The geochemistry and petrogenesis of an ophiolitic sequence from Pindos, Greece

Capedri, S.; Venturelli, G.; Bocchi, G.; Dostál, J.; Garuti, Giorgio; Rossi, Antonio

doi:10.1007/bf01132004

Cited by 90 publications

(31 citation statements)

References 42 publications

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“…3), dated as Late Triassic, based on conodonts from conformably overlying pelagic sediments (Kostopoulos, 1989). Abundant high-Ti MORB-type sheeted dykes and extrusives (Table 1) are also found at the basal part of the preserved ophiolite slices of the Aspropotamos Complex (see below ;Capedri et aL, 1980;Kostopoulos, 1989), but their age is uncertain . These basal units could therefore represent either: i) Late Triassic MORB-type crust, which was subsequently intruded by the products of later subduction-related magmatism (see below); or ii) younger Jurassic crust formed immediately prior to, or during, subductioninfluenced spreading.…”

Section: B) Early Spreading Stagementioning

confidence: 96%

Genesis and Emplacement of the Supra-Subduction Zone Pindos Ophiolite, Northwestern Greece

Jones

Robertson

Cann

1991

Ophiolite Genesis and Evolution of the Oceanic Lithosphere

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The north Pindos Mountains of mainland Greece expose a series of thrust sheets, which were emplaced towards the southwest during the Early Tertiary. The Jurassic Pindos ophiolite forms the upper part of this assemblage, and reveals a complex history, interpreted as mainly the result of suprasubduction zone spreading processes. Ophiolitic thrust sheets are additionally found structurally beneath the main peridotite body, and contain variable volcanic sequences, including units of island arc tholeiitic and boninitic affinities. The metamorphic sole formed in response to overthrusting of the young, hot, ophiolite, followed by emplacement onto the Pelagonian continental margin to the east. During the Cretaceous, the Pindos ocean existed as a remnant basin to the west of the emplaced ophiolite, and was infilled by deep marine sediments. During final Late Eocene collision, the Cretaceous sediments and Tertiary foreland basin deposits, were overthrust by the Pindos ophiolite and underlying thrust sheets, then emplaced onto Apulia to the southwest.

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Section: B) Early Spreading Stagementioning

confidence: 96%

Genesis and Emplacement of the Supra-Subduction Zone Pindos Ophiolite, Northwestern Greece

Jones

Robertson

Cann

1991

Ophiolite Genesis and Evolution of the Oceanic Lithosphere

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“…In Greece, ophiolite occurrences have been extensively studied by prominent researchers who have proposed different theories and models for interpreting their formation (e.g. Capedri et al 1980Capedri et al , 1985Beccaluva et al 1984;Magganas and Economou 1988;Magganas 2002;Robertson 2002Robertson , 2004Smith and Rassios 2003;Pe-Piper et al 2004;Papanikolaou 2009;Bortolotti et al 2013;Robertson et al 2013). Two long-standing scenarios have been proposed to explain their derivation, which are mostly based on their emplacement tectonic features, as well as on their different lithological and geochemical types and characters.…”

Section: Introductionmentioning

confidence: 99%

“…The MORB-OIB array is projected according toPearce (2008). For comparison, compositional fields show the volcanic rocks from West Othris(Bortolotti et al 2008;Barth and Gluhak 2009), Pindos(Capedri et al 1980;Pe-Piper et al 2004;Saccani and Photiades 2004), Rhodiani(Saccani et al 2008a), Vermion-Veria(Saccani et al 2008b), Alonissos and Kyra Panagia islands(Pe-Piper et al 1996), East Thessaly…”

mentioning

confidence: 99%

Boninitic and tholeiitic basaltic lavas and dikes from dispersed Jurassic East Othris ophiolitic units, Greece: petrogenesis and geodynamic implications

Koutsovitis

Magganas

2016

International Geology Review

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Pillow lavas, massive lava flows, and sub-volcanic dikes of tholeiitic basaltic composition are found to be members of the Vrinena, Aerino, Eretria, and Velestino dispersed Middle-Upper Jurassic ophiolitic units in East Othris. The Vrinena and Eretria ophiolitic units appear to have been emplaced onto the Pelagonian continental margin during the Upper Jurassic-Lower Cretaceous, whereas the Aerino and Velestino units seem to have been finally emplaced during postPalaeocene times. Geochemically these are divided into two groups: Group I includes subduction-related boninites and low-Ti basalts from the Vrinena and Aerino units, and Group II high-Ti basalts show spreading-type characteristics occurring in the Eretria and Velestino units. Primary magma of the Group I volcanics appears to have been formed after high partial melting degrees (~18%) of a highly depleted harzburgitic mantle source, under relatively high temperatures (mantle potential temperature~1372°C). Petrogenetic modelling also suggests that the primary magma of the Group II volcanics were formed after lower partial melting degrees (~7%) of a moderately depleted mantle source. The petrological and geochemical data from the East Othris dispersed and diversely emplaced ophiolitic units provide evidence of a common intra-oceanic supra-subduction zone (SSZ) origin within the Pindos oceanic strand of the Western Tethys. Specifically, Group I lavas and dikes from Vrinena seem to represent the extrusive part of an almost complete fore-to island-arc ophiolitic sequence. Dikes of Aerino most likely correspond to fore-arc magmatic material that intruded within exhumed serpentinized ultramafic rocks through a subduction channel that developed close to the slab and towards the fore-arc and the accretionary prism. The Group II volcanics either corresponded to a fore-arc magmatic expression, which extruded earlier than Group I volcanics and prior to the establishment of a mature subduction zone, or represent back-arc to island-arc magmatism that was contemporaneous to the fore-arc magmatic activity during rollback subduction. ARTICLE HISTORY

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“…Capedri et al 1980Capedri et al , 1982Noiret et al 1981). Relative enrichment in large-ionlithophile elements (LIL, e.g.…”

Section: (Ii) the Chemical Evidencementioning

confidence: 99%

Introduction: aspects of the geological evolution of the Eastern Mediterranean

Robertson¹,

Dixon²

1984

496

300

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SUMMARY: We review extensively the evidence and arguments bearing on the nature of Palaeotethys in relation to the age of formation, location and multiplicity of Neotethyan strands and their fate. We conclude that Palaeotethys did not die early but was only finally subducted northwards in the Tertiary along the Vardar-Intra Pontide-East Anatolian suture. Neotethyan strands must have opened into it at all times. The Adriatic promontory remained attached to Africa but rotated anti-clockwise in the mid-Tertiary. The Ponfldes are considered to be Eurasian and the Cimmerides are viewed as a 'collage terrain' formed along an oblique-convergence margin. The south Aegean, Greek and Turkish microcontinental blocks were rifted-off Gondwana in the Triassic but formation of braided Neotethyan oceanic crustal strands was essentially confined to mid-Jurassic in the Hellenides and to the Cretaceous in Turkey.We propose a new model of ophiolite genesis by asymmetrical spreading-ridge collapse in an attempt to explain both arc-like ophiolite chemistry prior to major volcanic arc edifice construction, and the synchroneity of sub-ophiolite metamorphic sole formation with Atlantic opening phases.Jurassic dispersal of Hellenide blocks had little effect in the unexpanded Turkish mosaic, but northwards Cretaceous opening of Tauride Neotethyan strands caused oblique collision deformation in the Pelagonian zone and unresolvable complexity in the Aegean. Late Cretaceous and Tertiary arc-volcanism was related in part to continuing Palaeotethyan subduction, and in part to Neotethyan destruction initiated after ridgecollapse. Diachronous collisions ensued from the Late Cretaceous onwards but significant oceanic tracts must have persisted at least to Mid-Tertiary to satisfy Africa-Eurasia separation constraints determined from Atlantic anomaly fitting. Our favoured plate evolutionary model is presented in 7 sketch-maps.

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The geochemistry and petrogenesis of an ophiolitic sequence from Pindos, Greece

Cited by 90 publications

References 42 publications

Genesis and Emplacement of the Supra-Subduction Zone Pindos Ophiolite, Northwestern Greece

Genesis and Emplacement of the Supra-Subduction Zone Pindos Ophiolite, Northwestern Greece

Boninitic and tholeiitic basaltic lavas and dikes from dispersed Jurassic East Othris ophiolitic units, Greece: petrogenesis and geodynamic implications

Introduction: aspects of the geological evolution of the Eastern Mediterranean

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