Selective agglutination of tourmaline grains by foraminifera in a deep-water flysch environment (Eocene Hieroglyphic beds, Silesian Nappe, Polish Outer Carpathians)

Abstract

Waoekowska, A., 2014. Se lec tive ag glu ti na tion of tour ma line grains by foraminifera in a deep-wa ter flysch en vi ron ment (Eocene Hi ero glyphic Beds, Silesian Nappe, Pol ish Outer Carpathians). Geo log i cal Quar terly, 58 (2): 337-352, doi: 10.7306/gq.1154De tri tal frag ments of automorphic tour ma line crys tals are com monly in cor po rated into the tests of sim ple ag glu ti nated foraminifera that lived in the deep-ma rine Carpathian turbidite ba sin in which the de po si tion of the Hi ero glyphic Beds (Eocene) took place. Such grains were ob served in the tests of 37 spe cies rep re sent ing 20 gen era. In spite of the fact that tour ma line oc curs in the Carpathian Flysch sed i ments as an ac ces sory min eral, still it was se lected by the foraminifera as the only heavy min eral to be in cor po rated into their tests. The pro por tion of tour ma line-bear ing spec i mens in an as sem blage usu ally amounts to a few per cent, but may reach 29% in ex treme cases. The par tic u lar pref er ence for tour ma line se lec tion and in cor po ra tion in the test walls is shown by the fol low ing gen era: Psammosiphonella, Reophax, Bathysiphon and Nothia.Key words: heavy min er als, tour ma line, ag glu ti nated foraminifera, deep-ma rine flysch en vi ron ment, Outer Carpathians.

Selective concentration of iron, titanium, and zirconium substrate minerals within Gregory’s diverticulum, an organ unique to derived sand dollars (Echinoidea: Scutelliformes)

“…The mystery surrounding the mechanism whereby these animals select and retain heavy minerals is deepened by the consideration that some agglutinated foraminifera also select and retain heavy minerals in their cytoplasm or even test ( Makled & Langer, 2010 ; Sabbatini et al, 2016 ; Garrison, 2019 ). These single-celled organisms select primarily the heavy minerals zircon, rutile, and ilmenite with a mean grain size of about 100 μm, although Waśkowska (2014) described a fossil species that preferentially selected tourmaline with a grain size of 39 to 69 μm (predominantly dravite, with a specific gravity of 3.0–3.2 g/cm 3 ).…”

The Eocene Hieroglyphic Beds of the Silesian Nappe in the Western Polish Carpathians – their development and foraminiferal record

“…They oc cur in dif fer ent lithostratigraphic po si tions within the Hiero glyphic Beds (e.g., Burtanówna et al, 1937;Ksi¹¿kiewicz, 1974b;Burtan, 1978;Paul, 1993;Wójcik et al, 1993b;Leszczyñski and Radomski, 1994;Wójcik and R¹czkowski, 1994;Waoekowska, 2014cWaoekowska, , 2015a) and mostly do not show lateral con ti nu ity in the west ern part of the Outer Carpathians except for the var ie gated de pos its un der ly ing the Hi ero glyphic Beds and over ly ing the Ciê¿kowice Sand stone (e.g., Burtan et al, 1956;Burtan, 1972Burtan, , 1973Szymakowska, 1979;Leszczyñski, 1981;Wójcik et al, 1993a, b;Leszczyñski and Radomski, 1994). The var ie gated de pos its within the Hi eroglyphic Beds usu ally oc cur as thick shale com plexes (Figs.…”

A lost carbonate platform deciphered from clasts embedded in flysch: Štramberk-type limestones, Polish Outer Carpathians

“…In the Sub-Silesian Unit, exotic clasts occur mainly in the Hradiště Formation and less commonly in the Veřovice Formation. Before the reorganization of the Late Cretaceous basin, the Sub-Silesian and Silesian sedimentary series were similar, because sedimentation in the western part of the Proto-Silesian Basin took place in similar basinal conditions (Golonka et al, 2006b;Waśkowska et al, 2009). The exotics from the Skole Unit, much rarer than the exotics in earlier units, are almost exclusively from the Maastrichtian-Paleocene Ropianka Formation.…”

“…The Silesian, Sub-Silesian and Skole nappes are composed mainly of thick flysch sequences, which are latest Jurassic-Miocene in age, but the oldest (latest Jurassic) deposits are preserved only locally in the Silesian Nappe. Initially, the flysch sequences were deposited in one sedimentary basin, the Proto-Silesian Basin (e.g., Golonka et al, 2006b;Waśkowska et al, 2009), also termed the Severin-Moldavidic realm (Balintoni, 1998;Ślączka et al, 2006), in Romania commonly referred as to the Outer Dacides and the Moldavides (e.g., Săndulescu, 1988). At the end of the Early Cretaceous, the Proto-Silesian Basin was developed again and deposition took place in several sub-basins separated by ridges (e.g., Książkiewicz, 1965;Golonka et al, 2000).…”

“…At the end of the Early Cretaceous, the Proto-Silesian Basin was developed again and deposition took place in several sub-basins separated by ridges (e.g., Książkiewicz, 1965;Golonka et al, 2000). The Sub-Silesian Series was deposited in shallower conditions than the Silesian and Skole series, possibly on the slope of the Sub-Silesian Ridge (e.g., Ślączka et al, 2006;Waśkowska et al, 2009), and variegated shales and marls are relatively frequent there.…”