Detrital tourmaline as an indicator of source rock lithology: an example from the Ropianka and Menilite formations (Skole Nappe, Polish Flysch Carpathians)

Abstract

Tour ma line pop u la tions stud ied from the Campanian-Maastrichtian part of the Ropianka (Up per Cre ta ceous-Paleocene) and Menilite (Oligocene) for ma tions of the Pol ish Carpathians, rep re sent a mix ture of first-cy cle and polycyclic grains. The tour ma lines of the de pos its stud ied dis play very strong re sem blance in terms of op ti cal fea tures and chem i cal com po si tion. They be long mostly to the schorl-dravite se ries with a mi nor con tri bu tion of tour ma lines of foititic or Mg-foititic com po si tion. Euhedral tour ma lines orig i nated from metasedimentary rocks, while the rounded grains crys tal lised in Li-poor gra nitic rocks or in pegmatites, Al-poor and Al-rich metasedimentary rocks. Most of the tour ma lines stud ied crys tal lised dur ing a sin gle igne ous or meta mor phic event. How ever, tour ma lines form ing in evolv ing chem i cal con di tions as well as polymetamorphic grains (hav ing a meta mor phic de tri tal core and meta mor phic overgrowths) are also pres ent. The chem i cal com po si tion of the meta mor phic tour ma lines stud ied in di cates their for ma tion in me dium-grade meta mor phic con di tions. This is sup ported by the crystallisation tem per a ture of the gar net-bi o tite in clu sion pres ent in one of rounded meta mor phic tour ma lines from the Ropianka For ma tion. The euhedral grains de rive from meta sedi ments, di rectly from a mas sif lo cated close to the Skole Basin. The scar city of euhedral grains in the tour ma line pop u la tions stud ied sug gests that their source rocks were poor in these min er als. The di rect sources of rounded tour ma lines (most prob a bly polycyclic grains), may have been Pa leo zoic and Me sozoic sed i men tary rocks of the Skole Ba sin fore land or crys tal line rocks of re mote source ar eas. The ini tial ig ne ous and metamor phic host rocks of the tour ma lines may have been crys tal line do mains of the Bo he mian Mas sif and/or the crys tal line base ment of Brunovistulicum.

Heavy minerals and exotic pebbles from the Eocene flysch deposits of the Magura Nappe (Outer Western Carpathians, eastern Slovakia): their composition and implications on the provenance

“…Although it may seem that the Bohemian Massif was a possible source for the Rača Unit, because it was proposed for more external zones of the Flysch Belt, much like for the western sector of the Magura Nappe (e.g., Krystek, 1965;Otava et al, , 1998Salata, 2014), this idea has no basis for the Mrázovce Mb. siliciclastics.…”

Heavy minerals from sedimentary rocks of the Malcov Formation and their palaeogeographic implications for evolution of the Magura Basin (Western Carpathians, Slovakia) during the Late Eocene – Late Oligocene

“…The use of heavy min eral as so ci a tions for the in ter pre ta tion of source ar eas in the Flysch Belt of the West ern Carpathians was ex ploited by Leško et al (1959), Starobová (1962), Ïurkoviè (1965, 1966), Koráb andÏurkoviè (1966, 1973) and Fejdiová (1990); more de ci sive re sults were ob tained by us ing the electron probe com bined with op ti cal meth ods (Otava et al, 1997(Otava et al, , 1998Salata and Oszczypko, 2000;Salata, 2002aSalata, , b, 2004Salata, , 2013Salata, , 2014aSalata, 2004, 2005;Grzebyk and Leszczyñski, 2006;Bónová et al, 2009aBónová et al, , b, 2010aUchman, 2012, 2013).…”

Sedimentary processes and architecture of Upper Cretaceous deep-sea channel deposits: a case from the Skole Nappe, Polish Outer Carpathians

“…During the Turonian-Paleocene times, the sediments of the Skole Basin are thought to have been derived from the southern part of the Upper Silesia and Małopolska blocks to the north (Książkiewicz 1962;Bromowicz 1974;Salata & Uchman 2013) and from the side of the Subsilesian Ridge (Węglówka Ridge) to the south (Książkiewicz 1962). The petrographic variety of the source area was repeatedly mentioned in the literature (e.g., Salata & Uchman 2013;Salata 2014;Łapcik et al 2016 and references therein). Four lithostratigraphic members of the Ropianka Formation were distinguished based on repeated carbonate-siliciclastic deposits ( Fig.…”