Stratigraphic position of alkaline volcanic rocks in the autochthonous cover of the High-Tatric Unit (Western Tatra Mts., Central Western Carpathians, Slovakia)
“…Volcanic products, mostly submarine hyaloclastic lava flows, occurred on passive continental margins of the Pennine rifts (distal European Silesian margin, Oravic Czorsztyn continental ribbon, and extended Austroalpine margin); e.g., Dostal and Owen (1998), Spišiak et al (2011, and references therein), Spišiak (1988, 1993), Spišiak and Hovorka (1997), and Trommsdorff et al (1990). In general, the first manifestations of this volcanism were detected in the Berriasian Tatric and Oravic successions around 145-140 Ma ago (Madzin et al, 2014;Oszczypko et al, 2012;Reháková et al, 2011), and then occurred throughout the Cretaceous with the main activity during the Aptian to Albian, that is, 125-100 Ma ago (Birkenmajer & Pécskay, 2000;Bujnovský et al, 1981;Grabowski et al, 2003;Lucińska-Anczkiewicz et al, 2002;Spišiak & Balogh, 2002) with extension into the Late Cretaceous (Spišiak et al, 2011).…”
Section: Tectonic Development Of the Pieniny And Magura Beltsmentioning
confidence: 97%
“…ii. Furthermore, extensional regime is associated with volumetrically limited but areally widespread alkaline basaltic volcanism of submarine hyaloclastic lava flows and dyke swarms frequently occurring in both the Tatric and Fatric regions ( Figure 6; Bujnovský et al, 1981;Hovorka & Spišiak, 1988Hovorka et al, 1999;Madzin et al, 2014;Spišiak & Balogh, 2002;Spišiak & Hovorka, 1997;Spišiak et al, 2011). iii.…”
The early Alpine tectonic evolution of the Western Carpathian orogenic system is differentiated into four main periods: (i) Middle-Late Triassic rifting and spreading of the Meliata Ocean, but its relationships to the Tethyan realm remain uncertain; (ii) Jurassic subduction of the Meliata oceanic lithosphere and coeval rifting of the Carpathian lower plate and oceanic breakup and spreading of the Atlantic-related Piemont-Váh Ocean, as well as short-term back-arc rifting of the Adriatic upper plate; (iii) Early Cretaceous slow and continuous but intermittent growth of the asymmetric, doubly vergent orogenic wedge still driven by the Meliata slab, concurrently with expansion of the outer Pennine oceanic zones; and (iv) Late Cretaceous to Middle Eocene northward drift of the Adriatic microplate with Austroalpine domains appended at its front that eliminated the external oceanic zones with intervening continental ribbons and sequentially accreted the Carpathian Penninic units. While dynamics of the periods (i) and (iv) was governed by the large-scale plate motions, periods (ii) and (iii) are interpreted as driven by the self-generated forces exerted by the subduction pull of oceanic and lower continental lithosphere. Tectonic evolution of particularly the latter two periods is documented in detail by rich structural, sedimentary, metamorphic, and magmatic rock records. It is inferred that periods of accelerating activity of the orogenic wedge progradation, distinguished as the regional tectonic phases, resulted from interactions between buildup of tectonic stresses and their structural realization dependent on the rheological properties of crustal rocks.
“…Volcanic products, mostly submarine hyaloclastic lava flows, occurred on passive continental margins of the Pennine rifts (distal European Silesian margin, Oravic Czorsztyn continental ribbon, and extended Austroalpine margin); e.g., Dostal and Owen (1998), Spišiak et al (2011, and references therein), Spišiak (1988, 1993), Spišiak and Hovorka (1997), and Trommsdorff et al (1990). In general, the first manifestations of this volcanism were detected in the Berriasian Tatric and Oravic successions around 145-140 Ma ago (Madzin et al, 2014;Oszczypko et al, 2012;Reháková et al, 2011), and then occurred throughout the Cretaceous with the main activity during the Aptian to Albian, that is, 125-100 Ma ago (Birkenmajer & Pécskay, 2000;Bujnovský et al, 1981;Grabowski et al, 2003;Lucińska-Anczkiewicz et al, 2002;Spišiak & Balogh, 2002) with extension into the Late Cretaceous (Spišiak et al, 2011).…”
Section: Tectonic Development Of the Pieniny And Magura Beltsmentioning
confidence: 97%
“…ii. Furthermore, extensional regime is associated with volumetrically limited but areally widespread alkaline basaltic volcanism of submarine hyaloclastic lava flows and dyke swarms frequently occurring in both the Tatric and Fatric regions ( Figure 6; Bujnovský et al, 1981;Hovorka & Spišiak, 1988Hovorka et al, 1999;Madzin et al, 2014;Spišiak & Balogh, 2002;Spišiak & Hovorka, 1997;Spišiak et al, 2011). iii.…”
The early Alpine tectonic evolution of the Western Carpathian orogenic system is differentiated into four main periods: (i) Middle-Late Triassic rifting and spreading of the Meliata Ocean, but its relationships to the Tethyan realm remain uncertain; (ii) Jurassic subduction of the Meliata oceanic lithosphere and coeval rifting of the Carpathian lower plate and oceanic breakup and spreading of the Atlantic-related Piemont-Váh Ocean, as well as short-term back-arc rifting of the Adriatic upper plate; (iii) Early Cretaceous slow and continuous but intermittent growth of the asymmetric, doubly vergent orogenic wedge still driven by the Meliata slab, concurrently with expansion of the outer Pennine oceanic zones; and (iv) Late Cretaceous to Middle Eocene northward drift of the Adriatic microplate with Austroalpine domains appended at its front that eliminated the external oceanic zones with intervening continental ribbons and sequentially accreted the Carpathian Penninic units. While dynamics of the periods (i) and (iv) was governed by the large-scale plate motions, periods (ii) and (iii) are interpreted as driven by the self-generated forces exerted by the subduction pull of oceanic and lower continental lithosphere. Tectonic evolution of particularly the latter two periods is documented in detail by rich structural, sedimentary, metamorphic, and magmatic rock records. It is inferred that periods of accelerating activity of the orogenic wedge progradation, distinguished as the regional tectonic phases, resulted from interactions between buildup of tectonic stresses and their structural realization dependent on the rheological properties of crustal rocks.
“… Figure 11. Schematic middle Albian cross-section displaying position of suspended hydrothermal activity near the Tatric Ridge, related to magmatic and volcanic processes in the surroundings. Interpretation based on data from the Tatra Mountains (Madzin, Sýkora & Soták, 2014) and the Križna Nappe (Bujnovský, Kantor & Vozäft, 1981; Spišiak & Balogh, 2002); geology after Michalík (2007) and Prokešová, Plašienka & Milovský (2012). …”
Section: Discussionmentioning
confidence: 99%
“…In the western part of this area, a few small lenticular bodies and bands (2–30 m thick) of alkaline volcanic rocks classified as hyalobasanites occur (Kotański & Radwański, 1959; Hovorka & Spišiak, 1981; Spišiak & Hovorka, 1997; Hovorka, Dostál & Spišiak, 1999; Ivan, Hovorka & Méres, 1999; Staniszewska & Ciborowski, 2000). They are sandwiched with carbonate breccia containing calpionellid microfaunas, whose stratigraphic position corresponds at the latest to the Tithonian through the ?early Valanginian (Madzin, Sýkora & Soták, 2014). These shallow-water Urgonian-type carbonate sediments (locally with volcanic rocks) partially emerged during late Aptian – early Albian time.…”
Section: Geological Settingmentioning
confidence: 99%
“…Nonetheless, hydrothermal sources of iron and silica cannot be excluded here, due to an occurrence of ocean-floor alteration processes at and near the Tatric Ridge (Hovorka & Spišiak, 1988; Spišiak et al . 1991; Spišiak & Balogh, 2002; Madzin, Sýkora & Soták, 2014).…”
Studies dealing with the response of subaqueous volcanic and hydrothermal activities to carbonate sedimentation in hemipelagic environments affected by tectonic processes are comparatively rare. Here, a microfacies record with combined chemical data from the neptunian dykes found at an intrabasinal ridge (Tatric Ridge; Carpathian domain of the Western Tethys), close to a source of alkaline volcanism with possible hydrothermal vents (Zliechov Basin), is presented. The characteristic features of the neptunian dykes, up to 20 cm thick, in the middle Albian echinoderm-foraminiferal limestones (Tatra Mountains, Inner Carpathians) are their red fillings. Microprobe and x-ray diffraction analyses show that this reddish material, partly mixed with sparitic clasts coming from the host limestone, consists mainly of hematite crystals which are associated with low crystalline silica and quartz. The microfacies data suggest that the reddish infillings of the dykes is partly related to dissolution processes inside the fissures that could have taken place during the transport of FeCl3 fluids together with silica gel. The fluids could have been derived from hydrothermal vents occurring along the extensional faults in the neighbouring Zliechov Basin. Rare Earth element (REE) signatures of the reddish infill (i.e. low values of total REE content, chondrite- and Post-Archean Australian Shale-normalized REE + Y patterns with negative Ce anomaly) and a high Y/Ho ratio suggest authigenic removal of REEs from the water column. This suggests that the fissures were open to the sea bottom and were in contact with sea water during their filling.
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