The petrogenesis of high-calcium boninite lavas dredged from the northern Tonga ridge

Falloon, Trevor J.; Crawford, Anthony J.

doi:10.1016/0012-821x(91)90030-l

Cited by 179 publications

(125 citation statements)

References 34 publications

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“…Th/La = 13.9-41.7 × N-MORB). These boninites are similar to the Ca-boninites of Falloon & Crawford (1991). A late microgabbroic dyke injected into the Haji-Abad mantle sequence (HG10-30) is compositionally similar to boninitic lavas.…”

Section: A3 Haji-abad Ophiolitementioning

confidence: 71%

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Geodynamic evolution of Upper Cretaceous Zagros ophiolites: formation of oceanic lithosphere above a nascent subduction zone

2011

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-The Zagros fold-and-thrust belt of SW Iran is a young continental convergence zone, extending NW-SE from eastern Turkey through northern Iraq and the length of Iran to the Strait of Hormuz and into northern Oman. This belt reflects the shortening and off-scraping of thick sediments from the northern margin of the Arabian platform, essentially behaving as the accretionary prism for the Iranian convergent margin. Distribution of Upper Cretaceous ophiolites in the Zagros orogenic belt defines the northern limit of the evolving suture between Arabia and Eurasia and comprises two parallel belts: (1) Outer Zagros Ophiolitic Belt (OB) and (2) Inner Zagros Ophiolitic Belt (IB). These belts contain complete (if disrupted) ophiolites with well-preserved mantle and crustal sequences. Mantle sequences include tectonized harzburgite and rare ultramafic-mafic cumulates as well as isotropic gabbro lenses and isolated dykes within the harzburgite. Crustal sequences include rare gabbros (mostly in IB ophiolites), sheeted dyke complexes, pillowed lavas and felsic rocks. All Zagros ophiolites are overlain by Upper Cretaceous pelagic limestone. Limited radiometric dating indicates that the OB and IB formed at the same time during Late Cretaceous time. IB and OB components show strong suprasubduction zone affinities, from mantle harzburgite to lavas. This is shown by low whole-rock Al 2 O 3 and CaO contents and spinel and orthopyroxene compositions of mantle peridotites as well as by the abundance of felsic rocks and the trace element characteristics of the lavas. Similarly ages, suprasubduction zone affinities and fore-arc setting suggest that the IB and OB once defined a single tract of fore-arc lithosphere that was disrupted by exhumation of subducted Sanandaj-Sirjan Zone metamorphic rocks. Our data for the OB and IB along with better-studied ophiolites in Cyprus, Turkey and Oman compel the conclusion that a broad and continuous tract of fore-arc lithosphere was created during Late Cretaceous time as the magmatic expression of a newly formed subduction zone developed along the SW margin of Eurasia.

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Section: A3 Haji-abad Ophiolitementioning

confidence: 71%

“…The Oman V1 (Geotimes unit) and V2 (Lasail unit) lavas follow the Zagros Bagci, Parlak & Hock, 2008). North Tonga boninites from Falloon & Crawford (1991); IBM fore-arc boninites from Arculus et al (1992). (c) Th/Yb v. Nb/Yb diagram (after Leat et al 2004) for OB and IB ophiolites.…”

Section: A Summary Of Upper Cretaceous Zagros Ophiolite Compositiomentioning

confidence: 99%

Geodynamic evolution of Upper Cretaceous Zagros ophiolites: formation of oceanic lithosphere above a nascent subduction zone

2011

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“…Another combination of broadly contemporaneous backarc tholeiites and high-Ca boninites associated with propagation of backarc spreading into arc lithosphere, has been described from the northern termination of the Tonga Ridge (e.g., Falloon and Crawford 1991;Danyushevsky et al 1995). The Tongan high-Ca boninites, similar to the UPL in compositions of primary melts and PT parameters of their origin in the mantle Sobolev and Danyushevsky 1994;Danyushevsky et al 1995), are formed as hot residual Samoan plume mantle intruded above the slab and subsequently re-melted due to interaction with the subduction-related component (Danyushevsky et al 1995).…”

Section: Possible Modern Analogs For the Troodos Ophiolitementioning

confidence: 99%

Coexistence of two distinct mantle sources during formation of ophiolites: a case study of primitive pillow-lavas from the lowest part of the volcanic section of the Troodos Ophiolite, Cyprus

Portnyagin

Danyushevsky²,

Kamenetsky³

1997

Contributions to Mineralogy and Petrology

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We present a detailed mineralogical, petrological and melt inclusion study of unusually fresh, primitive olivine + clinopyroxene phyric Lower Pillow Lavas (LPL) found near Analiondas village in the northeastern part of the Troodos ophiolite (Cyprus). Olivine phenocrysts in these primitive LPL show a wide compositional range (Fo 82±92 ) and have higher CaO contents than those from the Upper Pillow Lavas (UPL). Cr-spinel inclusions in olivine are signi®cantly less Cr-rich (Cr/Cr + Al = 28±67 mol%) compared to those from the UPL (Cr# = 70±80). These features reect di erences in melt compositions between primitive LPL and the UPL, namely higher CaO and Al 2 O 3 and lower FeO* compared to the UPL at a given MgO. LPL parental melts (in equilibrium with Fo 92 ) had $10.5 wt% MgO and crystallization temperatures $1210°C, which are signi®cantly lower than those previously published for the UPL (14±15 wt% MgO and $1300°C for Fo 92 ). The fractionation path of LPL parental melts is also di erent from that of the UPL. It is characterized initially by olivine + clinopyroxene cotectic crystallization joined by plagioclase at $9 wt% MgO, whereas UPL parental melts experienced a substantial interval of olivine-only crystallization. Primitive LPL melts were formed from a mantle source which was more fertile than that of tholeiites from well-developed intra-oceanic arcs, but broadly similar in its fertility to that of MidOcean Ridge Basalt (MORB) and Back Arc Basin Basalts (BABB). The higher degrees of melting during formation of the LPL primary melts compared to average MORB were caused by the presence of subduction-related components (H 2 O). Our new data on the LPL coupled with existing data for the UPL support the existing idea that the LPL and UPL primary melts originated from distinct mantle sources, which cannot be related by progressive source depletion. Temperature di erences between these sources ($150°C), their position in the mantle ($10 kbar for the colder LPL source vs 15±18 kbar for the UPL source), and temporal succession of Troodos volcanism, all cannot be reconciled in the framework of existing models of mantle wedge processes, thermal structure and evolution, if a single mantle source is invoked. Possible tectonic settings for the origin of the Troodos ophiolite (forearc regions of intra-oceanic island arc, propagation of backarc spreading into arc lithosphere) are discussed.

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“…SHMB is rare, even in Archean greenstone belts (Smithies et al, 2004a;Srivastava, 2006Srivastava, , 2008Srivastava et al, 2010), and is characterized by high MgO (>8%) and SiO 2 (51-55%), and low TiO 2 (<0.5%) and HFSE contents (Redman and Keays, 1985;Hall and Hughes, 1987;Cadman et al, 1997;Srivastava and Singh, 1999;Smithies, 2002;Smithies et al, 2004a,b;Gao and Zhou, 2013). Such signatures are comparable to common Phanerozoic boninites (Sun and Nesbitt, 1978;Cameron et al, 1979;Crawford et al, 1989;Falloon and Crawford, 1999). However, concluded that some main differences are evident between SHMB and Phanerozoic boninites, such as the absence of U-shaped REE patterns and positive Zr spikes in the former.…”

Section: Introductionmentioning

confidence: 93%

“…According to previous studies, the following tectonic settings can provide both the intense hydration and the elevated temperatures (up to 1350 • C) that are required to trigger partial melting of refractory mantle peridotite in order to generate boninitic rocks (Sun and Nesbitt, 1978;Beccaluva and Serri, 1988;Falloon and Danyushevsky, 2000): (1) initiation of a subduction zone along either a spreading center or a transfer fault (e.g., Falloon and Crawford, 1991;Ishikawa et al, 2002); (2) ridge subduction (e.g., Crawford et al, 1989;Piercey et al, 2001;Bourdon et al, 2003); (3) subduction of oceanic lithosphere beneath young hot oceanic lithosphere and back-arc basin openings (e.g., Coish et al, 1982;Tatsumi and Maruyama, 1989); (4) plume-island arc interaction (e.g., Danyushevsky et al, 1995;Kerrich et al, 1998;Boily and Dion, 2002;Falloon et al, 2008); and (5) extension of Pearce, 1983). Symbols and data as in Fig.…”

Section: Petrogenetic Modelmentioning

confidence: 99%

Neoarchean siliceous high-Mg basalt (SHMB) from the Taishan granite–greenstone terrane, Eastern North China Craton: Petrogenesis and tectonic implications

Peng

Wilde

et al. 2013

Precambrian Research

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The petrogenesis of high-calcium boninite lavas dredged from the northern Tonga ridge

Cited by 179 publications

References 34 publications

Geodynamic evolution of Upper Cretaceous Zagros ophiolites: formation of oceanic lithosphere above a nascent subduction zone

Geodynamic evolution of Upper Cretaceous Zagros ophiolites: formation of oceanic lithosphere above a nascent subduction zone

Coexistence of two distinct mantle sources during formation of ophiolites: a case study of primitive pillow-lavas from the lowest part of the volcanic section of the Troodos Ophiolite, Cyprus

Neoarchean siliceous high-Mg basalt (SHMB) from the Taishan granite–greenstone terrane, Eastern North China Craton: Petrogenesis and tectonic implications

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