Structures and kinematics in the northeastern Mediterranean: A study of an irregular plate boundary

Kempler, Ditza; Garfunkel, Zvi

doi:10.1016/0040-1951(94)90202-x

Cited by 94 publications

(78 citation statements)

References 22 publications

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“…Because the Neogene to present plate boundary in the Eastern Mediterranean is found between Cyprus and the Eratosthenes Seamount, we suggested that the Late Cretaceous suture between the Troodos-Baer-Bassit ophiolite belt and the Levant basin was reactivated in relation to this motion of the Anatolian plate ( Fig. 6; Kempler and Garfunkel, 1995). Plate convergence resumed along this segment of the Cypriot Arc through left-lateral oblique relative motion (Kempler and Garfunkel, 1994).…”

Section: Tertiary Evolutionmentioning

confidence: 99%

“…During the Late Cretaceous and early Tertiary period, it was located a few hundred kilometers from the then-active plate boundary (Fig. 6;Kempler, 1994b;Kempler and Garfunkel, 1995). Therefore, the effect of the early stages of Africa-Eurasia convergence on this structure was practically insignificant.…”

Section: Indications For a Mesozoic Originmentioning

confidence: 99%

“…Combined with other geophysical data and with plate kinematic considerations, their analyses enabled us to identify major structural elements of different ages and to suggest a composite model for the origin and evolution of the Eratosthenes structure within the Eastern Mediterranean geologic framework (Kempler and Ben-Avraham, 1987a;Kempler, 1994b;Kempler and Garfunkel, 1995). This model is presented and later examined here in view of the data from Leg 160.…”

Section: The Background Modelmentioning

confidence: 99%

“…Africa-Eurasia plate convergence in the Eastern Mediterranean region was restricted to north of Cyprus throughout early Tertiary time (Kempler, 1994b;Kempler and Garfunkel, 1995). A dramatic change in the regional tectonic regime was associated with the development of major strike-slip systems around the Eastern Mediterranean, first the Dead Sea Transform, in Oligocene/Miocene time, and then the Anatolian Transform Fault System, in late Miocene time (Ketin, 1948;Freund et al, 1968Freund et al, , 1970Garfunkel et al, 1981;¼en-gör et al, 1985;Barka, 1992).…”

Section: Tertiary Evolutionmentioning

confidence: 99%

“…This concept was further integrated into the regional tectonic scheme by Robertson (1990). Several studies have suggested different tectonic models of the Eratosthenes Seamount and have shown that drilling on the seamount has become indispensable to gain further progress in this field (e.g., Hsü, 1992;Kempler and Garfunkel, 1992;Mart et al, 1992;Robertson, 1992). The orthodox view of the Eratosthenes Seamount as a part of the African plate that subducts northward beneath the Anatolian plate and collides with Cyprus, became the working assumption for Ocean Drilling Program (ODP) Leg 160.…”

Section: Introductionmentioning

confidence: 99%

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Eratosthenes Seamount: the possible spearhead of incipient continental collision in the Eastern Mediterranean

Kempler¹

1998

Proceedings of the Ocean Drilling Program

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We compare earlier works, based on available geophysical data and plate kinematic considerations, about the origin and evolution of the Eratosthenes structure within the Eastern Mediterranean tectonic framework, with data from Ocean Drilling Program (ODP) Leg 160. The model under discussion is supported by the ODP data regarding the late evolution of the Eratosthenes Seamount; however, deeper drilling is needed for better understanding of the early history of this structure.Analysis of the available seismic reflection, seismic refraction, and magnetic data in view of the regional geologic history suggests that the deep structure of the Eratosthenes Seamount originated in early Mesozoic time. The ODP data confirm that the Eratosthenes structure, which was located a few hundred kilometers away from the Late Cretaceous/early Tertiary active plate boundary, was not affected by the major tectonic events of that period. The data also reflect the existence of the Eratosthenes structural high already in Late Cretaceous and Eocene times. The ODP data corroborate that the Africa-Anatolia plate boundary was reactivated as the Cypriot Arc, between Cyprus and the Eratosthenes structure, in the late Miocene, through subduction of remnant oceanic lithosphere of the Mesozoic Neotethys beneath Cyprus.The absence of Messinian evaporites on the Eratosthenes Seamount and within the surrounding depression was confirmed by Leg 160 data. Similar data led us to infer that this area formed a Messinian island, which subsided in post-Messinian time. The post-Messinian subsidence shaped the seamount and surrounding natural moat, which in turn are superimposed on the Eratosthenes structural high. The Miocene-Pliocene subduction along the Cypriot Arc changed into collision between Cyprus and the Eratosthenes structure after the elimination of oceanic lithosphere from this junction. The Cyprus-Eratosthenes collision triggered the extreme uplift of southern Cyprus at about 1.5−2 Ma. Pulsed uplift of Cyprus, apparently accompanied by pulsed subsidence of the Eratosthenes area, marks incipient continental collision in the Eastern Mediterranean. The Eratosthenes Seamount, therefore, is the possible spearhead of incipient continental collision and is the best candidate for the study of collisional processes in this area.

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Section: Tertiary Evolutionmentioning

confidence: 99%

Section: Indications For a Mesozoic Originmentioning

confidence: 99%

Section: The Background Modelmentioning

confidence: 99%

Section: Tertiary Evolutionmentioning

confidence: 99%

Section: Introductionmentioning

confidence: 99%

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Eratosthenes Seamount: the possible spearhead of incipient continental collision in the Eastern Mediterranean

Kempler¹

1998

Proceedings of the Ocean Drilling Program

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Longitudinal and Temporal Evolution of the Tectonic Style Along the Cyprus Arc System, Assessed Through 2‐D Reflection Seismic Interpretation

et al. 2018

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The Cyprus Arc system constitutes a major active plate boundary in the eastern Mediterranean region. This structure is directly linked with the northward convergence of the African and Eurasian plates since the Late Cretaceous. Two‐dimensional reflection seismic data were utilized, which image the main plate structures and their lateral evolution south of the island of Cyprus. Interpretation of these data allowed the identification of nine tectono‐sedimentary packages in three different crustal domains south of the Cyprus Arc system: (1) the Levant Basin (attenuated continental crust), (2) the Eratosthenes microcontinent (continental crust), and (3) the Herodotus Basin (oceanic crust). Within these domains, numerous tectonic structures were documented and analyzed in order to understand the mechanism and timing of deformation. In the north, south verging thrusting commenced in early Miocene along the Larnaca and Margat ridges, whereas no activity was identified before middle Miocene along the Latakia Ridge. Thus, the deformation front migrated southward and was accompanied by the development of flexural basins and stratigraphic onlaps as in the Cyprus Basin. The acme of deformation occurred in mid‐late Miocene. A regional unconformity of Pliocene age marks the end of the first deformation sequence. In Plio‐Pleistocene time, the westward escape of the Anatolian microplate resulted in the reactivation of existing structures. The evolution of deformation along the plate boundary is identified from the creation of positive flower structures revealing transpressive movements along the Larnaca and Latakia Ridges (eastern domains), whereas in the Eratosthenes domain a flexural basin highlights a compressive regime.

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The Anaximander Mountains: a clue to the tectonics of southwest Anatolia

2003

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The offshore Anaximander Mountains are an important link between the Hellenic and Cyprus arcs. They were formed by southeastward rifting from Turkey in post‐Miocene time. Gravity data have shown that the eastern part of the Anaximander Mountains is different from the western part; multibeam mapping seems to confirm that the eastern Anaximander Mountains have affinity with the Florence Rise structure (western Cyprus Arc). Faulting along and across the latter feature is characterized in the seismic data by anastomosing faults and pop‐up flower structures. It is likely that progressive adjustment to incipient collision developed into a broad zone of NW–SE transpressive wrenching extending towards south Turkey. In contrast, the western mountains are more directly related to the opening of the Rhodes Basin and the Finike Basin, as transtension may have dominated in southwest Turkey since the Pliocene. The connection with onshore Turkey is still unclear, but could be related to the Fethiye–Burdur Fault Zone that defines the western boundary of the complex Isparta Angle. The Anaximander Mountains and the Isparta Angle form together a tectonic accommodation zone between the active deformation in southwestern Turkey and the Aegean region and the tectonically quieter Cyprus region. Copyright © 2003 John Wiley & Sons, Ltd.

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Structures and kinematics in the northeastern Mediterranean: A study of an irregular plate boundary

Cited by 94 publications

References 22 publications

Eratosthenes Seamount: the possible spearhead of incipient continental collision in the Eastern Mediterranean

Eratosthenes Seamount: the possible spearhead of incipient continental collision in the Eastern Mediterranean

Longitudinal and Temporal Evolution of the Tectonic Style Along the Cyprus Arc System, Assessed Through 2‐D Reflection Seismic Interpretation

The Anaximander Mountains: a clue to the tectonics of southwest Anatolia

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