Strike-Slip faults

Sylvester, Arthur G.

doi:10.1130/spe253-p205

Cited by 132 publications

(188 citation statements)

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“…Such a large-scale restraining stepover has so far not been described from Poland, although similar structures have been widely recognized all over the world (e.g., Sylvester 1988;Wakabayashi et al 2004 Table 1. Historical earthquake epicentres in the Holy Cross Mountains region based on Shebalin et al (1998) and Guterch (2015).…”

Section: Discussionmentioning

confidence: 99%

“…The investigations have shown that strikeslip faulting plays a significant role in intercontinental deformation within e.g., collisional 'mobile' belts and inverted sedimentary basins (for discussion see e.g., Moody and Hill 1956;Sylvester 1988;Woodcock and Schubert 1994 and citations therein). Strike-slip structures need the precise identification of diagnostic tectonic structures that formed as a result of the strikeMnin restraining stepover -evidence of significant Cretaceous-Cenozoic dextral strike-slip faulting along the Teisseyre-Tornquist Zone?…”

Section: Introductionmentioning

confidence: 99%

“…Other structures useful for the precise identification of strike-slip movements in vertical cross-sections and on seismic profiles, as well as on geological maps and satellite images are: flower structures (e.g., Wilcox et al 1973), folds with a helicoidal geometry of the axial surfaces in restraining stepovers (Sylvester 1988;Babaahmadi et al 2010;Nadimi and Konon 2012), especially when they form an en échelon arrangement (Moody and Hill 1956;Jamison 1991;Woodcock and Schubert 1994), and vertical-axis rotated tectonic blocks bounded by major strike-slip faults (Woodcock and Fisher 1986;Mandl 1987;Sylvester 1988;Peacock et al 1998;Woodcock and Rickards 2003;Kim et al 2004;Konon 2007;Nadimi and Konon 2012). Apart from map-scale structures, identification of minor structures associated with major faults, such as slickensides observed within the near-surface parts of fault zones, horsetail splays, wing cracks or antithetic faults at the terminations of major faults, also demonstrate the presence of strike-slip movements.…”

Section: Introductionmentioning

confidence: 99%

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Mnin restraining stepover – evidence of significant Cretaceous–Cenozoic dextral strike-slip faulting along the Teisseyre-Tornquist Zone?

Konon¹,

Ostrowski²,

Rybak-Ostrowska³

et al. 2016

Acta Geologica Polonica

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ABSTRACT:Konon, A., Ostrowski, S., Rybak-Ostrowska, B., Ludwiniak, M., Śmigielski, M., Wyglądała, M., Uroda, J., Kowalczyk, S., Mieszkowski, R. and Kłopotowska, A. 2016. Mnin restraining stepover -evidence of significant Cretaceous-Cenozoic dextral strike-slip faulting along the Teisseyre-Tornquist Zone? Acta Geologica Polonica, 66 (3), 429-449. Warszawa.A newly recognized Mnin restraining stepover is identified in the Permo-Mesozoic cover of the western part of the Late Palaeozoic Holy Cross Mountains Fold Belt (Poland), within a fault pattern consisting of dextral strikeslip faults. The formation of a large contractional structure at the Late Cretaceous -Cenozoic transition displays the significant role of strike-slip faulting along the western border of the Teisseyre-Tornquist Zone, in the foreland of the Polish part of the Carpathian Orogen. Theoretical relationships between the maximum fault offsets/mean step length, as well as between the maximum fault offsets/mean step width allowed the estimation of the values of possible offsets along the Snochowice and Mieczyn faults forming the Mnin stepover. The estimated values suggest displacements of as much as several tens of kilometres. The observed offset along the Tokarnia Fault and theoretical calculations suggest that the strike-slip faults west of the Late Palaeozoic Holy Cross Mountains Fold Belt belong to a large strike-slip fault system.We postulate that the observed significant refraction of the faults forming the anastomosing fault pattern is related also to the interaction of the NW-SE-striking faults formed along the western border of the TeisseyreTornquist Zone and the reactivated WNW-ESE-striking faults belonging to the fault systems of the northern margin of the Tethys Ocean.

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Section: Discussionmentioning

confidence: 99%

Section: Introductionmentioning

confidence: 99%

Section: Introductionmentioning

confidence: 99%

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Mnin restraining stepover – evidence of significant Cretaceous–Cenozoic dextral strike-slip faulting along the Teisseyre-Tornquist Zone?

Konon¹,

Ostrowski²,

Rybak-Ostrowska³

et al. 2016

Acta Geologica Polonica

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“…These folds are generally confined to a narrow but persistent zone adjacent to a major fault (Sylvester, 1988). The en echelon anticlines and synclines have a mean axial trace of 029°N, explained by left simple shear.…”

Section: General Basin Characteristicsmentioning

confidence: 99%

“…Structural elements and internal basin geometry make possible the interpretation of basin-forming processess in strike-slip basins (Sylvester, 1988;Ringenbach and others, 1993). These fault-bounded basins are generated by a larger spectrum of deformation commonly associated with crustal-scale movements (Christie-Blick and Biddle, 1985;Ringenbach and others, 1993).…”

Section: General Basin Characteristicsmentioning

confidence: 99%

Implications of an archean strike-slip basin :

Corcoran¹

1996

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RESUMELa formation de Beaulieu Rapids est une séquence sédimentaire de 0,2 à 1 km d'épaisseur située au centre-sud de la Province structurale de l'Esclave. La formation représente un bassin en décrochement archéen qui s'est développé le long d'une faille majeure de direction NS. Des petits plutons de porphyres quartzo-feldspathiques à hornblende sont localisés le long de la zone de faille. Des datations U-Pb sur zircons donnent un âge approximatif de 2.6 Ga pour ces plutons. La présence de fragments de porphyres dans les conglomérats indique que la formation de Beaulieu Rapids doit conséquemment être plus jeune que cet âge. La marge ouest du basin est caractérisée par une discordance que sépare la ceinture volcanique de Rivière Beaulieu de la succession sédimentaire. Des failles NE tardives sont présentes sur les bordures nord et sud du bassin.Structuralement, la formation est caractérisée par une foliation penetrative NNE et par des plis en échelons dont l'orientation dominante est aussi NNE. Les plis se présentent sous la forme d'une alternance d'anticlinaux et de synclinaux localisés majoritairement dans la partie nord du bassin. Dans ce secteur, la direction de la polarité change rapidement alors que dans la partie sud du bassin les lits sont de direction nord avec une polarité généralement vers l'est. Quelques lits sont renversés mais les lits normaux sont plus communs.Les roches sédimentaires du bassin de Beaulieu Rapids montrent deux cycles positifs qui indiquent un contrôle tectonique sur la sédimentation. Le premier cycle est représenté par l'association de faciès du conglomérat I (CFA-I: Conglomerate faciès association I) et le faciès de siltstone-grès sus-jacent (SSFA: Siltstone-sandstone faciès association). L'association de faciès du conglomérat II (CFA-II: Conglomerate faciès association H) et l'association de faciès de grès riche en quartz (QSFA: Quartz-rich sandstone faciès association) qui se trouve juste au-dessus forment ensemble le second cycle de dépôt. Le CFA-I regroupe un conglomérat à cailloux et galets massif à stratifié et un conglomérat à support de matrice. Le premier est caractérisé par des conglomérats massifs à faiblement stratifiés (faciès Gm) et à lits entrecroisés en forme de fosse (Gt) à support de fragments, des conglomérats massifs à support de matrice (Gms), une unité mineure de grès à stratifications horizontales (faciès Sh) et entrecroisées (faciès St, Sp) et une argilite (FI). Localement, les galets deviennent imbriqués et montrent une composante d'écoulement NE prononcée. Le conglomérat massif à stratifié à cailloux et galets se compose des faciès Gm, Gt, Gp, St, Sh et Sp. Le CFA-I a été déposé par coulées de débris (Gms), courants de traction (Gm-Gt-StSp-Sh) et coulées en feuillets respectivement sur les portions proximale, médiale et distale du cône alluvionnaire. L'association de faciès du siltstone-grès contient une sous-unité dominée par des grès et caractérisée par les faciès Sp, St, Sh et FI qui se sont formés en raison de la migration des dunes et dépôts de levée...

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Late Cenozoic Basin Opening in Relation to Major Strike‐Slip Faulting Along the Porto–Coimbra–Tomar Fault Zone (Northern Portugal)

Gomes

Chaminé

Teixeira

et al. 2007

Sedimentary Processes, Environments and Basins

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Northern Portugal is located in a tectonically complex area affected by major strike-slip zones, namely the north-northwest-trending Porto-Coimbra-Tomar fault zone and the north-northeasttrending Verin-Régua-Penacova sinistral strike-slip fault. Within this region, the sector between Albergaria-a-Velha and Águeda is crucial since it is highly affected by large-scale strike-slip faults and extensional deformation events. Late Cenozoic tectonics in northern Iberia resulted from the collision of the Africa and Eurasia plates, especially in the eastern segment of the Azores-Gibraltar plate boundary. The continued plate indentation originated the movement of major strike-slip faults in the Iberian Massif. The movement on these faults, accompanying the regional stress-field during the early Miocene, initiated the formation of incipient Cenozoic pull-apart basins.The Albergaria-a-Velha-Águeda fault segment has been studied in an attempt to clarify the dynamic relationship between this active fault zone and the evolving landscape. Three geomorphological sectors were identified in the Albergaria-a-Velha region: (i) a littoral platform consisting of a polygenic erosion surface overlain by late Cenozoic alluvial-fluvial sequences; (ii) a tectonically controlled basin (Valongo do Vouga basin) located between hillslopes of two river valleys and normal faults with N-S orientation, where late Cenozoic subsidence is suggested by an influx of alluvial sandy conglomerates; and (iii) a domain of inner elevations of wide metapelitic landforms. Reactivation of the prevailing north-northwest-striking Upper Proterozoic/Palaeozoic basement is a regionally important control on the orientation and kinematics of late Cenozoic faults. Thus, the opening and development of these basins was influenced by the intersection of the northnorthwest-trending dextral faults with north-northeast-trending sinistral faults associated with north-south shortening and east-west extension.

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Strike-Slip faults

Cited by 132 publications

References 0 publications

Mnin restraining stepover – evidence of significant Cretaceous–Cenozoic dextral strike-slip faulting along the Teisseyre-Tornquist Zone?

Mnin restraining stepover – evidence of significant Cretaceous–Cenozoic dextral strike-slip faulting along the Teisseyre-Tornquist Zone?

Implications of an archean strike-slip basin :

Late Cenozoic Basin Opening in Relation to Major Strike‐Slip Faulting Along the Porto–Coimbra–Tomar Fault Zone (Northern Portugal)

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