L'arc concave zagro-taurique et les arcs convexes taurique et egeen; collision des arcs induits

Brunn, J. H.

doi:10.2113/gssgfbull.s7-xviii.2.553

Cited by 46 publications

(28 citation statements)

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“…Druekman's belief is that faulting had terminated by the mid-Jurassic followed by gradual subsidence. (Brunn et al 1970;Marcoux 1974;Robertson & Woodcock 1982). Early Triassic block-faulting and differential subsidence of a stable epeiric sea area was accompanied by localized volcanism of Pietre verdetype, which is well exposed in the Beyw Hoyran nappes (Monod 1977), followed by more quiescent mid-Triassic pelagic carbonate and radiolarite deposition, prior to renewed major subsidence and volcanism in the Upper Triassic (Carnian-Norian) (Juteau 1975;Robertson & Woodcock 1981;this volume).…”

Section: (I) Levantmentioning

confidence: 99%

Introduction: aspects of the geological evolution of the Eastern Mediterranean

Robertson¹,

Dixon²

1984

503

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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Section: (I) Levantmentioning

confidence: 99%

Introduction: aspects of the geological evolution of the Eastern Mediterranean

Robertson¹,

Dixon²

1984

503

300

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“…The eastern This account is compiled from the following selected sources and review articlesgeneral: Brunn (1976), Laubscher and Bernoulli (1977), Robertson and Woodcock (1980), Rocci et al (1980), Sengör and Yilmaz (1981), Jenkyns (1980b); Cyprus: Ealey and Knox (1975), Lapierre (1975), Lapierre and Rocci (1976), Robertson and Woodcock (1979), Swarbrick (1980), Swarbrick and Robertson (1980); Turkey: Dumont et al (1972), Juteau (1975), Marcoux (1970Marcoux ( , 1974Marcoux ( , 1976, Poisson (1978), Ricou et al (1974), Robertson and Woodcock (1981a, b, c), Waldron (1981); Syria: Delaune-Mayer (1978), , Delaune-Mayer et al, 1977), Delaune-Mayer and Saint-Marc (in press), Parrot (1974), A. H. F. Robertson and N. H. Woodcock (personal communication, 1982); Oman, Zagros Mountains: Coleman (1981), Glennie et al (1973Glennie et al ( , 1974, Graham (1980a, b), Pearce et al (1981), Searle et al (1980), Woodcock and Robertson (1982); Greece (esp. Othris: Aubouin et al (1970), Barton (1976), Baumgartner and Bernoulli (1976), Hynes et al (1972), Price (1977), Smith et al (1975).…”

Section: Eastern Tethysmentioning

confidence: 99%

Jurassic Sedimentation History of Site 534 (Western North Atlantic) and of the Atlantic-Tethys Seaway

Ogg¹,

Roberston²,

Jansa³

1983

Initial Reports of the Deep Sea Drilling Project

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Site 534 reflects a complex interplay of global, basinal, and local influences on sedimentation during the Callovian and Late Jurassic. Rifting and rapid subsidence of the continental margins of the North Atlantic-Tethys seaway occurred during the late Early Jurassic (Sinemurian-Pliensbachian), but rapid spreading between the North American margin (Blake Spur Ridge and magnetic lineation) and the northwest African margin did not commence until the Bathonian or earliest Callovian.Site 534, drilled on marine magnetic anomaly "M-28" of Bryan et al. (1980), was initially about 150 km from either continental margin. The ?middle Callovian basal sediments are dusky red silty marl. Callovian transgression led to active carbonate platforms on the margin, recorded at Site 534 as a rise in the CCD (carbonate compensation depth), then arrival of lime-rich turbidites from the Blake Plateau platform across the Blake Spur Ridge. The host pelagic sediment is greenish black, organic-rich, radiolarian-rich, silty claystone. Hydrothermal activity on the nearby spreading ridge enriched this lower unit in metals. In the Oxfordian, the input of terrestrial silt rapidly diminished; radiolarians or other bioclasts were not preserved. The dark variegated claystone has fine-grained marl and reddish claystone turbidite beds. The late Callovian-Oxfordian Western Tethys has radiolarian chert deposition, marine hiatuses, or organic-rich sediments.The Kimmeridgian and Tithonian had a stable or receding sea level. Near the end of the Jurassic many of the carbonate platforms of the margins were buried beneath prograding fan or alluvial deposits. Carbonate deposition shifted to the deep sea. Site 534 records the deepening of the CCD and ACD (aragonite compensation depth) during the Kimmeridgian and early Tithonian, then a rise of the ACD in the middle Tithonian. Similar trends occurred throughout the Western Tethys-Atlantic. High nannofossil productivity of the seaway led to deposition of very widespread white micritic limestone in the late Tithonian-Berriasian. The underlying sediment had a slower deposition rate of carbonate, therefore its higher clay and associated Fe content produced a red marl. A short sea-level incursion occurred on the Atlantic margins during the Kimmeridgian and is reflected in the Site 534 greenish gray marl unit by numerous turbidite beds of shallow-water carbonates.

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“…3). The location of the basin at the western prolongation of the North Anatolian Fault and its seismotectonic characteristics, implying a dextral strike-slip motion, have been the main argument for an induced basin because of wrench tectonics along the European margin, following the continental collision in the Caucasus area during the Middle Miocene and the subsequent lateral escape of Anatolia (Brunn, 1976;Dewey & Sengor, 1979;LePichon & Angelier, 1979;Armijo et al, 1999;McNeill et al, 2004;Kreemer et al, 2004).…”

Section: Figmentioning

confidence: 99%

“…In this escape model, the Hellenic arc and trench system obtained its differentiated kinematics, curvature, geometry and internal deformation under the push from the Anatolian microplate, itself been pushed away from the collision zone of Arabia and Eurasia (Brunn, 1976;Mercier et al, 1979;LePichon & Angelier, 1981). This model has not taken into consideration the geodynamic situation and changes of the plate boundary at the front of the Hellenic arc in the west but only the plate dynamics in the east.…”

Section: Driving Mechanism(s)mentioning

confidence: 99%