Isotopic and trace element composition of volcanic glasses from the Akaki Canyon, Cyprus: implications for the origin of the Troodos ophiolite

Rautenschlein, M.; Jenner, George A.; Hertogen, Jan; Hofmann, Albrecht W.; Kerrich, Robert; Schmincke, H.-U.; White, William M.

doi:10.1016/0012-821x(85)90180-3

Cited by 183 publications

(92 citation statements)

References 46 publications

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“…All samples are characterized by similar subparallel shapes of normalized patterns with higher ratios of Large Ion Lithophile Elements (LILE) to Rare Earth Elements (REE), and lower ratios of High Field Strength Elements (HFSE) to REE (except (Ti/REE) compared to Normal Mid Ocean Ridge Basalt (NMORB). These compositions are typical for Troodos lavas (e.g., Rautenschlein et al 1985), and together with elevated H 2 O contents, manifest their SSZ origin. The incompatible element abundances correlate negatively with MgO and for most elements may be accounted for by processes of crystal fractionation/accumulation.…”

Section: Petrography and Chemistrymentioning

confidence: 71%

“…The CaO contents of olivine from this rock are generally higher than those of the UPL olivine (0.16±0.28 wt% in Fo 89±94 ). Rautenschlein et al 1985;Flower and Levine 1987;Taylor 1987;Thy and Xenophontos 1991;Bailey et al 1991;Sobolev et al 1993;Bednarz and Schmincke 1994;Portnyagin unpublished data). The ®eld of homogenized melt inclusions in olivine phenocrysts from type I UPL picrites after Sobolev et al (1993).…”

Section: Mineralogy Of Picrite Trd-150mentioning

confidence: 95%

“…In this respect, the study of well-preserved and exposed suprasubduction zone ophiolites, such as Troodos (e.g., Schmincke et al 1983;Robinson et al 1983;McCulloch and Cameron 1983;Rautenschlein et al 1985;Cameron 1985;Rogers et al 1989), may provide additional constraints on the evolution of the SSZ magmatism in extensional settings.…”

Section: Introductionmentioning

confidence: 99%

“…Despite certain mineralogical and geochemical di erences among UPL rocks which led to their division into several types (e.g., Cameron 1985), the UPL as a whole represent a distinct magmatic group. They are characterized by the presence of high-forsteritic olivine phenocrysts (up to Fo 94 ), chromium-rich spinel {Cr# = 100*[Cr/(Cr + Al)] = 65±80}, an absence of plagioclase phenocrysts in all rock types but basaltic andesites, low TiO 2 (`1 wt%) and high H 2 O contents ($2 wt%), and trace element contents typical of subduction-related magmas (e.g., McCulloch and Cameron 1983;Rautenschlein et al 1985;Cameron 1985;Sobolev et al 1993). The petrological and geochemical features of the UPL have been used as a reference type for the high-Ca boninite magmatic suite (Crawford et al 1989).…”

Section: Introductionmentioning

confidence: 99%

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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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Section: Petrography and Chemistrymentioning

confidence: 71%

Section: Mineralogy Of Picrite Trd-150mentioning

confidence: 95%

Section: Introductionmentioning

confidence: 99%

Section: Introductionmentioning

confidence: 99%

See 2 more Smart Citations

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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“…, Cameron [1985], Hebert and Laurent [1990], Kay and Senechal [1976], Kidd and Cann [1974], Laurent [1990], Malpas [1990], Malpas and Langdon [1984], Malpas et al [1990], McCulloch and Cameron [1983], Miyashiro [1973Miyashiro [ , 1975aMiyashiro [ , 1975b, Moores [1975], Rautenschlein et al [1985], Robertson [1977], Robinson and Malpas [1990], Robinson et al [1983], Schmincke et al [1983], Schmincke and Bednarz [1990], Staudigel et al [1999], Taylor [1990] Semail (Oman) Alabaster et al [1982], Benn et al [1988], Bernoulli et al [1990], Boudier and Coleman [1981], Nicolas [1988, 1995] Robertson [1989], , Schiffman et al [1991], Shervais [1990], Kimbrough [1985a, 1985b] …”

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confidence: 99%

Birth, death, and resurrection: The life cycle of suprasubduction zone ophiolites

Shervais

2001

Geochem Geophys Geosyst

449

275

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[1] Abstract: Suprasubduction zone (SSZ) ophiolites display a consistent sequence of events during their formation and evolution that suggests that they form in response to processes that are common to all such ophiolites. This sequence includes the following: (1) birth, which entails the formation of the ophiolite above a nascent or reconfigured subduction zone; this stage is typically characterized by the eruption of arc tholeiite lavas and the formation of layered gabbros and sheeted dike complex; (2) youth, during which is continued melting of refractory asthenosphere (depleted during birth) occurs in response to fluid flux from the subducting slab, with extensional deformation of the older plutonic suite, eruption of refractory lavas, and the intrusion of wehrlite-pyroxenite; (3) maturity, with the onset of semistable arc volcanism, typically calc-alkaline, as the subduction zone matures and stabilizes, and the intrusion of quartz diorite and eruption of silicic lavas; and (4) death, which is the sudden demise of active spreading and ophiolite-related volcanism, which in many cases is linked to collision with an active spreading center and the onset of shallow underthrusting of the buoyant spreading axis; expressed as dikes and lavas with oceanic basalt compositions that crosscut or overlie rocks of the older suites; (5) resurrection, with emplacement by obduction onto a passive margin or accretionary uplift with continued subduction. The early stages (1± 3) may be diachronous, and each stage may overlap in both time and space. The existence of this consistent progression implies that ophiolite formation is not a stochastic event but is a natural consequence of the SSZ tectonic setting.

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A Mineralogical, Geochemical and Thermal Profile Through the Agrokipia “B” Hydrothermal Sulfide Deposit, Troodos Ophiolite Complex, Cyprus

Herzig

1988

Base Metal Sulfide Deposits in Sedimentary and Volcanic Environments

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Isotopic and trace element composition of volcanic glasses from the Akaki Canyon, Cyprus: implications for the origin of the Troodos ophiolite

Cited by 183 publications

References 46 publications

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

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

Birth, death, and resurrection: The life cycle of suprasubduction zone ophiolites

A Mineralogical, Geochemical and Thermal Profile Through the Agrokipia “B” Hydrothermal Sulfide Deposit, Troodos Ophiolite Complex, Cyprus

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