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Incipient boninitic arc crust built on denudated mantle: the Khantaishir ophiolite (western Mongolia)

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Abstract

The ~ 570 Ma old Khantaishir ophiolite is built by up to 4 km harzburgitic mantle with abundant pyroxenites and dunites followed by ~ 2 km of hornblende-gabbros and gabbronorites and by a ~ 2.5 km thick volcanic unit composed of a dyke + sill complex capped by pillow lavas and some volcanoclastics. The volcanics are mainly basaltic andesites and andesites (or boninites) with an average of 58.2 ± 1.0 wt% SiO2, X Mg = 0.61 ± 0.03 (X Mg = molar MgO/(MgO + FeOtot), TiO2 = 0.4 ± 0.1 wt% and CaO = 7.5 ± 0.6 wt% (errors as 2σ). Normalized trace element patterns show positive anomalies for Pb and Sr, a negative Nb-anomaly, large ion lithophile elements (LILE) concentrations between N- and E-MORB and distinctly depleted HREE. These characteristics indicate that the Khantaishir volcanics were derived from a refractory mantle source modified by a moderate slab-component, similar to boninites erupted along the Izu-Bonin-Mariana subduction system and to the Troodos and Betts Cove ophiolites. Most strikingly and despite almost complete outcrops over 260 km2, there is no remnant of any pre-existing MORB crust, suggesting that the magmatic suite of this ophiolite formed on completely denudated mantle, most likely upon subduction initiation. The architecture of this 4–5 km thick early arc crust resembles oceanic crust formed at mid ocean ridges, but lacks a sheeted dyke complex; volcanic edifices are not observed. Nevertheless, low melting pressures combined with moderate H2O-contents resulted in high-Si primitive melts, in abundant hornblende-gabbros and in a fast enrichment in bulk SiO2. Fractional crystallization modeling starting from the observed primitive melts (56.6 wt% SiO2) suggests that 25 wt% pyroxene + plagioclase fractionation is sufficient to form the average Khantaishir volcanic crust. Most of the fractionation happened in the mantle, the observed pyroxenite lenses and layers in and at the top of the harzburgites account for the required cumulate volumes. Finally, the multiply documented occurrence of highly depleted boninites during subduction initiation suggests a causal relationship of subduction initiation and highly depleted mantle. Possibly, a discontinuity between dense fertile and buoyant depleted mantle contributes to the sinking of the future dense subducting plate, while the buoyant depleted mantle of the future overriding plate forms the infant mantle wedge.

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Notes

  1. The following averages are all rotated: stereoplots and the original measurements (Online Resource 1 and Online Resource 9) are provided in the Electronic Appendix.

  2. One volcanic dyke is a completely un-metamorphosed alkali basalt (KT12-53, Electronic Appendix), not co-genetic to the rest of the suite. In analogy to other volcanism in the area it may be of tertiary age.

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Acknowledgements

We thank Lydia Zehnder for the measurement of XRF glass discs and Markus Wälle for assistance with LA-ICP-MS. Thanks to Uyanga Bold and Lkhagva-Ochir Said for helping to organize fieldwork logistics. We are grateful to Peter Kelemen for insightful comments on an early version of the manuscript. Thoughtful and thorough reviews by three anonymous referees were greatly appreciated. The authors were supported by ETH Zurich.

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Correspondence to Omar Gianola.

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Communicated by Timothy L. Grove.

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410_2017_1415_MOESM1_ESM.jpg

Structural data for the volcanics of the Khantaishir ophiolite. Measurements are rotated as the layering observed in the cherts would be in horizontal position. Symbols with bold red rims are for the Taishir massif, whereas normal symbols are for the Naran massif. The rotated orientations for the Moho of Naran and Taishir massifs are also reported (JPEG 589 kb)

410_2017_1415_MOESM2_ESM.jpg

a TAS diagram (Le Maitre 1984) for rocks of the Khantaishir ophiolite. b K2O-SiO2 space (Peccerillo and Taylor 1976). Data for the Mariana backarc basin and Izu-Bonin-Mariana boninites are from GEOROC (georoc.mpch-mainz.gwdg.de/georoc) and PetDB (www.earthchem.org/petdb). Color shading for Khantaishir: magenta = high-Ca boninites, pink = low-Ca boninites and yellow = high-Mg andesites of the andesitic suite. (JPEG 351 kb)

410_2017_1415_MOESM3_ESM.jpg

Comparison between volcanic rocks of the Khantaishir ophiolite and lavas from the Bay of Islands (data from Jenner et al. 1991) and Betts Cove (data from Bédard 1999) ophiolites. Color shading for Khantaishir: magenta = high-Ca boninites, pink = low-Ca boninites and yellow = high-Mg andesites of the andesitic suite. The alkaline dyke cutting the Naran harzburgite, characterized by normalized trace element patterns one order of magnitude higher than other rocks with similar XMg, is also reported. (JPEG 1650 kb)

410_2017_1415_MOESM4_ESM.jpg

Vertical chemical variations within the upper crust of the Khantaishir ophiolite. Color shading for Khantaishir: magenta = high-Ca boninites, pink = low-Ca boninites and yellow = high-Mg andesites of the andesitic suite. Ba, Th, Sr, Y and Eu are normalized to the primitive mantle (McDonough and Sun 1995). Eu* = (Sm x Gd)1/2 (JPEG 464 kb)

410_2017_1415_MOESM5_ESM.jpg

Longitude chemical variations within the upper crust of the Khantaishir ophiolite. Color shading for Khantaishir: magenta = high-Ca boninites, pink = low-Ca boninites and yellow = high-Mg andesites of the andesitic suite. Ba, Th, Sr, Y and Eu are normalized to the primitive mantle (McDonough and Sun 1995). Eu* = (Sm x Gd)1/2 (JPEG 529 kb)

410_2017_1415_MOESM6_ESM.jpg

Comparison of the average primitive melt composition of the Khantaishir ophiolite and average primitive melts from other settings. a Primitive melt compositions for the Khantaishir ophiolite and primitive MORB (Kelemen et al., 2003). b Primitive high-Mg andesites from the Mariana arc (Jagoutz and Schmidt 2013) and primitive high-Ca boninites from the Izu-Bonin arc (data from GEOROC and PetDB). c Primitive melts from the Mariana and Lau backarc basins (data from GEOROC and PetDB). d Primitive melts from the upper pillow lavas of the Troodos ophiolite (data from Simonian and Gass, 1978; Cameron, 1985) (JPEG 1100 kb)

410_2017_1415_MOESM7_ESM.jpg

Elemental ratios for the rocks of the Khantaishir ophiolite. Color shading for Khantaishir: magenta = high-Ca boninites, pink = low-Ca boninites and yellow = high-Mg andesites of the andesitic suite. Lavas for the EPR and the Mariana backarc basin (data from GEOROC and PetDB) are also reported. Data for forearc basalts and transitional lavas are from Reagan et al. (2010). Data for IODP Expedition 351 are from Arculus et al. (2015) and data for IODP Expedition 352 are from Reagan et al. (2015). Data for the Troodos ophiolite were compiled from König et al. (2008) and Regelous et al. (2014). (JPEG 697 kb)

410_2017_1415_MOESM8_ESM.jpg

Histograms illustrating SiO2-content, XMg, Ti/V and Cr concentrations for the volcanics of the Khantaishir ophiolite. As comparison, lavas from present oceanic-related settings and other ophiolites (Troodos and Oman) are also shown. Data for EPR, Mariana backarc basin and Izu-Bonin-Mariana boninites are from GEOROC and PetDB. Troodos ophiolite: Moores and Vine (1971), Simonian and Gass (1978), Cameron (1985), Flower and Levine (1987), Portnyagin et al. (1997). Oman ophiolite: Alabaster et al. (1982), Lippard et al. (1986), Ernewein et al. (1988), Einaudi et al. (2003), Godard et al. (2006) (JPEG 720 kb)

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Gianola, O., Schmidt, M.W., Jagoutz, O. et al. Incipient boninitic arc crust built on denudated mantle: the Khantaishir ophiolite (western Mongolia). Contrib Mineral Petrol 172, 92 (2017). https://doi.org/10.1007/s00410-017-1415-4

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