Submitted Successfully!
To reward your contribution, here is a gift for you: A free trial for our video production service.
Thank you for your contribution! You can also upload a video entry or images related to this topic.
Version Summary Created by Modification Content Size Created at Operation
1
Fei Liu
 + 2385 word(s) 2385 2021-11-15 05:07:37

Video Upload Options

We provide professional Video Production Services to translate complex research into visually appealing presentations. Would you like to try it?
No, upload directly Yes

Confirm

Are you sure to Delete?
Yes No
Cite
If you have any further questions, please contact Encyclopedia Editorial Office.
Liu, F. Diamond-Bearing Ophiolite. Encyclopedia. Available online: https://encyclopedia.pub/entry/16022 (accessed on 15 November 2024).
Liu F. Diamond-Bearing Ophiolite. Encyclopedia. Available at: https://encyclopedia.pub/entry/16022. Accessed November 15, 2024.
Liu, Fei. "Diamond-Bearing Ophiolite" Encyclopedia, https://encyclopedia.pub/entry/16022 (accessed November 15, 2024).
Liu, F. (2021, November 16). Diamond-Bearing Ophiolite. In Encyclopedia. https://encyclopedia.pub/entry/16022
Liu, Fei. "Diamond-Bearing Ophiolite." Encyclopedia. Web. 16 November, 2021.
Diamond-Bearing Ophiolite
Edit
This entry is adapted from the peer-reviewed paper 10.3390/cryst11111362

Ophiolites are fragments of ancient oceanic crust and upper mantle, which is created at ocean spreading ridges and then emplaced on land. Ophiolite-hosted diamond discovered in ophiolitic peridotite and chromitite is considered to be a new type that has been named an ophiolite-type by Yang et al., in 2011. 

Diamond Ophiolite Chromitite Peridotite Crustal recycling into deep mantle

1. Introduction

According to the differences in occurrence and genesis, natural diamonds are divided into various types, including diamonds occurring in kimberlite, lamproite, ophiolite, alkaline mafic rock, crust-derived ultrahigh-pressure (UHP) metamorphic rock, meteorolite-related and alluvial rocks [1][2][3][4][5]. Ophiolites are fragments of ancient oceanic crust and upper mantle, which is created at ocean spreading ridges and then emplaced on land [6]. Ophiolite-hosted diamond discovered in ophiolitic peridotite and chromitite is considered to be a new type that has been named an ophiolite-type in recent years [4][7].
It has been hundreds of years since the first discovery of diamonds in ophiolites [8][9][10]. Diamonds were successively discovered in ophiolites from Quebec in Canada [8], Kamenusha in the Urals (Russia) and Koryak in the Far East [9][10]. However, these early stage studies merely reported the occurrence of diamonds in ophiolites but did not systematically relate these discoveries to plate tectonics. Since the 1980s, the diamond group in the Chinese Academy of Geological Sciences discovered diamonds in the Luobusa ophiolite (also named Qusong) in the Indus-Yarlung Zangbo suture zone (IYSZ) and Dongqiao ophiolite in the Bangong Nujiang suture zone (BNSZ) in Tibet, China [11][12][13][14]. Subsequently, Jingsui Yang and his group continued this research, and diamonds were also discovered in the ophiolites of Luobusa, Purang, Dongbo, Dangqiong and Dingqing in Tibet, Sartohay in Xinjiang, Hegenshan in Inner Mongolia, Myitkyina and Kalemyo in Myanmar, Pozanti-Karsanti in Turkey, Mirdita in Albania and Horoman in Japan [15][16][17][18][19][20][21][22][23][24][25][26][27][28][29][30][31][32][33]. As these diamonds were extracted by heavy mineral separation in the early stage, their natural origin was initially doubted [7][34]. However, it was not until the in situ diamonds were discovered in the Luobusa and Polar Ural chromitites as well as the Nidar mantle peridotites [24][35]. Particularly, ophiolite-hosted diamonds have inclusions of fluid and Mn-Co-Ni alloy and obviously show trace elements, e.g., Ba, Pb, Th and Eu, and crust-derived carbon–nitrogen isotope compositions different from those of synthetic diamonds [5][36][37]. Following the independent discovery of diamonds in ophiolitic mantle peridotites and chromitites by Australian, Spanish and Indian geologists, the occurrence of the ophiolite-type diamond was widely accepted [35][36][38][39].
Ophiolite-hosted diamond and other UHP minerals have been globally discovered in ophiolites from various orogenic belts, suggesting that diamonds are widespread in mantle rocks [5][24][37][40]. The discovery of ophiolite-hosted diamond opens a new field for research on the genesis of ophiolitic chromitite and host mantle peridotite and for the exploration of the dynamics of crust–mantle recycling [41][42][43]. However, the amounts of diamonds extracted from various ophiolitic peridotites and chromitites differ greatly. For most massifs, several diamond grains were recovered per ton, while over one thousand diamond grains per ton were discovered from the Luobusa mantle peridotites and chromitites. In contrast, less than ten diamond grains per ton were recovered from mantle peridotites in the Xialu (Xigaze), Zedang, Dongbo and Myitkyina massifs [40][44]. It is still unclear what contributes to the difference in such diamond concentrations. A discussion of the spatial distribution and formation mechanism of ophiolite-hosted diamond has become a new direction of current research of ophiolites and plate tectonics [5][37][40]. This paper summarizes the geological characteristics of diamond-bearing ophiolites and discusses the four genetic models for the diamond-bearing and associated unusual minerals-bearing ophiolites, providing a basis for discussing the formation of ophiolitic chromitite and the dynamic process of crust–mantle material recycling.

2. Global Distribution of Diamond-Bearing Ophiolites

Twenty-five diamond-bearing ophiolites have been discovered across the globe, and they are mainly distributed along the Tethyan Orogenic Belt, the Ural-Central Asian Orogenic Belt, the Hidaka metamorphic belt, the Klamath–Acatlán Orogenic Belt in North America and the Andean Orogenic Belt in South America (Figure 1a). The Tethyan Orogenic Belt is a giant and long-lived plate subduction–collision system on the earth that separates the Gondwana supercontinent to the south from the Laurasia supercontinent to the north [45]. It displays a structural difference of continent–continent collision alternating with ocean–continent subduction from east to west (Figure 1b). This belt extends from the Alpine continent–continent collisional orogenic belt in Europe via the complicated Mediterranean ocean–continent subduction belt, eastwards to the Zagros continent–continent collisional orogenic belt in West Asia and the Makrun ocean–continent subduction belt to the east, and to the Himalayan continent–continent collisional orogenic belt. Then it connects with the ocean–continent subduction zone formed by East Indian oceanic slab subducting below Southeast Asia [46]. The Tethyan Orogenic Belt represents an oceanic system remnant commonly composed of Prototethyan, Paleotethyan and Neotethyan oceans that developed during the Early Paleozoic, Late Paleozoic and Mesozoic, respectively [45]. The Paleotethyan ocean represented by late Paleozoic-Triassic ophiolites was bounded by the Cimmerides to the south that mainly consists of Anatolia, Persia, Afghanistan and Tibet, and Cathaysides to the north that includes South China, Indochina, Sibumasu and Qamdo blocks [45][47][48]. The Neotethyan ocean documents the Mesozoic rifting of Pangea and comprises multiple seaways formed by seafloor spreading and widening eastwards and deep mantle circulation processes, including several stages of slab subduction and mantle plume activities [49].
Crystals 11 01362 g001 550
Figure 1. Distribution of twenty-five diamond-bearing ophiolites reported on the globe (a). Nineteen diamond-bearing ophiolites are distributed along the Neotethyan Orogenic Belt, Kunlun–Qilian–Qinling Paleotethyan Orogenic Belt (KQQ), Central Asian Orogenic Belt and Hidaka metamorphic belt (b). Ophiolites: C—Cuobuzha, D—Dongqiao, DB—Dongbo, DQ—Dingqing, DX—Dangqiong–Xiugugabu, EM—Eastern Mirdita (Albania), K—Kalamyo (Myanmar), L—Luobusa, M—Myitkyina (Myanmar), N—Nidar (Kashmir), P—Purang, PK—Pozanti Karsanti (Turkey), QL—Qilian, T—Troodos, WM—Western Mirdita (Albania), X—Xialu, Z—Zedang. Ural-Central Asian Orogenic Belt: Sartohay, Hegenshan, Ray-Iz (Polar Urals). Hidaka Metamorphic Belt: H—Horoman (Japan). BNSZ—Bangong Nujiang suture zone, IYSZ—Indus Yarlung Zangbo suture zone. Internal structures are modified from [50][51][52][53].
The Neotethyan Orogenic Belt, which was discovered with fifteen diamond-bearing ophiolites, includes three subbelts of the BNSZ, IYSZ and the Eastern Mediterranean zone (Figure 1b). Diamond-bearing Dongqiao and Dingqing ophiolites occur in the BNSZ, Tibet [13][14][27]; the Myitkyina ophiolite is located in the Burmese Eastern ophiolitic belt that is regarded to be the southern continuation of the BNSZ [54]. The Luobusa, Zedang, Xialu, Dangqiong–Xiugugabu, Purang, Dongbo, Cuobuzha and Nidar ophiolites occur in the IYSZ [7][14][20][23][25][26][35][55][56][57]; the Kalamyo ophiolite crops out in the Indo-Burma Range that is regarded to be connected with the IYSZ [58]. The Pozanti Karsanti (Turkey), East Mirdita (Bulqiza, Albania) and West Mirdita (Skenderbeu, Albania) ophiolites occur in the Mediterranean ophiolite belt [28][30][32] (Figure 1b).
The 495–550 Ma diamond-bearing Yushigou ophiolite in the North Qilian Orogenic Belt represents the relics of the Prototethyan ocean [59]. Diamond-bearing ophiolites in the Ural-Central Asian Orogenic Belt consist of the Ray-Iz massif in the Polar Urals [24], the Sartohay ophiolite in Xinjiang and the Hegenshan ophiolite in Inner Mongolia [21][22] (Figure 1b). The diamond-bearing Horoman mantle peridotites [33], each ~10 km long, ~8 km wide and ~3 km thick, are exposed along the southern edge of the NNW–SSE oriented, ~120 km long and 10~20 km wide Hidaka metamorphic belt, which is the boundary between the North American Plate (Okhotsk block) and the Eurasian Plate [60]. The Klamath–Acatlán Orogenic Belt includes the Klamath massif in western United States and the Acatlán complex in southern Mexico [39]. Ophiolite-hosted diamonds in this belt were discovered in the Jurassic Josephine peridotite [61] and the Early Paleozoic Tehuitzingo chromitite [39], respectively. About ten diamond grains were discovered in the Moa-Baracoa ophiolitic peridotite massif in eastern Cuba, which is about 100 km long and 10–30 km wide, covering an area of ~1500 km2 (Rui et al., in preparation). One diamond grain was obtained from the Taitao peridotite in Chile, the western part of the Andean Orogenic Belt (Wu et al., in preparation).

3. Geochemical Characteristics of Diamond-Bearing Ophiolites

The wall rocks of the ophiolite-hosted diamonds are podiform chromitite and mantle peridotite. Mantle peridotite is dominated by Cpx-bearing harzburgite (Figure 2). Diamond-bearing lherzolite was merely reported in the Purang and Horoman massifs [33][56]. Ophiolites in the IYSZ, including the Purang, Dongbo, Cuobuzha, Dangqiong, Xialu, Zedang and Luobusa massifs, commonly have harzburgites with low contents of Al and Ca but high contents of Mg relative to the primitive mantle. The REE and Os contents of these harzburgites are notably lower than those of the primitive mantle. These geochemical features are comparable with those of depleted abyssal peridotites, which have experienced variable degrees of partial melting [62][63]. Some samples are relatively enriched in LREE, Rb and Ba and have a comparatively large range of Cr# (Cr# = 100 × Cr/(Cr + Al), 18–75) in chromite (Cr-spinel). The diamond-bearing peridotites commonly show higher contents of platinum group elements (PGE) than those of the primitive mantle. Such geochemical characteristics suggest that these depleted abyssal peridotites were widely metasomatized by sulfide-rich, incompatible element-rich and high-PGE fluids/melts [62][63][64][65].
Crystals 11 01362 g002 550
Figure 2. Compiled stratigraphic-lithological columnar sections of the main diamond-bearing ophiolites shown in Figure 1b along the Neotethyan Orogenic Belt. Red triangles labeled as diamonds hosted in podiform chromitite, harzburgite and lherzolite. (a) Dingqing ophiolite from the eastern part of the BNSZ, Tibet [27][44]; (b) Dongqiao ophiolite from the central part of the BNSZ, Tibet [13][14][44]; (c) Dongbo, (d) Purang and (e) Xiugugabu ophiolites from the wetern part of the IYSZ [44]; (f) Luobusa ophiolite from the eastern part of the IYSZ [14][16][17]; (g) Xialu ophiolite from the central part of the IYSZ [26][44]; (h) East Mirdita (Bulqiza massif) from the eastern Mediterranean ophiolite belt [28].
In a rock–melt interaction process, Re-Os isotopes can reflect the impacts of infiltrating melts on the ophiolitic mantle [66][67]. Os is a highly compatible element during partial melting, while Re is a moderately incompatible element, which leads to comparatively low Re/Os ratios and increases the 187Os/188Os ratio in residual mantle peridotites, although the rate of growth reduces over time [66][67][68]. Thus, the lower 187Os/188Os ratios recorded in peridotites may indicate an earlier local melting event [63][68]. In addition, serpentinization, seafloor alteration and metasomatism of mantle peridotites by fluids/melts pose weak impacts on the whole rock’s 187Os/188Os ratio, and thus, the Re depletion model ages can reflect the time of partial melting [67][68]. Compared to the average 187Os/188Os ratio of a primitive upper mantle (0.1296) [69], seventy-eight 187Os/188Os ratios (0.113–0.145, with an average of 0.125) of the Purang, Dongbo and Cuobuzha harzburgites in the western segment of IYSZ overlap the ranges of the subcontinental lithospheric mantle (SCLM, 0.105–0.129) [70] and depleted oceanic lithospheric mantle (0.123–0.129) [70][71]. The Baigang and Dazhuqu mantle peridotites in central IYSZ display a relatively large range in 187Os/188Os (0.118–0.130, with an average of 0.126). Additionally, sixty-eight 187Os/188Os ratios of Luobusa and Zedang mantle peridotites in the eastern segment show a comparatively large range (0.121–0.137, with an average of 0.126 [63][72][73]. They all show hybrid signatures of depleted oceanic lithosphere and SCLM (Figure 3).
Crystals 11 01362 g003 550
Figure 3. Osmium isotopic values of diamond-bearing chromitite and peridotite in different ophiolites. Osmium isotopic values of primitive upper mantle, depleted mid-ocean-ridge-basalt mantle, Ocean-island basalt (OIB), Pico and Faial OIB from the Azores after [71]. Osmium istotopic data references: Purang [63][74][75]; Dongbo [62]; Cuobuzha [65]; Baigang [63]; Dazhuqu [76]; Zedang [63][77]; Luobusa [72][78][79]; Bangong Lake [80]; Yunzhug [81]; Dongqiao [67][79][82]; Sartohay [79]; Yushigou [59].
Podiform chromitite is defined as lenticular aggregates of chromite formed in Alpine-type peridotites and oceanic crust–mantle transition zones [83], and it normally contains over 20 vol.% chromite, and preserves abundant magma rheological and high-temperature deformation structures that are distinct from those of layered chromitite [83][84]. Podiform chromitite, by occurrences and Cr values of chromite, may be classified as follows: (1) According to the exposed locations of chromitite orebodies in a well-exposed ophiolitic sequence, ophiolite can be divided into subvarieties occurring below and within the MOHO transition zone [83][85][86]. The former is mostly enclosed in harzburgite with a thin dunite-envelope and usually occurs as large-sized deposits of economic value. The latter is generally distributed in thin-bedded dunite and usually forms small-sized, disseminated and banded chromitite deposits, which are commonly interlayered with cumulate dunite [86]. (2) According to the structural deformation features of podiform chromitite orebodies, chromitite deposits are mainly divided into discordant, subconcordant and concordant types compared with permeable structures of foliation and lineation developed in host mantle peridotites [87]. Discordant ore bodies are irregular and obviously cut through the foliation and lineation of peridotites, subconcordant orebodies usually have angles of 10°–25° with the foliation, and concordant ore bodies are commonly parallel to the foliation and lineation [87]. (3) According to the chromite aggregation forms, podiform chromitites are divided into massive, nodular, antinodular, densely/sparsely disseminated, banded and vein-like types [85][88][89]. (4) According to geochemical compositions of chromite in podiform chromitite, it can be divided into high-Cr (Cr# value > 60) type and high-Al (Cr# value < 60) type [90]. High-Al chromitite is usually considered to be precipitated from basaltic melts, which might be formed at a mid-ocean ridge (MOR) or derived from backarc or forearc settings at a suprasubduction zone (SSZ). High-Cr type is generally related to boninitic melt metasomatism in subduction zones [91][92]. Recently, Li et al. (2019) further subdivided chromitite from the Dingqing ophiolite in the BNSZ, China, into high-Cr (Cr# = 78–86), medium-high-Cr (Cr# = 60–74), medium-Cr (Cr# = 30–51) and low-Cr (Cr# = 9–14) types [89].
Ophiolite-hosted diamonds occur in both high-Cr chromitite, e.g., the Ray-Iz and Luobusa ophiolites [24][93], as well as in high-Al chromitite, e.g., the Sartohay and Hegenshan ophiolites [21][22]. They even have been recovered from high-Al and high-Cr type chromitites in the same ophiolite massif such as Dongbo, Purang, Dingqing, Mirdita and Pozanti Karsanti [29][32][89][94]. Current statistics show that the amount of diamond grains in high-Cr type chromitite is much higher than those in high-Al type chromitite [40]. For example, the number of diamond grains from the Luobusa, Kangjinla and Ray-Iz massive high-Cr chromitites reaches 1000 per ton in total [20][24][57], while in both high-Al type and high-Al-high-Cr type chromitites from, e.g., the Dongbo and Purang ophiolites, there are commonly only several to dozens of diamond grains per ton [7][56][95]. The reason for these differences is unclear.
187Os/188Os ratios of chromitites are significantly higher in high-Cr chromitites compared to high-Al chromitites. For example, for Dongbo and Purang, the high-Cr chromitites have 187Os/188Os compositions varying from 0.128 to 0.133 and 0.123 to 0.132, respectively, whereas their high-Al chromitites have values ranging from 0.120 to 0.126 and 0.124 to 0.127 [62][63][74][94]. It is noted that compared to the Purang and Dongbo high-Cr chromitites, the Luobusa high-Cr chromitites exhibit generally lower 187Os/188Os ratios of 0.104–0.127 [72][78][79] (Figure 3). The latter chromitite massif has been interpreted to have been formed by decompression partial melting of garnet and orthopyroxene (Opx) in the SCLM [37][79]. Alternatively, the Luobusa podiform chromitite was produced by mixing primitive asthenospheric Cr-rich melt and boninitic magma, triggering the saturation and crystallization of chromite [96].

References

  1. Stachel, T.; Harris, J.W. The origin of cratonic diamonds—Constraints from mineral inclusions. Ore Geol. Rev. 2008, 34, 5–32.
  2. Stachel, T.; Harris, J.W.; Muehlenbachs, K. Sources of carbon in inclusion bearing diamonds. Lithos 2009, 112, 625–637.
  3. Shirey, S.B.; Cartigny, P.; Frost, D.J.; Keshav, S.; Nestola, F.; Nimis, P.; Pearson, D.G.; Sobolev, N.V.; Walter, M.J. Diamonds and the Geology of Mantle Carbon. Rev. Mineral. Geochem. 2013, 75, 355–421.
  4. Yang, J.; Robinson, P.T.; Dilek, Y. Diamonds in ophiolites. Elements 2014, 10, 127–130.
  5. Lian, D.; Yang, J. Ophiolite-Hosted Diamond: A New Window for Probing Carbon Cycling in the Deep Mantle. Engineering 2019, 5, 406–420.
  6. Dilek, Y.; Furnes, H. Ophiolite genesis and global tectonics: Geochemical and tectonic fingerprinting of ancient oceanic lithosphere. Geol. Soc. Am. Bull. 2011, 123, 387–411.
  7. Yang, J.S.; Xu, X.Z.; Li, Y.; Li, J.Y.; Ba, D.Z.; Rong, H.; Zhang, Z.M. Diamonds recovered from peridotite of Purang ophiolite in the Yarlung-Zangbo suture of Tibet: A proposal for a new type of diamond occurrence. Acta. Petrol. Mineral. 2011, 27, 3171–3178, (In Chinese with English Abstract).
  8. Dresser, J.A. Preliminary Report on the Serpentine and Associated Rocks of Southern Quebec; Memoir-Geological Survey of Canada: Ottawa, ON, Canada, 1913; Volume 1, pp. 1–103.
  9. Kaminskiy, F.V.; Vaganov, V.I. Petrological conditions for diamond occurrences in Alpine-type ultrabasic rocks. Int. Geol. Rev. 1977, 19, 1151–1162.
  10. Shilo, A.N.; Kaminskiy, V.F.; Palandzhyan, A.S.; Tilman, M.S.; Tkachenko, A.L. First diamond finds in Alpine-type ultrabasic rocks in the Northeastern USSR. Doki. Akad. Nauk SSSR 1978, 241, 179–182.
  11. Fang, Q.S.; Bai, W.J. The discovery of Alpine~type diamond bearing ultrabasic intrusions in Xizang (Tibet). Geol. Rev. 1981, 5, 455–457, (In Chinese with English Abstract).
  12. Liang, R.X.; Yang, F.Y.; Fang, Q.S.; Yan, B.G. Diamond-bearing ultramafic rocks in ophiolite belt of Xizang province and its geological significance. Geol. China 1984, 2, 26–28, (In Chinese with English Abstract).
  13. Yan, B.G.; Liang, R.X.; Fang, Q.S.; Yang, F.Y.; Yuan, C.Y. Characteristics of diamond and diamond-bearing ultramafic rocks in Qiaoxi and Hongqu, Xizhang. CAGS Bul. Inst. Geol. 1986, 14, 61–118, (In Chinese with English Abstract).
  14. Bai, W.; Zhou, M.; Robinson, P.T. Possibly diamond-bearing mantle peridotites and podiform chromitites in the Luobusa and Donqiao ophiolites, Tibet. Can. J. Earth Sci 1993, 30, 1650–1659.
  15. Bai, W.J.; Yang, J.S.; Fang, Q.S.; Yan, B.G.; Shi, R.D. An unusual mantle mineral group in ophiolites of Tibet. Geol. China 2003, 30, 144–150, (In Chinese with English Abstract).
  16. Robinson, P.T.; Bai, W.J.; Malpas, J.; Yang, J.S.; Zhou, M.F.; Fang, Q.S.; Hu, X.F.; Cameron, S.; Staudigel, H. Ultra-high pressure minerals in the Luobusa Ophiolite, Tibet, and their tectonic implications. Geol. Soc. 2004, 226, 247–271.
  17. Yang, J.S.; Dobrzhinetskaya, L.; Bai, W.J.; Fang, Q.S.; Robinson, P.T.; Zhang, J.; Green, H.W. Diamond-and coesite-bearing chromitites from the Luobusa ophiolite, Tibet. Geology 2007, 35, 875–878.
  18. Xu, X.Z.; Yang, J.S.; Ba, D.Z.; Chen, S.Y.; Fang, Q.S.; Bai, W.J. Diamond discovered from the Kangjinla chromitite in the Yarlung Zangbo ophiolite belt, Tibet. Acta. Petrol. Mineral. 2008, 24, 1453–1462, (In Chinese with English Abstract).
  19. Yang, J.S.; Zhang, Z.M.; Li, T.F.; Li, Z.L.; Ren, Y.F.; Xu, X.Z.; Ba, D.Z.; Bai, W.J.; Fang, Q.S.; Chen, S.Y. Unusual minerals from harzburgite, the host rock of the Luobusa chromite deposit, Tibet. Acta. Petrol. Mineral. 2008, 24, 1445–1452, (In Chinese with English Abstract).
  20. Xu, X.Z.; Yang, J.S.; Chen, S.Y.; Fang, Q.S.; Bai, W.J.; Ba, D.Z. Unusual mantle mineral group from chromitite orebody Cr-11 in Luobusa ophiolite of Yarlung-Zangbo suture zone, Tibet. J. Earth Sci.-China 2009, 20, 284–302.
  21. Huang, Z.; Yang, J.; Robinson, P.T.; Zhu, Y.; Xiong, F.; Liu, Z.; Zhang, Z.; Xu, W. The discovery of diamonds in chromitites of the Hegenshan ophiolite, Inner Mongolia, China. Acta. Geol. Sin. (Engl. Ed.) 2015, 89, 341–350.
  22. Tian, Y.; Yang, J.; Robinson, P.T.; Xiong, F.; Li, Y.; Zhang, Z.; Liu, Z.; Liu, F.; Niu, X. Diamond Discovered in High-Al Chromitites of the Sartohay Ophiolite, Xinjiang Province, China. Acta. Geol. Sin. (Engl. Ed.) 2015, 89, 332–340.
  23. Xiong, F.; Yang, J.; Robinson, P.T.; Xu, X.; Ba, D.; Li, Y.; Zhang, Z.; Rong, H. Diamonds and Other Exotic Minerals Recovered from Peridotites of the Dangqiong Ophiolite, Western Yarlung-Zangbo Suture Zone, Tibet. Acta. Geol. Sin. (Engl. Ed.) 2016, 90, 425–439.
  24. Yang, J.; Meng, F.; Xu, X.; Robinson, P.T.; Dilek, Y.; Makeyev, A.B.; Wirth, R.; Wiedenbeck, M.; Cliff, J. Diamonds, native elements and metal alloys from chromitites of the Ray-Iz ophiolite of the Polar Urals. Gondwana Res. 2015, 27, 459–485.
  25. Guo, G.L.; Yang, J.S.; Liu, X.D.; Xu, X.Z.; Zhang, Z.M.; Tian, Y.Z.; Xiong, F.H.; Wu, Y. Implications of unusual minerals in Zedang mantle peridotite, Tibet. Geol. China 2015, 42, 1483–1492, (In Chinese with English Abstract).
  26. Xu, X.Z.; Yang, J.S.; Xiong, F.H.; Ba, D.Z.; Zhang, Z.M.; Li, Y. Diamond and other exotic minetals discovered from the Xigaze Mantle peridotite in the Yarlung-Zangbo sutute zone, Tibet. Acta. Geol. Sin. 2018, 92, 1389–1400, (In Chinese with English Abstract).
  27. Xiong, F.; Yang, J.; Dilek, Y.; Xu, X.; Zhang, Z. Origin and significance of diamonds and other exotic minerals in the Dingqing ophiolite peridotites, eastern Bangong-Nujiang suture zone, Tibet. Lithosphere 2018, 10, 142–155.
  28. Xiong, F.; Yang, J.; Robinson, P.T.; Dilek, Y.; Milushi, I.; Xu, X.; Zhou, W.; Zhang, Z.; Rong, H. Diamonds Discovered from High–Cr Podiform Chromitites of Bulqiza, Eastern Mirdita Ophiolite, Albania. Acta. Geol. Sin. (Engl. Ed.) 2017, 91, 455–468.
  29. Wu, W.; Yang, J.; Wirth, R.; Zheng, J.; Lian, D.; Qiu, T.; Milushi, I. Carbon and nitrogen isotopes and mineral inclusions in diamonds from chromitites of the Mirdita ophiolite (Albania) demonstrate recycling of oceanic crust into the mantle. Am. Mineral. 2019, 104, 485–500.
  30. Wu, W.; Yang, J.; Ma, C.; Milushi, I.; Lian, D.; Tian, Y. Discovery and Significance of Diamonds and Moissanites in Chromitite within the Skenderbeu Massif of the Mirdita Zone Ophiolite, West Albania. Acta. Geol. Sin. (Engl. Ed.) 2017, 91, 882–897.
  31. Lian, D.; Yang, J.; Wiedenbeck, M.; Dilek, Y.; Rocholl, A.; Wu, W. Carbon and nitrogen isotope, and mineral inclusion studies on the diamonds from the Pozanti–Karsanti chromitite, Turkey. Contrib. Mineral. Petr. 2018, 173, 72.
  32. Lian, D.; Yang, J.; Dilek, Y.; Wu, W.; Zhang, Z.; Xiong, F.; Liu, F.; Zhou, W. Deep mantle origin and ultra-reducing conditions in podiform chromitite: Diamond, moissanite, and other unusual minerals in podiform chromitites from the Pozanti-Karsanti ophiolite, southern Turkey. Am. Mineral. 2017, 102, 1101–1113.
  33. Li, Y.; Yang, J.; Nida, K.; Yamamoto, S.; Lin, Y.; Li, Q.; Tian, M.; Kon, Y.; Komiya, T.; Maruyama, S. The mineralogical and chronological evidences of subducted continent material in deep mantle: Diamond, zircon and rutile separated from the Horoman peridotite of Japan. In Proceedings of the AGU Fall Meeting, New Orleans, LA, USA, 11–15 December 2017; AGU: Seattle, WA, USA, 2017; p. DI51C-0418.
  34. Taylor, W.R.; Milledge, H.J.; Griffin, B.J.; Nixon, P.H.; Mattey, D.P. Characteristics of microdiamonds from ultramafic massifs in Tibet: Authemic ophialitic diamonds or contamination. In Proceedings of the Sixth International Kimberlite Conference Extended Abstract, Novosibirsk, Russia, 19 September 1995; pp. 623–624.
  35. Das, S.; Basu, A.R.; Mukherjee, B.K. In situ peridotitic diamond in Indus ophiolite sourced from hydrocarbon fluids in the mantle transition zone. Geology 2017, 45, 755–758.
  36. Howell, D.; Griffin, W.L.; Yang, J.; Gain, S.; Stern, R.A.; Huang, J.X.; Jacob, D.E.; Xu, X.; Stokes, A.J.; O’Reilly, S.Y.; et al. Diamonds in ophiolites: Contamination or a new diamond growth environment? Earth Planet. Sci. Lett. 2015, 430, 284–295.
  37. Yang, J.; Wu, W.; Lian, D.; Rui, H. Peridotites, chromitites and diamonds in ophiolites. Nat. Rev. Earth Environ. 2021, 2, 198–212.
  38. Griffin, W.L.; Afonso, J.C.; Belousova, E.A.; Gain, S.E.; Gong, X.; González-Jiménez, J.M.; Howell, D.; Huang, J.; McGowan, N.; Pearson, N.J. Mantle Recycling: Transition Zone Metamorphism of Tibetan Ophiolitic Peridotites and its Tectonic Implications. J. Petrol. 2016, 57, 655–684.
  39. Farré-de-Pablo, J.; Proenza, J.A.; González-Jiménez, J.M.; Garcia-Casco, A.; Colás, V.; Roqué-Rossell, J.; Camprubí, A.; Sánchez-Navas, A. A shallow origin for diamonds in ophiolitic chromitites. Geology 2019, 47, 75–78.
  40. Liu, F.; Yang, J.S.; Lian, D.Y.; Xiong, F.H.; Wu, W.W. Diamonds and other unusual minerals in global ophiolites. Acta. Geol. Sin. 2020, 94, 2588–2605, (In Chinese with English Abstract).
  41. Liou, J.G.; Tsujimori, T.; Yang, J.; Zhang, R.Y.; Ernst, W.G. Recycling of crustal materials through study of ultrahigh-pressure minerals in collisional orogens, ophiolites, and mantle xenoliths: A review. J. Asian Earth Sci. 2014, 96, 386–420.
  42. Coleman, R.G. The ophiolite concept evolves. Elements 2015, 10, 82–84.
  43. Rollinson, H. Surprises from the top of the mantle transition zone. Geol. Today 2016, 32, 58–64.
  44. Liu, F.; Yang, J.S.; Lian, D.Y.; Li, G.L. Geological features of Neothyan ophiolites in Tibetan Plateau and its tectonic evolution. Acta. Petrol. Mineral. 2020, 36, 2913–2945, (In Chinese with English Abstract).
  45. Wu, F.Y.; Wan, B.; Zhao, L.; Xiao, W.J.; Zhu, R.X. Tethyan geodynamics. Acta. Petrol. Mineral. 2020, 36, 1627–1674, (In Chinese with English Abstract).
  46. Li, Z.H.; Xu, Z.Q. Dynamics of along-strike transition between oceanic subduction and continental collision: Effects of fluid-melt activity. Acta. Petrol. Mineral. 2015, 31, 3524–3530, (In Chinese with English Abstract).
  47. Xu, Z.; Dilek, Y.; Cao, H.; Yang, J.; Robinson, P.; Ma, C.; Li, H.; Jolivet, M.; Roger, F.; Chen, X. Paleo-Tethyan evolution of Tibet as recorded in the East Cimmerides and West Cathaysides. J. Asian Earth Sci. 2015, 105, 320–337.
  48. Metcalfe, I. Gondwana dispersion and Asian accretion: Tectonic and palaeogeographic evolution of eastern Tethys. J. Asian Earth Sci 2013, 66, 1–33.
  49. Dilek, Y.; Furnes, H. Tethyan ophiolites and Tethyan seaways. J. Geol. Soc. Lond. 2019, 176, 899–912.
  50. Dilek, Y. Collision tectonics of the Mediterranean region: Causes and consequences. Spec. Pap.-Geol. Soc. Am. 2006, 409, 1–13.
  51. Seltmann, R.; Porter, T.M.; Pirajno, F. Geodynamics and metallogeny of the central Eurasian porphyry and related epithermal mineral systems: A review. J. Asian Earth Sci. 2014, 79, 810–841.
  52. Şengör, A.M.C.; Natal’In, B.A. Turkic-type orogeny and its role in the making of the continental crust. Annu. Rev. Earth Planet. Sci. 1996, 24, 263–337.
  53. Liu, Y.; Li, W.; Feng, Z.; Wen, Q.; Neubauer, F.; Liang, C. A review of the Paleozoic tectonics in the eastern part of Central Asian Orogenic Belt. Gondwana Res. 2017, 43, 123–148.
  54. Chen, Y.; Yang, J.; Xu, Z.; Tian, Y.; Lai, S. Diamonds and other unusual minerals from peridotites of the Myitkyina ophiolite, Myanmar. J. Asian Earth Sci. 2018, 164, 179–193.
  55. McGowan, N.M.; Griffin, W.L.; González-Jiménez, J.M.; Belousova, E.; Afonso, J.C.; Shi, R.; McCammon, C.A.; Pearson, N.J.; O’Reilly, S.Y. Tibetan chromitites: Excavating the slab graveyard. Geology 2015, 43, 179–182.
  56. Xiong, F.; Liu, Z.; Kapsiotis, A.; Yang, J.; Davide, L.; Robinson, P.T. Petrogenesis of lherzolites from the Purang ophiolite, Yarlung-Zangbo suture zone, Tibet: Origin and significance of ultra-high pressure and other ‘unusual’ minerals in the Neo-Tethyan lithospheric mantle. Int. Geol. Rev. 2019, 61, 2184–2210.
  57. Xu, X.; Yang, J.; Robinson, P.T.; Xiong, F.; Ba, D.; Guo, G. Origin of ultrahigh pressure and highly reduced minerals in podiform chromitites and associated mantle peridotites of the Luobusa ophiolite, Tibet. Gondwana Res. 2015, 27, 686–700.
  58. Liu, F.; Yang, J.; Niu, X.; Dongyang, L.; Xiong, F.; Sein, K. Diamonds in MOR-type and SSZ-type peridotites in eastern Neotethyan ophiolites: A new observation on unusual minerals and continental materials cycling within deep mantle. Lithos 2021. in preparation.
  59. Feng, G.; Yang, J.; Niu, X.; Liu, F.; Qiu, T.; Dilek, Y. Formation processes and tectonic implications of mantle peridotites of the Yushigou ophiolite in the North Qilian Orogenic Belt, NW China. Lithos 2021, 400–401, 106430.
  60. Niida, K. Petrology of the Horoman ultramafic rocks in the Hidaka metamorphic belt, Hokkaido, Japan. J. Fac. Sci. Hokkaido Univ. 1984, 21, 197–250.
  61. Liu, F.; Yang, J.; Lian, D.; Li, G.; Wu, W. Diamonds first reported from the Josephine ophiolitic peridotites in North America, western cost of the Pacific Ocean. In Proceedings of the International Symposium on Deep Earth Exploration and Practices, Nanjing, China, 26–31 October 2021.
  62. Niu, X.; Yang, J.; Dilek, Y.; Xu, J.; Li, J.; Chen, S.; Feng, G.; Liu, F.; Xiong, F.; Liu, Z. Petrological and Os isotopic constraints on the origin of the Dongbo peridotite massif, Yarlung Zangbo Suture Zone, Western Tibet. J. Asian Earth Sci. 2015, 110, 72–84.
  63. Xu, Y.; Liu, J.; Xiong, Q.; Su, B.; Scott, J.M.; Xu, B.; Zhu, D.; Pearson, D.G. The complex life cycle of oceanic lithosphere: A study of Yarlung-Zangbo ophiolitic peridotites, Tibet. Geochim. Cosmochim. Ac. 2020, 277, 175–191.
  64. Lian, D.; Yang, J.; Robinson, P.T.; Liu, F.; Xiong, F.; Zhang, L.; Gao, J.; Wu, W. Tectonic Evolution of the Western Yarlung Zangbo Ophiolitic Belt, Tibet: Implications from the Petrology, Mineralogy, and Geochemistry of the Peridotites. J. Geol. 2016, 124, 353–376.
  65. Feng, G.; Yang, J.; Dilek, Y.; Liu, F.; Xiong, F. Petrological and Re-Os isotopic constraints on the origin and tectonic setting of the Cuobuzha peridotite, Yarlung Zangbo suture zone, southwest Tibet, China. Lithosphere 2018, 10, 95–108.
  66. Büchl, A.; Brügmann, G.E.; Batanova, V.G.; Hofmann, A.W. Os mobilization during melt percolation: The evolution of Os isotope heterogeneities in the mantle sequence of the troodos ophiolite, Cyprus. Geochim. Cosmochim. Acta 2004, 68, 3397–3408.
  67. Shi, R.; Griffin, W.L.; O’Reilly, S.Y.; Huang, Q.; Zhang, X.; Liu, D.; Zhi, X.; Xia, Q.; Ding, L. Melt/mantle mixing produces podiform chromite deposits in ophiolites: Implications of Re–Os systematics in the Dongqiao Neo-tethyan ophiolite, northern Tibet. Gondwana Res. 2012, 21, 194–206.
  68. Rudnick, R.L.; Walker, R.J. Interpreting ages from Re–Os isotopes in peridotites. Lithos 2009, 112, 1083–1095.
  69. Becker, H.; Dale, C.W. Re–Pt–Os Isotopic and Highly Siderophile Element Behavior in Oceanic and Continental Mantle Tectonites. Rev. Mineral. Geochem. 2016, 81, 369–440.
  70. Shirey, S.B.; Walker, R.J. The Re-Os isotope system in cosmochemistry and hightemperature geochemistry. Annu. Rev. Earth Planet. Sci. 1998, 26, 423–500.
  71. Widom, E. Ancient mantle in a modern plume. Nature 2002, 420, 281–282.
  72. Shi, R.; Alard, O.; Zhi, X.; O’Reilly, S.Y.; Pearson, N.J.; Griffin, W.L.; Zhang, M.; Chen, X. Multiple events in the Neo-Tethyan oceanic upper mantle: Evidence from Ru–Os–Ir alloys in the Luobusa and Dongqiao ophiolitic podiform chromitites, Tibet. Earth Planet. Sci. Lett. 2007, 261, 33–48.
  73. Li, J.Y. Genesis of Mantle Peridotite in the Luobusa, Tibet—The Study of Scientific Drilling Core (LSD-1). Ph.D. Thesis, Chinese Academy of Geological Science, Beijing, China, 2012; pp. 1–179.
  74. Liu, C.; Wu, F.; Chu, Z.; Ji, W.; Yu, L.; Li, J. Preservation of ancient Os isotope signatures in the Yungbwa ophiolite (southwestern Tibet) after subduction modification. J. Asian Earth Sci. 2012, 53, 38–50.
  75. Gong, X.; Shi, R.; Griffin, W.L.; Huang, Q.; Xiong, Q.; Chen, S.; Zhang, M.; O’Reilly, S.Y. Recycling of ancient subduction-modified mantle domains in the Purang ophiolite (southwestern Tibet). Lithos 2016, 262, 11–26.
  76. Liu, T.; Wu, F.; Liu, C.; Zhang, C.; Ji, W.; Xu, Y. Reconsideration of Neo-Tethys evolution constrained from the nature of the Dazhuqu ophiolitic mantle, southern Tibet. Contrib. Mineral. Petr. 2019, 174, 23.
  77. Lai, S.; Yang, J.; Dilek, Y.; Xiong, F.; Jiang, R.; Chen, Y. Petrological and Os Isotopic Characteristics of Zedong Peridotites in the Eastern Yarlung–Zangbo Suture in Tibet. Acta. Geol. Sin. (Engl. Ed.) 2018, 92, 442–461.
  78. Zhang, C.; Liu, C.; Liu, T.; Wu, F. Evolution of mantle peridotites from the Luobusa ophiolite in the Tibetan Plateau: Sr-Nd-Hf-Os isotope constraints. Lithos 2020, 362, 105477.
  79. Shi, R.D.; Huang, Q.S.; Liu, D.L.; Fan, S.Q.; Zhang, X.R.; Ding, L. Recycling of Ancient Sub-Continental Lithospheric Mantle Constraints on the Genesis of the Ophiolitic Podiform Chromitites. Geol. Rev. 2012, 58, 643–652, (In Chinese with English Abstract).
  80. Huang, Q.S.; Shi, R.D.; Ding, B.H.; Liu, D.L.; Zhang, X.R.; Fan, S.Q.; Zhi, X.C. Re-Os isotopic evidence of MOR-type ophiolite from the Bangong Co for the opening of Bangong-Nujiang Tethys Ocean. Acta. Petrol. Mineral. 2012, 31, 465–478, (In Chinese with English Abstract).
  81. Huang, X.; Shi, R.; Gong, X.; Huang, Q.; Griffin, W.L.; O’Reilly, S.Y.; Chen, S. Oceanization of the subcontinental lithospheric mantle recorded in the Yunzhug ophiolite, Central Tibetan Plateau. Lithos 2020, 370, 105612.
  82. Huang, Q.; Shi, R.; O’Reilly, S.Y.; Griffin, W.L.; Zhang, M.; Liu, D.; Zhang, X. Re-Os isotopic constraints on the evolution of the Bangong-Nujiang Tethyan oceanic mantle, Central Tibet. Lithos 2015, 224, 32–45.
  83. Thayer, T.P. Principal features and origin of podiform chromite deposits, and some observations on the Guelman-Soridag District, Turkey. Econ. Geol. 1964, 59, 1497–1524.
  84. Cameron, G.N. Chromite in the central sector of the eastern Bushveld Complex, South Africa. Am. Mineral. 1977, 62, 1082–1096.
  85. Lago, B.L.; Michel, R.; Adolphe, N. Podiform Chromite Ore Bodies: A Genetic Model. J. Petrol. 1982, 23, 103–125.
  86. Arai, S.; Miura, M. Formation and modification of chromitites in the mantle. Lithos 2016, 264, 277–295.
  87. Cassard, D.; Nicolas, A.; Rabinovitch, M.; Moutte, J.; Leblanc, M.; Prinzhofer, A. Structural classification of chromite pods in southern New Caledonia. Econ. Geol. 1981, 76, 805–831.
  88. Leblanc, M.; Nicolas, A. Ophiolitic chromitites. Int. Geol. Rev. 1992, 34, 653–686.
  89. Li, G.L.; Yang, J.S.; Bo, R.Z.; Rui, H.C.; Xiong, F.H.; Guo, T.F.; Zhang, C.J. Dingqing ophiolite chromite in the eastern segment of Bangong Co-Nujiang suture zone, Tibet: Occurrence characteristics and classifications. Geol. China 2019, 46, 1–20, (In Chinese with English Abstract).
  90. Dick, H.J.B.; Bullen, T. Chromian spinel as a petrogenetic indicator in abyssal and alpine-type peridotites and spatially associated lavas. Contrib. Miner. Petr. 1984, 86, 54–76, (In Chinese with English Abstract).
  91. Arai, S. Conversion of low-pressure chromitites to ultrahigh-pressure chromitites by deep recycling: A good inference. Earth Planet. Sci. Lett. 2013, 379, 81–87.
  92. Zhou, M.; Robinson, P.T.; Su, B.; Gao, J.; Li, J.; Yang, J.; Malpas, J. Compositions of chromite, associated minerals, and parental magmas of podiform chromite deposits: The role of slab contamination of asthenospheric melts in suprasubduction zone environments. Gondwana Res. 2014, 26, 262–283.
  93. Xiong, F.; Yang, J.; Robinson, P.T.; Xu, X.; Liu, Z.; Li, Y.; Li, J.; Chen, S. Origin of podiform chromitite, a new model based on the Luobusa ophiolite, Tibet. Gondwana Res. 2015, 27, 525–542.
  94. Xiong, F.; Yang, J.; Robinson, P.T.; Xu, X.; Liu, Z.; Zhou, W.; Feng, G.; Xu, J.; Li, J.; Niu, X. High-Al and high-Cr podiform chromitites from the western Yarlung-Zangbo suture zone, Tibet: Implications from mineralogy and geochemistry of chromian spinel, and platinum-group elements. Ore. Geol. Rev. 2017, 80, 1020–1041.
  95. Xu, X.Z.; Yang, J.S.; Ba, D.Z.; Zhang, Z.M.; Xiong, F.H.; Li, Y. Diamond discovered from the Dongbo mantle peridotite in the Yarlung Zangbo suture zone, Tibet. Geol. China 2015, 42, 1471–1482, (In Chinese with English Abstract).
  96. Ruan, T.; Zhong, H.; Zhu, J.; Bai, Z. The formation of giant podiform chromitite by asthenospheric melts in supra-subduction zone environments. Nat. Commun. 2021. submitted.
More
© Text is available under the terms and conditions of the Creative Commons Attribution (CC BY) license; additional terms may apply. By using this site, you agree to the Terms and Conditions and Privacy Policy.
Upload a video for this entry
Information
Subjects: Geology; Geochemistry & Geophysics; Mineralogy
Contributor MDPI registered users' name will be linked to their SciProfiles pages. To register with us, please refer to https://encyclopedia.pub/register :
Fei Liu
View Times: 856
Revision: 1 time (View History)
Update Date: 22 Nov 2021
Table of Contents
    1000/1000
    Hot Most Recent
    ScholarVision Creations
    Feedback