Bedrock Geologic Map of the Greater Lefkosia Area, Cyprus

Harrison, Richard W.; Newell, Wayne L.; Panayides, I.; Stone, Byron D.; Tsiolakis, Efthymios; Necdet, Mehmet; Batihanli, Hilmi; Ozhur, Ayse; Lord, Alan; Berksoy, Okan; Zomeni, Zomenia; Schindler, J. Stephen

doi:10.3133/sim3046

Cited by 12 publications

(15 citation statements)

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“…Ophiolite and slower wave speed underlying Anatolian continental crust (Mackenzie et al 2006;Feld et al 2017) may introduce receiver function complexity. Terrestrial sediments of thickness ∼3 km (Harrison et al 2008) surrounding the ophiolite may also generate additional P-to-S conversions (Fig. 1c).…”

Section: A S E S T U Dy 2 -T H E E T H I O P I a N T R A P S : N E mentioning

confidence: 99%

A reappraisal of the H–κ stacking technique: implications for global crustal structure

Ogden

Bastow

Gilligan

et al. 2019

Geophysical Journal International

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SUMMARY H–κ stacking is used routinely to infer crustal thickness and bulk-crustal VP/VS ratio from teleseismic receiver functions. The method assumes that the largest amplitude P-to-S conversions beneath the seismograph station are generated at the Moho. This is reasonable where the crust is simple and the Moho marks a relatively abrupt transition from crust to mantle, but not if the crust–mantle transition is gradational and/or complex intracrustal structure exists. We demonstrate via synthetic seismogram analysis that H–κ results can be strongly dependent on the choice of stacking parameters (the relative weights assigned to the Moho P-to-S conversion and its subsequent reverberations, the choice of linear or phase-weighted stacking, input crustal P-wave velocity) and associated data parameters (receiver function frequency content and the sample of receiver functions analysed). To address this parameter sensitivity issue, we develop an H–κ approach in which cluster analysis selects a final solution from 1000 individual H–κ results, each calculated using randomly selected receiver functions, and H–κ input parameters. 10 quality control criteria that variously assess the final numerical result, the receiver function data set, and the extent to which the results are tightly clustered, are used to assess the reliability of H–κ stacking at a station. Analysis of synthetic data sets indicates H–κ works reliably when the Moho is sharp and intracrustal structure is lacking but is less successful when the Moho is gradational. Limiting the frequency content of receiver functions can improve the H–κ solutions in such settings, provided intracrustal structure is simple. In cratonic Canada, India and Australia, H–κ solutions generally cluster tightly, indicative of simple crust and a sharp Moho. In contrast, on the Ethiopian plateau, where Palaeogene flood-basalts overlie marine sediments, H–κ results are unstable and erroneous. For stations that lie on thinner flood-basalt outcrops, and/or in regions where Blue Nile river incision has eroded through to the sediments below, limiting the receiver function frequency content to longer periods improves the H–κ solution and reveals a 6–10 km gradational Moho, readily interpreted as a lower crustal intrusion layer at the base of a mafic (VP/VS = 1.77–1.87) crust. Moving off the flood-basalt province, H–κ results are reliable and the crust is thinner and more felsic (VP/VS = 1.70–1.77), indicating the lower crustal intrusion layer is confined to the region covered by flood-basaltic volcanism. Analysis of data from other tectonically complex settings (e.g. Japan, Cyprus) shows H–κ stacking results should be treated cautiously. Only in regions of relatively simple crust can H–κ stacking analysis be considered truly reliable.

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Section: A S E S T U Dy 2 -T H E E T H I O P I a N T R A P S : N E mentioning

confidence: 99%

A reappraisal of the H–κ stacking technique: implications for global crustal structure

Ogden

Bastow

Gilligan

et al. 2019

Geophysical Journal International

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“…Recent P wave tomography interpretations largely support these geodynamic interpretations, including a large tear between the Cyprus and Aegean slabs, a minor tear between western Cyprus and the Isparta Angle (approximately along the Paphos transform (PT), Figure 1), and apparently no slab to the east of Cyprus [ Biryol et al , 2011]. Some authors have suggested that Cyprus itself overlies a locked portion of the subduction zone [e.g., Harrison et al , 2008]. Such locking may be linked to the collision of the Erathosthenes Seamount with the Cyprus Arc, as the collision appears to have induced structural changes throughout the E Mediterranean [ Schattner , 2010].…”

Section: Geologic and Tectonic Settingmentioning

confidence: 99%

Surface expression of eastern Mediterranean slab dynamics: Neogene topographic and structural evolution of the southwest margin of the Central Anatolian Plateau, Turkey

et al. 2012

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The southwest margin of the Central Anatolian Plateau has experienced multiple phases of topographic growth, including the formation of localized highs prior to the Late\ud Miocene that were later affected by wholesale uplift of the plateau margin. Our new biostratigraphic data limit the age of uplifted marine sediments at the southwest plateau margin at 1.5 km elevation to <7.17 Ma, and regional lithostratigraphic correlations\ud imply that the age is <6.7 Ma. Single-grain CA-TIMS U-Pb zircon analyses from a reworked ash within the marine sediments yield dates as young as 10.6 Ma, indicating a maximum age that is consistent with the biostratigraphy. Our structural measurements within the uplifted region and fault inversion modeling agree with previous findings in surrounding regions, with early contraction followed by strike-slip and extensional deformation during uplift. Focal mechanisms from shallow earthquakes show that the extensional phase has continued to the present. Broad similarities in the change in the\ud tectonic stress regime (after 8 Ma) and the onset of surface uplift (after 7 Ma) imply that deep-seated process(es) caused post-7 Ma uplift. The geometry of lithospheric slabs beneath the plateau margin, Pliocene to recent alkaline volcanism, and the uplift pattern with\ud accompanying normal faulting point toward slab tearing and localized heating at the base of\ud the lithosphere as a probable mechanism for post-7 Ma uplift of the southwest margin. Considering previous work in the region, there appears to be an important link between slab dynamics and surface uplift throughout the Anatolian Plateau’s southern margin

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“…Calon et al () identified that the Larnaca Ridge is uplifted in Middle to late Miocene time as the sediments are thick toward the north (away from the Ridge) but thin rapidly toward the Ridge. Mid‐Miocene thrusting activity is also identified onshore in the Mesaoria Basin (Cleintuar et al, ; Harrison et al, ) as the Ovgos Fault zone is thrusting the deeper Kythrea flysch Formation next to the shallower pelagic marls and chalks of the Pakhna Formation (Cleintuar et al, ).…”

Section: Discussionmentioning

confidence: 97%

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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Bedrock Geologic Map of the Greater Lefkosia Area, Cyprus

Cited by 12 publications

References 0 publications

A reappraisal of the H–κ stacking technique: implications for global crustal structure

A reappraisal of the H–κ stacking technique: implications for global crustal structure

Surface expression of eastern Mediterranean slab dynamics: Neogene topographic and structural evolution of the southwest margin of the Central Anatolian Plateau, Turkey

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

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