Structural evolution of the Transylvanian Basin (Romania): a sedimentary basin in the bend zone of the Carpathians

Huismans, Ritske S.; Bertotti, Giovanni; Ciulavu, D.; Sanders, Carlo; Cloetingh, S.A.P.L.; Dinu, C.

doi:10.1016/s0040-1951(96)00261-2

Cited by 52 publications

(44 citation statements)

References 15 publications

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“…Several contrasting data have been published. Huismans et al (1997), Huismans (1999), and Ciulavu (1999) support the existence of a small scale, east-west oriented, early Mid-Miocene tensional phase in the Transylvanian Basin. However, no major regional faults have been identified so far.…”

Section: Early Mid-miocene (Early To Mid-badenian): Tst1-lst4mentioning

confidence: 94%

Middle to late Miocene sequence stratigraphy of the Transylvanian Basin (Romania)

Krézsek¹,

Filipescu

2005

Tectonophysics

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The history of Middle to Late Miocene evolution of the Transylvanian Basin was determined by the bordering Carpathian orogen evolution, the tectonic events being well recorded by the sedimentary history. The basin evolved in a back-arc setting, under a regional, compressional stress field. The major tectonic events produced during the Late Sarmatian and Post-Pannonian were related to the reactivation of the pre-Badenian fault systems. The Transylvanian Basin got uplifted after the Late Pannonian (? during the Pliocene), and at least 500 m of sedimentary cover was eroded. Based on seismic and well-log interpretation, core and outcrop sedimentology, and microfauna, eight sequences were defined. The early Middle Miocene sequences are roughly synchronous to five 3rd order global sea-level cycles. Most of the recognized sequence boundaries are enhanced by regional tectonic events. The sedimentary evolution was also strongly influenced by salttectonics, active starting with the Late Sarmatian. Two sequences were identified in the Lower Badenian deposits. The third sequence (late Early Badenian to early Mid Badenian) preserves information about deeper shelf settings. The lowstand of the following sequence was responsible for the deposition of the salt formation (late Mid Badenian), an important lithostratigraphic marker in the sedimentary record of the basin. In general, the Upper Badenian deposits (parts of the 4th and 5th sequences) belong to deep marine submarine fan systems. The Sarmatian (partially 5th, 6th and partially 7th sequences) was characterized by diverse salinity conditions, stretching from brackish to hypersaline, and by high tectonic instability, which induced several significant relative sea-level falls. During that time, deltaic north) and fandeltaic (east) systems fed submarine fans, stacked between salt-related submarine heights ("channeled" deepmarine depocenters). Most of the Pannonian deposits (partially 7th and 8th sequences) belong to submarine fan systems, but shallower facies were also found in the western and eastern part of the basin.

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Section: Early Mid-miocene (Early To Mid-badenian): Tst1-lst4mentioning

confidence: 94%

Middle to late Miocene sequence stratigraphy of the Transylvanian Basin (Romania)

Krézsek¹,

Filipescu

2005

Tectonophysics

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“…In the western Pannonian basin S. directions bend toward the north and northwest, thus taking up the characteristic West European pattern. In the eastern Pannonian basin the bend is toward the northeast, so much as in Transylvanian basin and Eastern Carpathians SH directions toward the east are predominating (see for recent stress data in the Transylvanian basin Huismans et al, 1997). This radial pattern of regional stress field is presumably generated by superposition of internal body forces (e.g., crustal thickness variations) and boundary forces (e.g., push by the Adriatic promontory).…”

Section: Seismicity and Recent Stress Fieldmentioning

confidence: 99%

Stress-induced late-stage subsidence anomalies in the Pannonian basin

1996

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Subsidence, sedimentation and tectonic quiescence of the Pannonian basin was interrupted a few million years ago by tectonic reactivation. This recent activity has manifested itself in uplift of the western and eastern flanks, and continuing subsidence of the central part of the Pannonian basin. Low-to medium-magnitude earthquakes of the CarpathianPannonian region are generated mostly in the upper crust by reverse and wrench fault mechanisms. There is no evidence for earthquakes of extensional origin.2-D model calculation of the subsidence history shows that a recent increase in magnitude of horizontal compressional intraplate stress can explain fairly well the observed Quaternary uplift and subsidence pattern. We propose that this stress increase is caused by the overall Europe/Africa convergence. In Late Pliocene, consumption of subductible lithosphere at the eastern margin of the Pannonian basin was completed, and the lithosphere underlying the Pannonian basin became locked in a stable continental frame. Consequently extensional basin formation has come to an end, and compressional inversion of the Pannonian basin is in progress.

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“…In this paper two independent methods and studies are combined to better understand the tectonic evolution of the region, namely outcrop-scale structural studies (Huismans et al 1997, Tischler et al 2007) and paleomagnetic investigations. The latter became possible since the recent regional tectonic study by Tischler et al (2007) provided suitable outcrops for paleomagnetic sampling, in a generally badly exposed area with friable lithologies.…”

Section: Introductionmentioning

confidence: 99%

The contact zone between the ALCAPA and Tisza-Dacia mega-tectonic units of Northern Romania in the light of new paleomagnetic data

Marton¹,

Tischler

Csontos

et al. 2007

Swiss j geosci

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Paleomagnetic analyses were carried out on samples from 19 localities within two different mega-tectonic units in Northern Romania: Tisza-Dacia (11 localities) and ALCAPA (8 localities). The samples cover a range of different lithologies: (1) Late Cretaceous red-coloured marl to marly limestone, (2) EoOligocene flysch sediments, and (3) mid-Miocene (Langhian) tuffite (Dej tuff and related sediments). The Late Cretaceous and mid-Miocene specimens carry secondary paleomagnetic signals exhibiting a counter clockwise deflection of the paleo-declinations by some 30°, while the Eo-Oligocene localities indicate an overall clockwise deflected (between some 45°and >90°) paleodeclination with respect to present-day north. Clockwise rotation postdates the age of sedimentation (Lower Oligocene), as well as (at least partially) thrusting of the Pienides onto the Tisza-Dacia mega-tectonic unit, which occurred between 20.5 and 18.5 Ma. Clockwise rotation predates post-12 Ma counter clockwise rotations inferred for the mid-Miocene localities.Surprisingly, the clockwise rotations of the first rotational stage not only affected the (par-) autochthonous sedimentary cover of the Tisza-Dacia megatectonic unit, but also the allochthonous flysch nappes of the Pienides, i.e. the eastern tip of the ALCAPA mega-tectonic unit. Well-documented opposed rotation of the remainder of ALCAPA necessitates a detachment of this eastern tip of ALCAPA after 18. Die Rotation der Eo-Oligozänen Proben fand nach der Sedimentation der jüngsten Proben (unteres Oligozän), und zumindest teilweise nach dem Deckenschub der Pieniden (20.5-18.5 Ma) auf den Tisza-Dacia Block statt. Diese Rotation mit dem Uhrzeigersinn geht der durch die mittel-Miozänen Proben dokumentierten gegenläufigen Rotation (ab 12 Ma) voraus.Die Rotationen der früheren Phase wurden nicht nur in den Sedimenten aus der (par-) autochthonen Bedeckung von Tisza-Dacia, sondern auch in den überschobenen Pieniden nachgewiesen. Dieses Ergebnis ist auf den ersten Blick überraschend, da sie Teil von ALCAPA sind, der Rest von ALCAPA zu dieser Zeit aber in einem gegenläufigen Sinn, also gegen den Uhrzeigersinn, rotierte. Diese gegenläufigen Rotationen erfordern also eine tektonische Ablösung der östlichsten Spitze von ALCAPA vom Rest dieser grosstektonischen Einheit. Der wahrscheinlichste Ort für eine solche Ablösung befindet sich an den Rändern der Transkarpathischen Depression. Die zweite Rotationsphase, ca. 30°gegen den Uhrzeigersinn nach 12 Ma, ist auch aus dem OstSlovakischen Becken bekannt. Sowohl die Internen West-Karpathen westlich des Ost-Slovakischen Beckens, als auch das südliche Apuseni Gebirge, zeigen nach 12 Ma ein vom Arbeitsgebiet abweichendes Rotationsverhalten.

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Structural evolution of the Transylvanian Basin (Romania): a sedimentary basin in the bend zone of the Carpathians

Cited by 52 publications

References 15 publications

Middle to late Miocene sequence stratigraphy of the Transylvanian Basin (Romania)

Middle to late Miocene sequence stratigraphy of the Transylvanian Basin (Romania)

Stress-induced late-stage subsidence anomalies in the Pannonian basin

The contact zone between the ALCAPA and Tisza-Dacia mega-tectonic units of Northern Romania in the light of new paleomagnetic data

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