~20 s background acquisition (gas blank) followed by 60 s data acquisition [32]. The beam was set to a diameter of ~60 μm with a repetition rate of 5 Hz and laser energy of 100 mJ. The NIST glass 610 was used as an external standard, the NIST glasses 612 and 614 were used as monitoring standards [33], and the 24 Mg content obtained by the EMP analyses was used as an internal standard. Homogeneous sections of the signals were selected to derive the results so that the influences of any potential inclusions and fractionations encountered by the laser beam could be removed. The final data reduction was carried out using the Glitter software package [34].
The water content of the olivine was examined by using a Nicolet iN10 MX IR Microscope, which was equipped with a high-energy Ever-Glo TM infrared source, a standard KBr beam splitter, and a liquid-nitrogen-cooled MCT detector at the High-Pressure Laboratory of Peking University [35,36]. Transmission IR spectra were collected on olivine crystals or fragments from a free-standing, doubly polished thin section. To make the thin section, the general preparing procedure outlined in Liu et al. [37] was followed. Firstly, a slice of rock cut off from the specimen JAY04 by using a low-speed diamond saw was placed on a glass slide with some crystal-bond, and subsequently reduced to a thickness of ~160 μm by using a series of silicon carbide abrasive papers. The thickness of the final rock thin section was determined by utilizing a digital micrometer, and the accuracy of the measurement was ~2 μm. Secondly, the rock thin section was thoroughly washed in acetone for 24 h to dissolve the crystal-bond, cleaned in ethanol for several times, and dried at ~110 °C for several hours. Thirdly, 11 clean olivine crystal plates (or fragments from different olivine crystals) with no discernible cracks or inclusions were manually picked up under an optical microscope, transferred and placed on a BaF2 sample holder, and analyzed by the FTIR. The spectra from 7800 to 675 cm −1 were recorded with an aperture of 50 × 50 μm 2 , 512 scans, and a resolution of 4 cm −1 . The data were processed by using the OMNIC8 software and PeakFit V4.12 software.

Petrography
The rock contains roughly 60% olivine, 30% serpentine, and 10% brucite, with olivine clearly as a primary phase and serpentine and brucite as secondary phases ( Figure 3). The olivine grains, often up to ~2 mm in diameter, are extensively fractured, with the fractures (and the grain boundaries as well) filled by fine-grained serpentine aggregates and brucite aggregates. This spatial arrangement obviously indicates the following hydration reaction (i.e., serpentinization reaction), olivine + fluid = serpentine + brucite (1) In general, the hydration zones along the grain boundaries of the olivines, with coarser serpentine and brucite grains, are wider than those in the fractures within the olivine grains, indicating a hierarchic fluid-transport system operating in the hydration process ( Figure 4). Both along the grain boundaries and in the fractures of the olivine grains, the serpentine aggregates, appearing as layers, often locate themselves next to the olivines and sandwich the layers of the brucite aggregates. This phenomenon might imply that, if both the Mg cations and the Si cations contained by the serpentines and brucites were from the olivines, the Mg cations would have diffused much faster than the Si cations in the fluid, leading to the crystallization of the serpentines near the olivines and the crystallization of the brucites slightly farther away. In addition, we expect that the serpentinization reaction should have hardly approached its completion due to the gradual isolation of the olivine grains from the fluid by the serpentine aggregates and brucite aggregates. The observed phase assemblage, olivine + serpentine + brucite + fluid, in the rock generally indicates a T of ~425(25) °C and a wide P range of ~0-10 kbar for the hydration reaction [38,39]. At this high T, the cation diffusion rates are generally fast, and the compositions of the olivines and serpentines can be adequately adjusted, leading to no precipitation of magnetite and no formation of hydrogen [40,41]. Indeed, no magnetite has been detected so far.
The textures of the protolith of this rock seemingly have escaped the hydration process at least to some extent. The severely hydrated olivines usually contain numerous tiny inclusions (presumably serpentines) likely appearing along some special but undetermined crystallographic orientations ( Figure 4a). In contrast, the less hydrated olivine grains are usually inclusion-free ( Figure 4b). Whatever the extents of the hydration reaction are, the initial crystallographic orientations of the olivine grains have been well preserved, as indicated by the almost identical extinction angles of the different fragments from the same olivine crystals (Figure 3b,d). Further, the initial equilibrium texture of the olivine grains seems also well preserved, as implied by the nearly 120° dihedral angels at the triple junctions ( Figure 3d).
Distinctly, orthopyroxene, clinopyroxene, garnet, spinel, plagioclase, and other minerals frequently encountered in the ultramafic rocks have not been found in the rock so far.

Phase Identification
The primary olivine has been identified as nearly pure forsterite (Fo) and the secondary serpentine as antigorite (Atg) by resorting to Raman spectroscopy. The identity of the secondary brucite has also been confirmed by our Raman data. No other phases have been suggested by the Raman spectra so far. , in which needle-shaped fine mineral inclusions align along certain special crystallographic orientation, shows relatively weak serpentinization. In comparison, the olivine grain in the upper left part of the image (broken down into several relatively large olivine fragments) shows relatively strong serpentinization, that in the upper right part (broken down into many relatively small olivine fragments) shows strong serpentinization, and that either in the left part or in the right part (completely replaced by serpentine and brucite) shows complete serpentinization. (b) A hierarchic fluid-transporting system displayed by grain boundaries and cracks of different widths (from > 60 to < 10 μm) near a ruptured olivine grain, which is filled with serpentine aggregates and brucite aggregates. The examined area is generally the lower left part of the sample shown in Figure 3c,d. In most cracks, two layers of serpentine aggregates, thick or thin, generally occur next to the olivines and sandwich a layer of brucite aggregates. In some cases, the serpentine aggregates and brucite aggregates may form interbedded thin layers and display complicated textures. (c) A close-up view of the serpentine aggregates and brucite aggregates along the grain boundary in the upper left part of (b). Note that the olivine grain is almost inclusion-free, suggesting a weak serpentinization reaction. Ol, olivine; Serp, serpentine; Brc, brucite.
Representative Raman spectra for the primary olivines investigated here are shown in Figure 5, along with a reference Raman spectrum of the synthetic forsterite from Liu et al. [29]. The most prominent Raman peaks of olivine are those two occurring in the spectral regions of 815-825 and 838-857 cm −1 . As the Mg# of olivine rises, they should both shift from low wavenumbers toward high wavenumbers, and respectively reach the wavenumbers of ~825 and 857 cm −1 for the forsterite composition [42,43]. Our Raman spectra show these two peaks, respectively, at ~824 and 857 cm −1 , suggesting that these olivines should have compositions close to the forsterite, i.e., with extremely low Fe.  [29]. The major Raman feature of the olivine is the two peaks occurring at ~815-825 cm −1 and ~838-857 cm −1 . To illustrate clearly, only one Raman spectrum is shown for each sample, although multiple Raman spectra have been collected.
Typical Raman spectra of the secondary serpentine phase are shown in Figure 6. They demonstrate a prominent peak at ~230 cm −1 , which is one of the characteristic Raman signals for antigorite [44][45][46]. In comparison, lizardite usually shows a Raman peak at a slightly higher wavenumber like ~233 cm −1 [47], ~234 cm −1 [48], or ~236 cm −1 [45], with a relatively low intensity [44]. The possibility of lizardite can thus be ruled out. Chrysotile may have a strong Raman peak at a similar wavenumber of ~231 cm −1 [47], which, however, mostly negatively correlates with the Al contents [45]. For Al-poor chrysotile, this Raman peak occurs at ~235 cm −1 [45]. Our serpentine contains no Al (with a chemical formula close to Mg6Si4O10(OH)8; to be shown later), and hence cannot be chrysotile. Briefly, our Raman data have identified the serpentine as antigorite. This conclusion is in agreement with all existing investigations. According to Evans [39,40] and Schwartz et al. [49], the stable serpentine polymorph at the P-T conditions of ~425(25) °C and ~0-10 kbar should be antigorite. Figure 6. Typical Raman spectra of the large serpentines (antigorites) from jianite. Note that the Raman spectra from different samples (labeled with the text next to the spectrum) are almost identical. To illustrate clearly, only one Raman spectrum is shown for each sample, although multiple Raman spectra have been collected.
Typical Raman spectra of the secondary brucite phase are shown in Figure 7, along with a reference Raman spectrum for brucite and one Raman spectrum for antigorite. Although the Raman spectra have been somewhat contaminated by neighboring antigorites because of the small grain size of the brucites, the characteristic Raman peaks of brucite can be clearly observed at ~279 and 443 cm −1 [50,51], confirming the identity of the brucite. Due to the small grain sizes of the brucite, its Raman spectra have been contaminated by nearby antigorites. To illustrate clearly, only one Raman spectrum is shown for each sample (labeled with the text next to the spectrum), although multiple Raman spectra have been collected.
Natural antigorite is relatively scarce [52] and usually contains significant amounts of Fe and Al [44,45]. As a result, no Raman data for any Fe-and Al-poor natural antigorite approximating the Mg6Si4O10(OH)8 composition has been reported. Reynard and Wunder [46] reported a Raman spectrum for a synthetic antigorite with the Mg6Si4O10(OH)8 composition, with many bands displaying small splitting, exhibiting shoulders, and being broad. Our antigorite has a composition close to the Mg6Si4O10(OH)8 formula, and its Raman spectrum should be very informative. Figure 8 shows the Raman spectra (for the intensity data see Supplementary Table S1).

Chemistry of Minerals
The EMP analyses, performed on the rims, the mantles, and the cores of some randomly selected olivine grains (or fragments), are summarized in Table 1. The distinct compositional feature of the primary olivine is an unusually high Mg#, ranging from ~99.67(3) at the rims to ~99. 64(1) at the cores so that these olivines are virtually homogeneous forsterites with extremely limited Mg-Fe variations ( Figure 9). In addition, these forsterites are likely slightly short in Si (i.e., less than 1 Si per formula unit), especially for their rims, implying a low SiO2 activity for the interacting fluid. Figure 9. Compositions of the olivines in jianite, plotted in the SiO2-MgO-FeO composition triangle (wt%). All analyses from different olivine grains (or fragments) from different specimens have been mixed together and grouped according to their relative analyzing positions (rim, mantle, or core). The cores have little Fe-Mg variation, but the rims attain some Fe-Mg variation. Overall, the Fe-Mg variation in the olivines is extremely small.  The LA-ICP-MS analyses, performed on the rims and the cores of some randomly selected olivine grains, are summarized in Table 2. The first feature shown by these analyses is that the olivines have very homogeneous trace element distributions. The second feature is that with the exceptions of B and P, all other analyzed trace elements have abundances much lower than those found in typical low-T mantle olivines, in residual mantle olivines after melt extraction to some degrees, or in cumulative olivines crystallizing from mafic magmas [53][54][55][56][57]. Consequently, we believe that the initial trace element characteristics of the olivines have been completely removed by an extremely Benriched aqueous fluid during the serpentinization process. Thirdly, the B contents of the analyzed olivine are unusually high, ranging from 1697 to 1804 wt ppm, implying that the fluid must have been extremely enriched in boron. This is hardly surprising since significantly elevated B contents were previously observed for some serpentinized materials from the Mayihe formation [28].  The EMP analyses of the antigorite and brucite are summarized in Table 3. It can be seen that the antigorite and brucite have negligible amounts of Fe, implying an excellent chemical equilibrium between them and the forsterite. If the analytical contamination by the brucite grains underneath is removed from the EMP analyses (Figure 10a), one should obtain the general chemical formula Mg6Si4O10(OH)8 for the antigorite. In comparison, the deduced chemical formula from the EMP analyses for the brucite is Mg(OH)2 ( Figure 10b).
Obviously, the extremely low Fe components in these minerals can be essentially ignored, and Equation (1) can be quantitatively approximated by 4Mg2SiO4 + 6H2O = Mg6Si4O10(OH)8 + 2Mg(OH)2 As ~40% olivine of the dunite was consumed (Figure 3), a substantial amount of aqueous fluid then must have presented the serpentinization process. As a result, all initial trace element characteristics of the olivine could have been effectively erased. We thus infer that the distinct trace element abundances and ratios of the olivine observed here could form some of the key signals to a fluid-mediated process with the presence of a large amount of aqueous fluid at relatively low P-T conditions (e.g., ~450 o C and a few kbar), particularly supplementary to those well-established compositional parameters for various processes in the mantle [58,59].    Table 3). The EMP analyses of the brucite may have suffered a beam-focusing problem, leading to much higher totals (the total of the anhydrous components should be close to ~69.1%).

Water in Olivine
The unpolarized IR spectra taken from the forsterite are shown in Figure 11. As can be seen in the figure, all the crystals (or fragments) contain some prominent water peaks, suggesting that all the olivines have been extensively hydrated. In addition, the IR spectra indicate that water in the olivine is incorporated as hydrogen defects rather than molecular water. Further, water homogeneously distributes in the olivine crystals, as reflected by the nearly identical intensities of the water peaks from the olivine rims and from the olivine cores (red curves versus black curves).
Using the olivine-specific calibration of Bell et al. [60], the water content in the olivine has been estimated as 1450(300) wt ppm. Although it is not clear whether or not all the 11 analyzed olivine crystals or fragments were from different olivine grains with different orientations, we are sure that they were from at least three arbitrarily selected crystals. The water content then has been constrained to good accuracy (better than 25%) [61]. Figure 11. Unpolarized infrared spectra of the forsterite in jianite. Each pair of IR spectra is from one forsterite crystal (or fragment), with the spectrum in black representing the central position and the spectrum in pink representing the rim position. Numbers next to the IR spectrum is the integrated absorbance for the region 3750-3200 cm −1 , with the numbers in the parentheses representing one standard deviation (294 (15) read as 294 ± 15).
All the IR spectra have been carefully deconvoluted, with one example shown in Figure 12. There are 13 strong water peaks at ~3639, 3631, 3623, 3611, 3599, 3590, 3581, 3567, 3556, 3538, 3523, 3483, and 3420 cm -1 , and eight less intense water peaks at ~3645, 3507, 3475, 3443, 3405, 3384, 3348, and 3328 cm -1 . In general, the water peaks in olivine can be roughly divided into two groups: Group I in the range of ~3650-3450 cm −1 and Group II in the range of 3450-3200 cm −1 , with the former indicating hydrogens associating with Si vacancies and the latter suggesting hydrogens attributable to Mg vacancies [62][63][64]. Clearly, the Group I water peaks of our olivine are very strong while the Group II water peaks are very weak ( Figure 12) so that our olivine must contain significant amounts of Si vacancies, in good agreement with the composition data obtained from our EMP analyses (Table 1). Hence, the fluid that hydrated the olivine must have had a low silica activity.
Notably, the IR spectra of our olivine contain a distinct water peak at ~3538 cm -1 , which has been assigned to some boron-related defects (B 3+ + H + = Si 4+ ) by Matsyuk and Langer [65]. Indeed, our olivine is boron-rich (Table 2).

Figure 12.
Gaussian-Lorentzian deconvolution of the OH infrared peaks of the forsterite in jianite (the 3750-3200 cm −1 region). We used the PeakFit V4.12 software (SPSS Inc.) to process the IR data. The detected 21 Gaussian-Lorentzian peaks (the black curves) can be roughly divided into two groups, Group I in the range of ~3650-3450 cm −1 and Group II in the range of ~3450-3200 cm −1 . The sum (the red curve) of the 21 component peaks agrees well with the raw data (the blue curve) for the most data range.

Discussion: Jianite and Its Petrogenesis
The protolith of the serpentinized dunite reported here is unusual. As depicted above, the rock contains no other primary minerals such as orthopyroxene and clinopyroxene but olivine. Further, the olivine is virtually forsterite with little iron. According to Huang et al. [41,66] and Evans [40], the serpentinization process is not very efficient in removing Fe from the system. This is presumably partially because the end part of the hierarchic fluid-transport system is readily clogged due to the continuous volume expansion as the process advances [52], and partially because the serpentinization process takes place at very low T (here at ~425(25) °C). The same should be true for other major elements like Al and Ca. If the protolith had contained some other primary minerals like orthopyroxene and clinopyroxene, the Al and Ca hosted by these minerals should have been retained in the rock and easily detected by our analyses. Consequently, we tend to believe that the protolith was entirely made of forsterite. On this ground, we would like to coin the word "jianite" (集安岩) to emphasize this lithology, with Jian after Ji'an (集安), the name of the county where we collected our specimens.
The jianite found in Ji'an County is distinct from nearly all conventional dunites. To the best of our knowledge, the closest example to the jianite, in terms of phase assemblage and phase composition, is the dunite xenolith QX-18 from Qixia, North China Craton, which consists entirely of mosaic textured olivine with an Mg# of 98 [7]. However, the size of that dunite xenolith is mostly ~2-5 cm only, and the olivine grains might be coarser (presumably larger than a few mm). In comparison, the jianite reported here occupies a vast area of at least up to ~50 m 2 and contains relatively fine-grained forsterite (~2 mm in size).
The petrogenesis of the monomineralic jianite is unclear and so is that of the dunite xenolith QX-18. The dunite xenolith QX-18 was brought up by the 9-18 Ma Qixia nephelinites, along with other relatively fertile peridotitic xenoliths of young formation ages (Mesozoic or younger) [7]. Since there is not any good means to date the forsterites (Personal communication with Prof. Weidong Sun), it remains at least a possibility that this xenolith might represent the ancient and refractory lithospheric mantle of the North China Craton. In analog to this speculation, we propose that the jianite reported here might stand for the ancient and refractory lithospheric mantle of the North China Craton as well, which was somehow transported into the Liao-Ji Proterozoic rift zone. Along with other rocks in the Mayihe formation of the Ji'an group, the jianite might have experienced the regional amphibolitegranulite facies metamorphic event at ~1881-1870 Ma [24,67], being serpentinized by a B-rich, Si-poor aqueous fluid potentially originating from the dehydration process of a subducted slab [28]. The relatively small grain size of its forsterite (up to ~2 mm) remains to be explained though.
Another potential process that could have led to the formation of the jianite is that the forsterite might have quickly crystallized at relatively low temperatures from a special hydrous magma with its anhydrous components close to the forsterite composition [38]. If this scenario were correct, the quick crystallizing process could be used to explain the relatively small grain size of the forsterite. However, how and where such a hydrous magma could be geologically generated are presently beyond the reach of our cognition.
Other processes leading to the formation of nearly pure forsterite include serpentinization/deserpentinization of dunites and silicification of dolomite [18][19][20][21][22][23]. However, there has not been any mechanism to concentrate thus-formed forsterite grains to form a massive monomineralic rock like the jianite reported in this study. Minerals such as spinel, magnetite, dolomite, and calcite usually appear along with the forsterite.
With a rather uncertain petrogenesis, the jianite, i.e., massive dunite solely made of pure forsterite, may have some implications to the geochemical, geophysical, and geodynamic processes of the Earth. For example, it may affect the geodynamic process of subducted slabs, as implied by the stable/metastable phase relations of forsterite and the corresponding variations of the physical properties like density and sound velocity of forsterite and its polymorphs at typical subduction zone P-T conditions [68][69][70]. It is certain that much remains to be probed.