The oceanic "Metis Geotectonic Event" (Callovian/Oxfordian) and its implications for the peri-Tethyan area of Poland

• Autorzy: Matyja B. , Wierzbowski A.
• Konferencja: International Congress on the Jurassic System (7 ; 06-18.09.2006 ; Kraków, Poland)
• Języki publikacji: EN

Abstrakty

EN

Condensed deposits of the Middle/Upper Callovian and/or lowermost Oxfordian are spread over vast areas of peri-Tethyan Europe from Portugal, and Spain through France, Switzerland, Germany, Poland, to Romania. A number of hypotheses for the origin of these deposits have been presented. Melendez et al. (1983) suggested that they originated due to the rise of CCD in relation to increased igneous activity. Other proposed explanations include: an extra-terrestrial event (Brochwicz-Lewifski et al. 1989) and erosional events and related taphonomic reworking of fossils during long episodes of subaerial exposure (Aurell et al. 1991). Palaeomagnetic data from the Pieniny Klippen Belt (Carpathians) of southwestern Ukraine (Lewandowski et al. 2005), and western Slovakia (Lewandowski et al. 2006) indicate that during Middle Callovian - Early Oxfordian time span a relatively fast opening of the oceanic domain took place in the outer part of the Tethys. This newly open basin (possibly corresponding to the Magura Basin in the Carpathian domain) attained 1100-1400 km in width. The rocks that formed during the Middle Callovian - Early Oxfordian in the epi-platform area of Poland bear witness to this geotectonic event. It is highly probable that the total spatial range of the geo-tectonic event within the Tethys (cf. Lewandowski et al. 2006) has been much greater, however, which indicates that the obtained results can be applied to the whole peri-Tethyan Europe. Thus, to distinguish this phenomenon independently of which particular part of the Tethys it affected, we propose to name it the "Metis Geotectonic Event"(Metis in Greek mythology was the Oceanid, and the daughter of Tethys). The appearance of condensed deposits in the epi-platform area of Poland (Giżejewska & Wieczorek 1974; Dembicz & Praszkier 2003, and other papers cited therein) remains in close time relation with recognized extension in the Tethyan domain. The short time interval of the extension (about 5 Ma) plus a large-scale displacement could have resulted in a sudden change in deposition from shallow-marine to pelagic environment, as well as in chemical corrosion of earlier accumulated carbonates. This change of deposition was controlled by relative sea-level rise as well as by upwelling of cold oceanic waters into the epi-platform area. This interpretation is consistent with recognized isotopic thermometry results indicating drastic cooling of sea water at lower middle latitudes (Dromart et al. 2003). The development of the sponge megafacies covering the peri-Tethyan part of the Late Jurassic shelf of Europe remains in close relationship with discussed phenomena. These deposits showed during Oxfordian similar spatial distribution as older condensed deposits, and represent the non-actualistic deep environment of the Late Jurassic shelf (Matyja & Pisera 1991; Matyja & Wierzbowski 1996).

Słowa kluczowe

EN

Callovian-Oxfordian condensed deposits; Tethys Ocean; epicratonic areas

• Wydawca: Państwowy Instytut Geologiczny - Państwowy Instytut Badawczy
• Czasopismo: Volumina Jurassica
• Rocznik: 2006
• Tom: Vol. 4, no. 1
• Strony: 60--61
• Opis fizyczny: Bibliogr. 10 poz.

Twórcy

autor

Matyja B.

autor

Wierzbowski A.

• Institute of Geology, University of Warsaw, Al. Żwirki i Wigury 93, PL-02089 Warszawa, Poland,

Bibliografia

• 1. Aurell M. et al. 1991. The Middle-Upper Jurassic oolitic ironstone facies: eustatic implications. 3rd International Symposium on Jurassic Stratigraphy, Poitiers 1991. Abstract volume, 13.
• 2. Brochwicz-Lewiński W. et al. 1989. Middle-Upper Jurassic events and their implications. Przeglad Geologiczny, 11: 559-563. (in Polish with English summary)
• 3. Dembicz K. and Praszkier T. 2003. Stratygrafia, mikrofacje i środowisko sedymentacji osadów keloweju z profilu Włodowic koło Zawiercia. Tomy Jurajskie, 1: 35-48.
• 4. Dromart G. et al. 2003. Ice age at the Middle-Late Jurassic transition? Earth and Planetary Science Letters, 213: 205-220.
• 5. Giżejewska M. and Wieczorek J. 1977. Remarks on the Callovian and Lower Oxfordian of the Zalas Area (Cracow Upland, Southern Poland). Bulletin de l’Academie Polonaise des Sciences, Série des Sciences de la Terre, 24: 167-175.
• 6. Lewandowski M. et al. 2005. Palaeogeographic evolution of the Pieniny Klippen Basin using stratigraphic and palaeomagnetic data from the Veliky Kamenets section (Carpathians, Ukraine). Palaeogeograpy, Palaeoclimatology, Palaecology, 216: 53-72.
• 7. Lewandowski M., Aubrecht R. , Krobicki M., Matyja B. A., Reháková D., Schlögl J., Sidorczuk M. and Wierzbowski A. 2006. Palaeomagnetism of the Pieniny Klippen Belt (Carpathians): evidence for lowlatitude origin and palaeogeographic dispersion of the Upper Jurassic carbonates. Volumina Jurassica, 4, 7th International Congress on the Jurassic System, Abstracts volume: this issue.
• 8. Matyja B. A. and Pisera A. 1991. Late Jurassic European sponge megafacies: general perspective. 3rd International Symposium on Jurassic Stratigraphy, Poitiers 1991. Abstracts volume, 81.
• 9. Matyja B. A. and Wierzbowski A. 1996. Sea-bottom relief and batymetry of late Jurassic sponge megafacies in Central Poland. GeoResearch Forum, 1-2: 333-340.
• 10. Melendez G. et al. 1983. Lower Oxfordian in the Iberian Chain, Spain; Part I. Biostratigraphy and nature of gaps. Bulletin de l’Academie Polonaise des Sciences, Série des Sciences de la Terre, 30: 159-172.