seismic analysis of structural and stratigraphic features and compaction effects The link between tectonics and sedimentation in the Pannonian basin:
Acknowledgements
References
Magyar I., Radivojevic D., Sztanó O., Synak R., Ujszászi K., Pócsik, M. 2013: Progradation of the paleo-Danube shelf margin across the Pannonian Basin during the Late Miocene and Early Pliocene. Global and Planetary Change, 103, 168–173.
Prosser S. 1993: Rift related depositional system and their seismic expression. Tectonics and Seismic Sequence Stratigraphy. In: Williams, G.D. Dobb, A. (Eds.),Geol. Soc. Spec. Publ., 71, 35-66.
Schmid S. M., D. Bernoulli, B. Fügenschuh, L. Matenco, S. Schefer, R. Schuster, M. Tischler, and K. Ustaszewski 2008: The Alpine–Carpathian–Dinaridic orogenic system: Correlation and evolution of tectonic units, Swiss J. Geosci., 101(1), 139–183.
Fig. 7: Kiskunhalas half-graben: note the inverted structure Fig. 6: Derecske Trough: note the inverted structures
2,3 4 5 1
Attila Balázs , 1 Liviu Matenco , Imre Magyar , Orsolya Sztanó , Ferenc Horváth , and Sierd Cloetingh
(1) Netherlands Research Centre for Integrated Solid Earth Science, Utrecht University, Faculty of Geosciences, Utrecht, the Netherlands, e-mail: a.balazs@uu.nl (2) MOL Hungarian Oil and Gas Plc., Budapest, Hungary; (3) MTA-MTM-ELTE Research Group for Paleontology, Budapest, Hungary
(4) Department of Physical and Applied Geology, Eötvös Loránd University, Budapest, Hungary; (5) Geomega Ltd, Budapest, Hungary
1
This research is partly financed by the Netherlands Centre for Integrated Solid Earth Sciences (ISES) for the study of the Pannonian basin in collaboration with Eötvös Loránd University, Budapest as well as by the Hungarian National Research Fund OTKA no. 113013. MOL Plc, TXM Ltd, RAG Ltd, and Hungarian Horizon Ltd are acknowledged for the provided seismic and well data. BeicipFranlab is thanked for the academic license for DionisosFlow. We thank the fruitful discussions with Didier Granjeon, László Fodor, and Gábor Bada.
Conclusions and further research
Ÿ
Great Hungarian Plain was diachronous and migrated in space and time across the basin between ca. 20-8 Ma. Internal deformation accommodated the different amounts of rotations in various parts of the area (Figs. 2 and 4)
.
Ÿ
Ÿ
Ÿ Water depth and sedimentary transport routes were primarily determined by inherited and/or local active tectonics and compaction effects including the control of the Miocene shelf- margin progradation directions and Recent fluvial transport routes (Figs. 10 and 12b).
Ÿ
Our study demonstrates that the 270 km of extension in the entire
Lower order tectonic induced sedimentary cycles characterize the main phases of extension in various sub-basins, the higher order cyclicity and associated unconformities define individual moments of fault (re-)activation (Figs. 5 and 7).
Highest water depth values characterized the SE latest Miocene to Pliocene remnant of the lake due to the higher subsidence rates and more distal position from the main source areas (Figs. 10 and 12).
The Túrkeve fault was previously misinterpreted as a strike-slip zone. Correlation of channels on horizon attribute maps demonstrates the pure normal kinematics of fault segments with upwards increasing throw revealing its connection with differential compaction (Fig. 12).
Neotethys ophiolites
L. Balaton
TISZA- DACIA
Alps
Dinarides
Apuseni M.
E Carpathians Vb
T ransylvanian basin
W Carpathians
S Carpathians
Moesian Platform
Sb
Dr S
Kkh Db
ES
Ma TDR
-8000 m 0
Basement depth
28 º
43º 48º
22 º
17 º
44º
27 º48 º
500 km 13 Ma 20 Ma
30 Ma
a
b
50 º
14º
Dinarides AlCaPa
Tisza Dacia volcanics Alpine Tethys
Neotethys
external thrust belt undeformed foreland
c
c
De
Miocene back-arc extension of the Pannonian basin resulted in the formation of a series of half- grabens followed by post-rift subsidence and sedimentation. We performed a novel tectonic a n d s e i s m i c s e q u e n c e s t r a t i g r a p h i c interpretation. We separated tectonic systems tracts of the half-graben deposits that formed as a result of the interplay between subsidence, sedimentation and water-level variations. Lower order systems tracts were defined by separating rift initiation, rift climax, immediate post-rift and late post-rift systems tracts, while a higher order transgressive-regressive cyclicity and associated unconformities were locally identified in the syn- tectonic basin fill.
Extension and half-graben formation migrated in time and space in the basin between Early to Late Miocene between ca. 20-8 Ma (Balázs et al., 2016).
Introduction
Fig. 14: Numerical stratigraphic modeling of half-graben evolution
e
e
Fig. 1 Fig. 2
Fig. 3
Fig. 4: Depocentre migration Fig. 5: Tectonic systems tracts
on well logs
Neotectonic strike-slip faults
Atectonic compaction induced faults
ALCAPA
MH FZ
Fig. 4
Fig. 8: Makó half-graben. Note the perpendicular extensional structures
Fig. 11:
Seismic sections a) and b) oriented p a r a l l e l w i t h t h e d i r e c t i o n o f progradation in the Jászság sub-basin showing typical progradational (in orange), aggradational (in yellow), deposits during forced regression (red), and above retrogradational pattern in the Great Hungarian Plain (location in Figure 10).
Fig. 10:
Positions of the prograding shelf-margin slopes during the Miocene – Pliocene sedimentation (modified after Magyar et al., 2013). Blue circles indicate our calculated water depth values.
Fig. 12a: Túrkeve fault zone
Fig. 12b: Interpreted seismic attribute maps. Note the channelized sedimentary features.
Fig. 13:
Balaton fault zone
Post-rift sedimentation
The Late Miocene-Pliocene Lake Pannon persisted for about 7-8 Myr and was progressively filled by clastic material sourced by the surrounding mountain chains and transported by large rivers, such as the paleo-Danube and paleo-Tisza. We combined sedimentological observations with a backstripping methodology facilitated by well lithology and porosity data to gradually remove the sediment overburden.
The large amount of compaction associated with lateral variations of Neogene sediment thicknesses has created non-tectonic normal fault offsets and gentle folds.
Fig. 11 Fig. 13
Fig. 12
Várkonyi A., Törő B., Sztanó O., Fodor L. 2013: Late Cenozoic deformation and tectonically controlled sedimentation near the Balaton zone (central Pannonian basin, Hungary). Occasional Papers of the Geological and Geophysical Institute of Hungary, 72–73.
Szalay Á. 1982. A rekonstrukciós szemléletű földtani kutatás lehetőségei a szénhidrogénperspektívák előrejelzésében. Candidate thesis, Hungarian Academy of Sciences, Budapest, 146 p.
Balázs A., Matenco L., Magyar I., Horváth F., Cloetingh S. 2016: The link between tectonics and sedimentation in back-arc basins: new genetic constraints from the analysis of the Pannonian Basin. Tectonics 35, 1526–1559. doi: 10.1002/2015TC004109
Fig. 6
Fig. 7 Fig. 8
compaction induced faults
