Feature Gems & Gemology, Winter 2021, Vol. 57, No. 4

Gemological Characterization of Peridot from Pyaung-Gaung in Mogok, Myanmar

Faceted peridot from the Pyaung-Gaung mine in Mogok
Figure 1. Left: Five faceted peridot samples from the Pyaung-Gaung mine in Mogok, Myanmar, weighing 5.18–7.52 ct, were examined in this study. Right: This 15.0 × 16.9 × 6.5 mm rough crystal showing a rhombus-shaped tabular habit and rounded faces, with minor white carbonate and talc, is also from the Pyaung-Gaung mine. Photos by T. Sripoonjan.


The Pyaung-Gaung area in the Mogok township of Myanmar is one of the essential sources of high-quality peridot for the international gem trade. Pyaung-Gaung peridot possesses an attractive deep olive green color and can be found in large sizes (>10 ct) in the market. It has long been mined from ultramafic rocks, largely dunite, at a primary deposit near Bernard-Myo. Internal features consist mainly of circular decrepitation halos (“lily pads”), fluid inclusions, and fiber tufts. Common mineral inclusions are dark biotite-phlogopite and chromite, sometimes coexisting with serpentine, magnesite, chlorite, and talc. Pyaung-Gaung peridot also contains olivine inclusions not previously found in peridot from other locations. 2D and 3D cross-plots of the trace element contents of Cr, V, Co, Sc, Ni, and Ti provide helpful separations among Burmese, Chinese, and Pakistani localities.

Peridot is a gem-quality variety of the mineral forsterite. It belongs to the olivine group, an isomorphous series whose main members are forsterite (magnesium silicate, Mg2SiO4), fayalite (iron silicate, Fe2SiO4), and tephroite (manganese silicate, Mn2SiO4) (Sinkankas et al., 1992; Deer et al., 2013). It crystallizes in the orthorhombic system with a rhombus-shaped habit (figure 1, right). In general, peridot yields a range of colors, including pale yellowish green to deep green, greenish brown to brown, and rarely brown with a dull, vitreous/greasy luster. The most desired and valuable color is saturated green without any tinge of yellow or brown. The green color is caused by iron content (Fe2+) within the structure.

Among the major modern localities, the primary sources of peridot are peridotite xenoliths in alkali basalts (United States and China) (Shen et al., 2011) and serpentinized dunites showing recrystallized olivine in tension gashes in sheared dunite bodies (Pakistan) (Bouilhol et al., 2015). Several articles have presented geological and mineralogical data for gem peridot deposits worldwide, including Zabargad (Egypt), Arizona (United States), Mogok (Myanmar), Yiqisong (China), Kohistan (Pakistan), the Central Highlands of Vietnam, and localities in Ethiopia and Tanzania (Gübelin, 1981; Jan and Khan, 1996; Fuhrbach, 1998; Thuyet et al., 2016). Other studies have focused on peridot’s gemological, chemical, and spectroscopic characteristics (e.g., Stockton and Manson, 1983; Koivula and Fryer, 1986; Fritsch and Lulzac, 2004; Adamo et al., 2009; Bouihol et al., 2015; Surour, 2018; Sripoonjan et al., 2019; Zhang et al., 2019).

Mogok is well known as one of the single most important sources of high-quality ruby, sapphire, and spinel (Kane and Kammerling, 1992; Waltham, 1999). But Mogok is also a significant supplier of large, fine peridot to the global gem trade. Mogok peridot has been known since the fifteenth century (Iyer, 1953). Its intense green is quite distinct and sometimes comparable to that of Pakistani peridot, but with a slight difference in clarity. Much of the finest-color peridot comes from Myanmar and Pakistan (GIA, n.d.).

The peridot mines at Mogok lie in the Pyaung-Gaung, Htin-Shu Taung, and Bernard-Myo areas (Thu and Zaw, 2017). Of these, the Pyaung-Gaung mines produce the finest color and largest sizes. Pyaung-Gaung peridot is typically yellowish green, while the highest-quality stones possess a rich olive green color (figure 1). Harlow and Thu (2014) studied samples in peridotite rocks from Pyaung-Gaung and compared them with those from the original Sapat deposit of Pakistan and the ancient Zabargad Island deposit of Egypt. They suggested that Mogok peridot was recrystallized in a cavity containing hydrous fluid of olivine, with the help of Earth’s tectonic activity. However, no insight into the gemological characteristics of peridot from Mogok has been widely available.

In May 2019, two of the authors (MS and TS) had the opportunity to visit the Pyaung-Gaung mine, where they witnessed the mining process, collected firsthand information, and briefly examined olivine samples on-site. The first sample group (five faceted stones and ten pieces of larger rough) was purchased from miners in the area, and additional samples were obtained through various marketing channels in Mogok. The present article provides an update on the Pyaung-Gaung peridot deposit.

Map of the Pyaung-Gaung peridot deposit
Figure 2. The Pyaung-Gaung peridot deposit is located in Bernard-Myo, north-northwest of Mogok township. Modified after Thu (2007), Themelis (2008), and Kan-Nyunt et al. (2013).


Mogok is known as one of the world’s oldest and most famous gem sources. The gem-rich area of Mogok (also known as the “Mogok Stone Tract”) is located in Kathe District of Upper Burma, 200 km northeast of Mandalay (Kyaw Thu, 2007). The area is situated in the central part of the Mogok Metamorphic Belt (MMB), which is composed mainly of rocks such as marble, gneiss, quartzite, and calc-silicate, as well as various types of igneous rocks from felsic to ultramafic (Iyer, 1953; Phyo et al., 2019). The complex structure involving folds and faults indicates that Mogok has been subjected to several major tectonic processes over extended periods of time, and this yielded a wide range of mineral assemblages and gem materials (e.g., ruby, sapphire, peridot, and spinel) that are the result of magmatic/metamorphic events in the area (Kane and Kammerling, 1992) (figure 2). Mogok has been mined for gemstones from both primary deposits (underground and open pits) and secondary deposits (in alluvial and eluvial placers).

Photos from the Pyaung-Gaung peridot deposit
Figure 3. A: Mountains in the Pyaung-Gaung area. B: A mining site at the primary deposit in Pyaung-Gaung. C: A pit dug into the peridot-rich area of the peridotitic host rock. D: Serpentinized fine-grained dunite, the precursor host rock of gem-quality peridot, was abundant around the mine. Photos by T. Sripoonjan.

The Pyaung-Gaung peridot mining area is located approximately 10 km north-northwest of the town of Mogok (again, see figure 2) and situated on a ridge along Taung Me Mountain, the highest mountain in the Mogok metamorphic complex, underlain by large granitic intrusives of biotite microgranite (Kabaing) (Iyer, 1953; Harlow and Thu, 2014; Sripoonjan et al., 2017). Kyaw Thu (2007) suggested that the Kabaing granite intruded into the peridotite at Pyaung-Gaung, indicating the possible emplacement of ultramafic rocks during the early Jurassic and generally earlier than the Mogok Metamorphic Belt. However, peridot from Pyaung-Gaung is derived from ultramafic rocks that occurred as a layered intrusion in the associated garnet-biotite gneiss (Kabe). The area has been mined mainly for fine-quality peridot in the outcrops of precursor dunite, an olivine-dominant variety of peridotite, as this rock was commonly present around the mine area. Nevertheless, well-formed crystals are usually found in veinlets and pockets within fine-grained serpentinized peridotites (Kyaw Thu, 2007), partly due to recrystallization of olivine in tension gashes or tectonic fractures during lateral displacement and uplift along the Momeik fault (Lin, 2014; Bouilhol et al., 2015; Thu and Harlow, 2017) (figure 3).

Mining at the Pyaung-Gaung peridot deposit
Figure 4. A: Miners entering the tunnel of an underground mine at the Pyaung-Gaung peridot deposits. B: A miner drills the rock along the tunnel wall with a pneumatic hammer to extract the peridot samples. C: Miners working in the main tunnel. Photos by M. Seneewong-Na-Ayutthaya (A) and T. Sripoonjan (B and C).

Traditional mining methods are used at the Pyaung-Gaung peridot deposits. The rock along the hillside is drilled with a jackhammer and blasted off with dynamite. This results in an extensive network of tunnels, generally 3–5 m wide and extending inward or downward to more than 50 m deep. Within the tunnels, the miners use a pneumatic hammer or primitive tools such as hammer and chisel to extract peridot embedded in the partially serpentinized dunite host rock along the tunnel walls. An electric generator is used for lighting and power tools (figure 4). A mine cart and rope system transports the mined material and equipment out from the tunnels. For safety reasons, we were not allowed to see the in situ samples after the fresh exposure of rock was cut open. However, the rough peridot is typically extracted and collected from the mines, followed by cleaning, cutting, and polishing locally in the town of Mogok before entering the gem markets.

The Pyaung-Gaung peridot rough samples from the study
Figure 5. The 28 Pyaung-Gaung peridot rough samples, 1.78–29.02 ct, collected and examined for this study. Photo by T. Sripoonjan.


Samples. All together, 33 peridot samples from the Pyaung-Gaung area were collected and used for this study. These consisted of five faceted stones weighing from 5.18–7.52 ct each (again, see figure 1) and 28 pieces of rough stones from 1.78–29.02 ct each (figure 5). The rough stones were divided into two groups: 10 larger stones purchased directly from a local miner and 18 smaller ones from a reliable supplier in the town of Mogok. All faceted stones and larger rough stones had a rich olive green color; the smaller ones were yellowish green. All of the rough stones were cut and polished with a Facetron faceting machine to have two parallel windows (regardless of orientation) for gemological and spectroscopic investigation. Standard gemological instruments were used to measure refractive indices (RIs), specific gravity (SG), pleochroism, and fluorescence reaction to long-wave (~365 nm) and short-wave (~254 nm) ultraviolet lamps. In addition, this study used GIT-GTL peridot reference samples for elemental comparison and discrimination. These reference samples comprised 15 Pakistani peridots obtained from highly trusted traders from Pakistan and 26 Chinese peridots provided directly by Yanbian Fuli Olivine Mining Co., Ltd. of China. The GIT-GTL reference samples all ranged in size from 1.60 to 9.80 ct.

Microscopic Analysis and Spectroscopy. Internal features and photomicrographs were observed at 10×–75× magnification with a Zeiss Stemi 508 standard binocular gemological microscope attached to a Canon EOS 5D Mark III digital camera. Incident, darkfield, reflected, and oblique illumination techniques were employed to investigate internal characteristics. A polarizing filter was used to reduce the doubling effect from the birefringence of peridot.

A Renishaw inVia Raman microscope with a 532 nm laser was used for identifying mineral inclusions in the samples. Raman spectra were collected in the range of 1500–200 cm–1. The laser output power was 45 watts, and the spot size was 1.5 μm. The exposure time per scan was 10 s. The mineral inclusions were identified and compared with the RRUFF and Renishaw mineral databases through Thermo Scientific’s Spectral ID software. Unoriented ultraviolet/visible/near-infrared (UV-Vis-NIR) spectra were collected from 350 to 1500 nm with a PerkinElmer Lambda 1050 spectrophotometer using a data interval of 3 nm and a scan speed of 405.07 nm/min operating with a 150 integrating sphere accessory. Fourier-transform infrared spectroscopy (FTIR) was carried out using Thermo Scientific Nicolet iN10 FTIR microscope (mid-IR spectra, 1200–500 cm1) in reflection mode at 4 cm–1 resolution and 128 scans.

Chemical Analysis. Quantitative chemical composition was analyzed by an electron probe micro-analyzer (EPMA), JEOL model JXA-8100. The analyses were carried out with an accelerating voltage of 15 kV and beam current of 25 nA, using a focused beam (smaller than 1 μm). Measurement times were set at 10 s for both the peak and background counts of all analyzed elements, leading to an empirical detection limit of about 0.005 wt.%. For quantitative analyses, most of the standards used for calibration were pure oxide and mineral standards, including quartz for Si, periclase for Mg, manganosite for Mn, nickel oxide for Ni, fayalite for Fe, and wollastonite for Ca.

Laser ablation–inductively coupled plasma–mass spectrometry (LA-ICP-MS) was applied to analyze the trace element concentrations, using a Thermo Scientific iCAP RQ series ICP-MS coupled with an Elemental Scientific Lasers NWR-213 Nd:YAG laser ablation system. The laser employed a 10 Hz pulse rate and 55 μm diameter spot size. The energy density was about 9 J/cm2. Ablation was carried out in a He atmosphere, and the sample gas was mixed with Ar before entering the plasma. The gas background for pre-ablation was measured for 30 s to remove surface contamination, followed by a measurement time of 60 s and an elapsed interval time of 30 s. NIST-SRM 610 and 612 glasses reference materials were used as the external calibration standards (Jochum et al., 2011). Data reduction was carried out using Thermo Scientific’s Qtegra Intelligent Scientific Data Solution software to analyze the following elements: Li, Be, B, Na, Mg, Al, Sc, Ti, V, Cr, Mn, Co, Ni, Cu, Zn, Rb, Sr, Y, Zr, Nb, Cs, Ba, Hf, Ta, Th, U, Pb, and the rare-earth elements from La to Lu.

Table 1. Summary of gemological properties of peridot from Pyaung-Gaung, Mogok.


Gemological Properties. The gemological properties of the 33 studied stones are summarized in table 1. Again, the colors were rich olive green for the faceted and larger rough samples and yellowish green for the smaller samples. All of the samples were transparent. RI and birefringence values fell in the range of 1.648–1.689 and 0.030–0.041, respectively. SG varied between 3.24 and 3.36. The samples showed weak to moderate pleochroism in green and yellowish green. All were inert to both long-wave and short-wave UV radiation.

Internal features of Pyaung-Gaung peridot
Figure 6. Internal features of Pyaung-Gaung peridot. Left: A typical lily pad inclusion with a black chromite crystal in the center surrounded by a decrepitation halo; field of view 2.8 mm. Right: Typical discoid fissures around tiny inclusions; field of view 5.6 mm. Photomicrographs by M. Seneewong-Na-Ayutthaya.

Microscopic Characteristics. One of the most common inclusions of the Pyaung-Gaung peridot was the so-called lily pad (figure 6). These are round to oval-shaped decrepitation halos surrounding dark chromite or other mineral inclusions.

Internal features of Pyaung-Gaung peridot
Figure 7. Internal features of Pyaung-Gaung peridot. Left: A dark octahedral chromite crystal; field of view 1.8 mm. Right: An isolated octahedral chromite crystal surrounded by tension fractures; field of view 2.2 mm. Photo­micrographs by M. Seneewong-Na-Ayutthaya.

Other common inclusions were opaque black octahedral chromite crystals, sometimes containing tension fractures oriented in three dimensions (figure 7), similar to those previously noted in peridot from the United States and China (Koivula, 1981; Koivula and Fryer, 1986; Sripoonjan et al., 2019; Zhang et al., 2019).

Internal features of Pyaung-Gaung peridot
Figure 8. Internal features of Pyaung-Gaung peridot. A and B: An olivine crystal surrounded by partially healed fractures in a peridot host; field of view 3.8 mm. C–E: Olivine crystal inclusions in a peridot host; field of view 7.5 mm. F: Cluster of olivine crystals with wispy or smoky veils along with partially healed fractures; field of view 7.5 mm. Photomicrographs by M. Seneewong-Na-Ayutthaya.

Moreover, most of the samples contained abundant small olivine inclusions that have not been reported in peridot from other locations (figure 8). Some olivine crystals were surrounded by partially healed fissures (figure 8, A and B). One of the included crystals was cut open on the surface of the host peridot and identified by Raman spectroscopy and subsequent EPMA and LA-ICP-MS analyses (see figure 15 and the Chemical Composition section below).

Careful observation showed that the external shapes of the olivine inclusions were partly resorbed, probably due to the change of environment during the host’s crystallization (Harlow and Thu, 2014; Patil et al., 2017; Thu and Harlow, 2017). As such, these olivine inclusions could be crystals from an earlier generation incorporated into the peridot host, making them “protogenetic” inclusions (Gübelin and Koivula, 2005). These protogenetic olivine inclusions may be considered a diagnostic characteristic of Pyaung-Gaung peridot.

Internal features of Pyaung-Gaung peridot
Figure 9. Internal features of Pyaung-Gaung peridot. A: Unidentified flat crystals (probably phlogopite-biotite micas) of various sizes; field of view 3.8 mm. B: A rutile inclusion; field of view 1.8 mm. C: Inclusions of magnesite, serpentine, and talc (the inclusion in the center was cut open and identified by Raman spectroscopy); field of view 2.2 mm. Photomicrographs by M. Seneewong-Na-Ayutthaya
Mineral inclusions in Pyaung-Gaung peridot
Figure 10. An assemblage of mineral inclusions comprising chromite, magnesite, and chlorite, surrounded in part by serpentine; field of view 5.6 mm. Their Raman spectra were used to prove the mineral species. Photomicrograph by M. Seneewong-Na-Ayutthaya.

Some solid inclusions occasionally found in these samples appeared to be biotite-phlogopite micas (figure 9A) and rutile (figure 9B), as well as secondary magnesite, serpentine, and talc (figure 9C). In addition, an inclusion assemblage of chromite, secondary magnesite, and chlorite surrounded by white serpentine was found in one sample (figure 10). Except for the biotite-phlogopite micas, all were identified by Raman spectroscopy.

Chromite is often found within olivine-rich cumulates and occurs as small grains in ultramafic rock associated with serpentine, talc, and magnesite (Barnes, 1998; Salem et al., 2012). Some metamorphisms can also produce predominantly chlorite in association with talc (Sharp and Buseck, 1988). The presence of serpentine is commonly referred to as a hydration reaction (serpentinization) that occurred when olivine was infiltrated by aqueous fluids, while talc and magnesite were produced through a carbonation reaction when carbon dioxide (CO2) was present (Kelemen and Hirth, 2012; Lafay et al., 2018). The combined hydration and carbonation processes could be an indication of retrograde alteration in these Mogok peridot as the result of tectonic movements (Jan and Khan, 1996; Kelemen and Hirth, 2012; Bouilhol et al., 2015; Tzamos et al., 2020).

Tufts of very fine fibers in a Pyaung-Gaung peridot
Figure 11. Tufts of very fine fibers (probably chrysotile) in a Pyaung-Gaung peridot; fields of view 1.8 mm (left) and 3.8 mm (right). Photomicrographs by M. Seneewong-Na-Ayutthaya.

In faceted samples, low magnification commonly revealed unidentified tufts of very fine fibers (probably chrysotile; G. Harlow, pers. comm., 2021) that resembled black needles (figure 11).

Internal features of Pyaung-Gaung peridot
Figure 12. Internal features of Pyaung-Gaung peridot. A: A tiny crystal surrounded by super­imposed partially healed fractures; field of view 9.0 mm. B: Partially healed fissures showing a fingerprint-like attribute; field of view 5.6 mm. C: A typical healed fracture; field of view 4.5 mm. D: Fluid-like inclusions; field of view 1.8 mm. E: Needle-like inclusions with an iridescent effect; field of view 2.8 mm. Photomicrographs by M. Seneewong-Na-Ayutthaya.

Healed fissures (figure 12, A–C) and fluid-like inclusions (figure 12D) were regularly present and exhibited wide variation in appearance. Burmese peridot, as a product of partial metamorphism, has undergone recurring inner damage during the growth process. As a result, healing fissures and fluid-like inclusions formed within it from the process of continuous repair in the crystal itself during the recrystallization process (Gübelin and Koivula, 2004). Unfortunately, these inclusions could not be identified by Raman spectroscopy. Also observed in the Pyaung-Guang peridot were needle-like inclusions (figure 12E) showing an iridescent effect in reflected light.

Non-polarized UV-Vis-NIR spectrum of Pyaung-Gaung peridot
Figure 13. This representative non-polarized UV-Vis-NIR spectrum of Pyaung-Gaung peridot is characterized mainly by Fe2+ absorption features.

Spectroscopy. UV-Vis-NIR Spectra. The UV-Vis-NIR absorption spectra of the Pyaung-Gaung peridot samples all showed similar patterns, as illustrated in figure 13. The absorption coefficient (α) was calculated from the true absorbance in an uncorrected absorbance (A) and the thickness (t) of the sample in centimeters, according to the equation below (Dubinsky et al., 2020):

α =2.303A/t

The figure 13 spectrum displays a broad absorption band peak at 1050 nm, a shoulder at about 864 nm in the near IR, and additional weak bands at 381, 402, 453, 495, and 633 nm. The gradual increase in absorption from the visible to the UV region allows a broad transmission window minimum at around 560 nm, giving rise to the green coloration of the stone. The absorption feature of this Burmese peridot is usually attributed to Fe2+, which is a main chromophore contributing to the green color. This spectroscopic feature is also observed in peridot from other localities (e.g., Adamo et al., 2009; Thuyet et al., 2016; Sripoonjan et al., 2019).

Representative FTIR spectrum of a Pyaung-Gaung peridot
Figure 14. A representative FTIR spectrum obtained from a Pyaung-Gaung peridot. All the marked absorption bands are related to internal Si-O vibrations (Burns and Huggins, 1972).

FTIR Spectra. A representative FTIR spectrum of the Pyaung-Gaung peridot samples is shown in figure 14. Characteristic mid-IR spectra revealed several absorption bands located at 1053, 980, 950, 902, 845, 627, 552, and 536 cm–1. These bands were assigned to internal Si-O vibrations (Burns and Huggins, 1972). Although the IR patterns are quite similar to those of Sardinian peridot (reported in Adamo et al., 2009), the maxima positions of all IR bands can be shifted to either lower or higher frequency values depending on the content of iron (Fe2+), as previously suggested by Duke and Stephens (1964), Burns and Huggins (1972), and Jovanovski et al. (2006).

Laser spots from LA-ICP-MS analysis of a Pyaung-Gaung peridot
Figure 15. Laser spots (marked by arrows) show where an olivine inclusion and the peridot host were analyzed by LA-ICP-MS. Photomicrograph by M. Seneewong-Na-Ayutthaya; field of view 1.8 mm.
Table 2. Contents of major elements (by EPMA) and trace elements (by LA-ICP-MS) of the host peridot sample and the olivine inclusion (average and range).

Chemical Compositions. Olivine Inclusion. To understand the chemical relationship between the olivine inclusion and the host crystal, major element (by EPMA) and trace element concentrations (by LA-ICP-MS) of a cut-open inclusion and nearby host crystal were analyzed (see figure 15). The results, presented in table 2, showed that the major contents of SiO2, MgO, CaO, FeO, MnO, and NiO and trace contents of Li, B, Na, Al, Sc, Ti, V, Cr, Mn, Co, Ni, Zn, Ge, and Zr of the inclusion and the host are relatively similar.

Table 3. Chemical composition of peridot samples from Pyaung-Gaung and other localities by EPMA (average and range).
Table 4. Trace element concentrations of peridot samples from Pyaung-Gaung and other localities by LA-ICP-MS (average and range).

Major and Trace Elements. The compositions of major elements by EPMA and trace elements by LA-ICP-MS of the peridot samples from the three localities of Pyaung-Gaung, Yiqisong in China, and Sapat in Pakistan (GIT-GTL reference samples) are presented in tables 3 and 4, respectively. The chemical composition of Pyaung-Gaung peridot ranged from 92.00% to 92.37% forsterite (Mg2SiO4) and 7.63% to 8.00% fayalite (Fe2SiO4), suggesting a mantle source. The composition of major elements was 50.04 wt.% MgO and 42.62 wt.% SiO2, averages similar to those of peridot from Yiqisong and Sapat. The FeO, MnO, NiO, and CaO contents were nearly identical across the three localities. The average MnO and NiO contents were 0.10 wt.% and 0.15 wt.%, respectively, indicating the olivine was from a mantle origin (Ishimaru and Arai, 2008). The atomic proportions were recalculated to present the ratios of Mg/(Mg+Fe), for which all locations had a similar value.

The average trace element contents of peridot from the three origins, listed in table 4, show somewhat similar concentrations. Ni was the most abundant trace element, followed by Mn, Co, Na, Al, Zn, Cr, Sc, Ti, B, Li, Ge, V, and Zr. The Pyaung-Gaung peridot contained higher concentrations of Ni and Zn than the Sapat peridot but lower B, Na, Sc, and Mn. The Yiqisong peridot possessed higher Na, Al, and Cr contents than the Pyaung-Gaung samples. Previous studies showed that the formation of Yiqisong peridot was related to serpentinization (Zhang et al., 2019) and/or spinel lherzolite that was quite similar to those of peridot from Sardinia and Vietnam (Adamo et al., 2009; Thuyet et al., 2016). In contrast, the study of Harlow and Thu (2014) indicated that samples from Pyaung-Gaung and Sapat shared a similar origin. The next section of this study reveals some differences in trace element concentration that are very helpful for geographic origin determination.

2D scatter plots of trace element contents in peridot
Figure 16. 2D scatter plots of trace element contents in peridot from the three geographic origins.
3D scatter plots of trace element contents in peridot
Figure 17. 3D scatter plots of trace elements in peridot from the three localities. Plots oriented to show origin separations.

Origin Determination. The trace element data were then displayed and discriminated in 2D plots of Al-Mn, Cr-Ni, Sc-Cr, Co-Mn, V-Ni, and V-Mn (figure 16) and 3D plots of Ni-Co-V, Ni-Ti-Cr, Ni-Ti-V, Cr-V-Sc, Co-V-Sc, and Cr-V-Co (figure 17). The 2D and 3D cross-plots showed a positive correlation and proved very useful in separating Pyaung-Gaung peridot from the Yiqisong and Sapat deposits for the samples and reference materials measured. Although overlap may occur between some Pyaung-Gaung and Yiqisong data points in the 2D plots, the 3D cross-plots provide a very helpful and straightforward way to determine the origin of peridot from these three deposits. While Ni can be precisely determined using EPMA, this technique is less accurate for other elements at lower concentrations (Shen et al., 2011; Leelawatanasuk et al., 2011). LA-ICP-MS has been proven to be an efficient method for origin determination of these peridot by chemical fingerprinting. However, statistical approaches such as discriminant or multivariate analysis may be needed since they can potentially provide additional data to enhance the certainty of the provenance assignment and reduce error.

17.69 ct oval-cut peridot from the Bernard-Myo area of Mogok
Figure 18. This 17.69 ct oval-cut peridot is from the Bernard-Myo area of Mogok, Myanmar. It is part of the GIA Collection. Photo by Robert Weldon/GIA.


Gemological investigation indicates that Burmese peridot from the Pyaung-Gaung area of Mogok (figure 18) contains tufts of very fine fibers and distinctive protogenetic olivine inclusions. These diagnostic mineral inclusions, as well as inclusions of chromite, magnesite, and chlorite, provide evidence that retrograde metamorphism and/or recrystallization occurred in tension fractures or veinlets during a tectonic event. These inclusions can be used as a locality-specific feature for geographic origin determination in combination with chemical analysis by LA-ICP-MS. Based on our data, 2D and 3D cross-plots of the trace element contents of Al, Sc, Ti, V, Cr, Mn, Co, and Ni are relatively efficient discriminators to distinguish peridot from the major producing sites of Pyaung-Gaung, Yiqisong (China), and Sapat (Pakistan). However, we used only the data obtained by our own study, in order to control the analytical consistency of reference materials. Additional data and more reliable samples from these and other localities will further refine the provenance assignment of peridot in the future.

Dr. Montira Seneewong-Na-Ayutthaya is a research scientist, and Wassana Chongraktrakul is a gemologist, at GIT in Bangkok. Tasnara Sripoonjan (tasnara@hotmail.com) is a chief gemologist at G-ID Laboratories in Bangkok.

This research was fully supported by The Gem and Jewelry Institute of Thailand (Public Organization). The authors are grateful to academic advisors Assoc. Prof. Dr. Visut Pisutha-Arnond, Wilawan Atichat, and Prof. Dr. Chakkaphan Sutthirat for their valuable comments and kind review of this article. We greatly appreciate the useful comments and resources from Dr. George E. Harlow from the American Museum of Natural History. Special thanks also go to Thanong Leelawatanasuk (GIT deputy director) and Malin Sawatekitithum (former GIT chief of research and development) for their suggestions and encouragement. We are thankful to Jirapit Jakkawanvibul, Waratchanok Suwanmanee, Yadawadee Kowinthaweewat, and Pattarat Termpaisit for their technical assistance and Dr. Alongkot Fanka for his helpful discussion during the course of this project. Finally, the authors would like to thank Aung Naing Tun and his family for assistance in the field during our trip to Mogok.

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