DOCSLIB.ORG

Upper Maastrichtian and Paleocene Deposits At

Total Page：16

File Type：pdf, Size：1020Kb

Download full-text PDF Read full-text
Upper Maastrichtian and Paleocene Deposits At ROCZNIK POLSKIEGO TOWARZYSTWA GEOLOGICZNEGO ANNALES DE LA SOCIÉTÉ GÉOLOGIQUE DE POLOGNE Vol. XLVIII — 1: 27—37 Kraków 1978 Stefan W. Alexandrowicz1, Krzysztof Birkenmajer2 UPPER MAASTRICHTIAN AND PALEOCENE DEPOSITS AT SZAFLARY, PIENINY KLIPPEN BELT, CARPATHIANS, POLAND <4 Pig., 1 Tab.) Utwory górnego mastrychtu i paleocenu w Szaflarach, pieniński pas skałkowy ■ (4 fig., 1 tab.) Abstract: At the contact of the Pieniny Klippen Belt with the Podhale Flyseh (Palaeogene) at Szaflary (Polish Carpathians), occur late Maastrichtian and Paleocene deposits of small thickness, characterized by aibundant, pre­ dominantly planktonie foraminiferal assemblages, developed in a facies unknown from the Klippen successions in Poland. These deposits correspond to a zone known in Slovakia as the „peri-KBppen” zone, resp. Myjava Furrow, which was situated to (the south of the Klippen Belt basin and its southern exotic massif, and to the north of the folded Central Carpathian (Su'b-Taitric and High-Tatric) units. INTRODUCTION At the contact of the Pieniny Klippen Belt and the Podhale Palaeo­ gene flyseh at Szaflary (Polish Carpathians), occur late Maastrichtian and Paleocene deposits developed in a facies unknown from the Klip­ pen successions of Poland. These rock’s are younger than the young­ est ilithostratigrap'hic units of 'the Klippen successions, which are rep­ resented by preorogenic flyseh of the Sromowce Formation (Coniacian to Lower Campanian — see Birkenmajer, 1977) in the southern tectonic units, and by pelagic Globotruncana marlis of the Pustelnia Marl Member (Turonian to Lower Maastrichtian — see A lexandro­ wicz, 1975; Birkenmajer, Jednorowska, 1976; Birken­ majer, 1977) in the northernmost part of the geanticlinal Czorsztyn Succession. 1 Instytut Geologii i Surowców Mineralnych AGH, al. MLokiewicza 30, 30-059 Kraków. 8 Zakład Nank Geologicznych PAN, ul. Senacka 3, 31-002 Kraków. — 28 The Paleöcene rooks at Szaflary have been recognized in 1964 by Durand --Del g a (1965) on microfaunal investigation by J. M a g- n é. Small outliers of the Campanian-Maastrichtian, Paleocene (?) and Eocene-Oligocene rocks of small thickness, have been traced west of Szaflary, along the boundary of the Pieniny Klippen Belt with the Podhale Palaeogene, by Morgi el and Sikora (1972, 1973). The sequence discussed differs both in age and in facies from those recog­ nized in the Klippen successions (Birkenmajer, 1965, and later papers), and represents an independent succession which was attribu­ ted to the so-called „Złatne succession” by Morgiel and Sikora (op. cit.), but correlated with the Myjava succession of West Slovakia by Birkenmajer (1977, p. 140). T he M aastrichtian unit of the succession is partly coeval with the Maastrichtian flysch and molasse of the Jarmuta Formation, which is represented by coarsely to fine- -detrital clastics with abundant rock material from the Klippen succes­ sions as secondary deposit, and which was deposited unconformably upon folded Klippen successions and, besides, in the Magura basin (Graj­ carek Unit — see Birkenmajer, 1965, 1970, 1977) — to the north of the Czorsztyn geanticline. Fig. 1. Location of Szaflary within the Pieniny Klippen Belt. 1 — Magura Nappe; 2 — Podhale Flysch; 3 — Pieniny Klippen Belt; 4 — Northern and southern tec­ tonic boundaries of the Pieniny Klippen Belt Fig. 1. Położenie Szaflar w pienińskim pasie skałkowym. 1 — płaszczowina magur­ ska; 2 — flisz podhalański; 3 —• pieniński pas Skałkowy; 4 — północna i połud­ niowa granica tektoniczna pienińskiego pasa skałkowego The present paper gives the results of lithologie and microfaunal investigations of a section exposed along the right bank of the Duna­ jec River at Szaflary (Fig. 1), at the southern contact of the Pieniny Klippen Belt. The field work fwas done in 1969. LITHOLOGY, MICROFAUNA AND AGE OF THE DEPOSITS The section along the right bank of the Biały Dunajec River expo­ ses several! Upper Cretaceous lilt bostratigraphic units of the Pieniny Succession (Fig. 2: 6—S) on the north, and a 25 m thick complex of Cd £ g "O ? a> fQ »000 cu g - g 3 c/> a ■S'S ^ Sg^l? .0 d ,'0«s sSö,a o *? s-s J ® j.s tuo cö w ^ ^ £ v £ «g^g” *£5 •■-> g§ oi - eMä ś G tu V ^ 0) cd ' 3 CD 0N'Ö « bh . —G15 o g I iT-k £ > . >» O S) C- >N O 5 N t-i cd g - J Ctf -(-< o1 ^ s ! ; K. ^ S OS - h i* l . £ cfl a r.a w| g yji rt ISI tn <n M 8 cd -Ü O ^ S a , «1 I I OIE cd C'JI « o _Q 0) M M ^ uV * i>£J 00 pj Æ Ui S ' o cd 1) M01 tfl N»i Ct.rl S?| O >j nj 3 y ■£'m O Ä a <M Swllg|'S o I M ^ G :£ '•£ § C?J« I cd- cd cd W a * p : G «h ^ I 2 £ U J- I § «M <u ia f-i t-. •*-( g ~n 'O <D <?li° i , M (IJ «1H M ^ it? c . .£ M « bd Ö< iG Ph m a< CO ;.“ K m u ä >> M !s'| ' . » 1 1) « PL, tO) a g G • •~' V C d t5 ■I •S S-g^g§I|lgi l,- - ^ ■ _ M □ > ca c - g s | | 5 pöS“(§ Sö8§g M f i ü P §} 3 2 Ö<u 'S■§ 'SS "WJ y <u~ fl) §.ggwl _ , £ < “ æ 3 . * •Hl,ü -, ft)'V ,_|C .a - p5 aj co .S q E ^w â g ö to 3» « ^ g ■§ V-e-3 ö f li ■s s iii “5 0> M r l S Irl!h ’>5 ni 0) cd ■5 .^ j ,1^ J3,-4 9" wS 'öaca £, f i « | i S Ü £ £} Cd -H V3 w cy tj «h s&S p *3 SZ1m "H,2 „ fi ®g ^ S"l§sr . s r S s ‘ rĆ-I T3‘P ■»co 'S.O sbf MS"*' § Cd O .2 |x) 1 G■ sm s s JT ^ X S n O CO -S 01 e . - X3 cd u g I o- . CU « ^ G I 3 05 G ^ C W . • M <U rt) »—« </) bJO cd g cd 35 Wl {-I , .5 cö . x: 2 I .0 -r* p >> O! w SO jd a S, m-( w) à'w 'o 30 — Maastrichtian and Paleocene rocks on the south, at the contact with the Podhale Flyseh (Zakopane Formation, Upper Eocene). The rocks are vertical or dip at very steep angles to the south or to the north, and are often recumbent. The Maastrichtian-Paleocene complex is repre- AGE M ID D LE PALEOCENE Fig. 3. Lith-ostratigraphie coluimn of the Upper Maastrichtian and Middle Paleocene sediments at Szaflary, f — Tectonic contacts Fig. 3. Kolumna lit o stratygraficzna osadów górnego mastrychtu i środkowego paleo­ cenu w Szaflarach, f - kontakty tektoniczne sented by two lithostratigraphic units of formation rank: the older marly complex (with sandstone-sedimentaTy breccia intercalation in the middle) which yielded Upper Maastrichtian foraminifers, and the youn­ ger, shaly complex which yielded Paleocene foraminifers (Fig. 3). Upper Maastrichtian Unit 1 (8 m) The oldest part of the Maastrichtian complex tectonically contacts with the Podhale Flyseh (Zakopane Formation, Upper Eocene) which is overturned in a narrow zone adjoining the contact, then (further south) it dips normally towards the south. The Maastrichtian unit 1 is repre­ sented by pale-grey, pale-green, whitish weathered, strongly cleaved marls and m arly limestones (Fig. 2: 1). Ten samples for microfauna were taken. The microfossils were dif­ ficult to separate from hard marls and marly limestones, where they were often deformed, and only softer marls yielded determinable forms. The dominant element of the microfaunal spectrum (Tab. 1: as­ semblage 1) is represented by planktonie forms, of which Globotrun- cana stuartiformis Dalbiez is the most common, and is associated with stratigraphically important G. stuarti (Lapparent), G. conica White, Abathomphalus mayaroensis (Bolli) and Pseudotextularia spp. Of the T a b le 1 Microfaunal spectra of the Upper Maastrichtian (units 1, 3) and Middle Paleocene (unit 4) pelagic sediments from Szaflary s _ single; r — rare; f — few; c — common; a — abundant Species Ldfchostratigraphic unit: 1 Assemblage: 1 Reophax sp. s s Hormosina ovulum ((Grzybowski) r s Nodellum velascoense (Cushman) s Glomospira charoides (Jones et Parker) r Glomospira gordialis (Jones et Parker) s s Ammodiscus siliceus (Tenquem) s r Trochamminoides irregularis White s Textularia. plummerae Lalicker s s Spiroplectammina semicomplanata (Carsey) r r Gaudryina of. pyramidata Cushman s s s Tritaxia tricarinata Reuss r s s Areno bvlimina sp. s s s Dorothia bulleta Carsey s s s Dorothia trochoides (Marsson) r s s Leniicidina maorodisca (Reuss) s s Lenticulina milcoxensis (Cushman et Ponton) s Astacolus compressas (d’Orfoigny) Vaginulina trilobata (d’Orbigny) s Neoflabellina cf. numdsmalis Wedekind s Pseudoglandulina parallela (Marsson) s Gyroidinoides nitidus (Reuss) s r Stensioeina caucasica (Subbotina.) s s Stensioeina pommerana Brotoen r s Eponides cf. franhei Brotzen r Anomalina cf. welleri (Plummer) Gavelinella pertusa (Marsson) Pseudovalvulineria cf. praeacuta Vassilenko Cibicidoides cf. actulagayensis Vassilenko Globigerina triloculinoides Pllumimer a Globorotalia aegua Cushman et Renz r Globorotalia angvlata (White) c Globotruncana area (Cushman) f Globotruncana contusa -(Cushman) f Globotruncana conica White f Globotrunca-na of. gagnebini Tilev s Globotruncana ganss&ri Belli r Globotruncana stuarti (Dapparemt) r s Globotruncana stuartiformis Dadbiez c r Abathomphalus mayaroensis (BoLli) r Rugoglobigerina rugosa (Pllummer) f c Reussella szajnochae (Grzybowski) s s Pleurostomella sp. s s Aragonia ouezzanensis (Rey) s Bolivina incrassata Reuss s Bolivinoides giganteus Hiiltermann et Koch s Pseudotextularia acervulinoides (Egger) r s Pseudotextularia elegans (Rzehak) f s Pseudotextularia varians (Rzehak)^ s — 32 — benthie forms, the most characteristic are: Gavelinella pertusa (Mars- son), Stensioeina pommerana Brotzen, S. caucasica (Su'bbotina) and Reussella szajnochae (Grzybowski). The variation within the foramini- ferai 'spectrum between the samples is negligible, and depends on the percentage of benthos (10—20%). The assemblage indicates the Upper • Maastrichtian, possibly the latest Upper Maastrichtian, age of the marls.
Load more

Recommended publications
  • The Šariš Transitional Zone, Revealing Interactions Between Pieniny
    Swiss Journal of Geosciences (2018) 111:245–267 https://doi.org/10.1007/s00015-017-0297-9 (0123456789().,-volV)(0123456789().,-volV) The Sˇarisˇ Transitional Zone, revealing interactions between Pieniny Klippen Belt, Outer Carpathians and European platform Edyta Jurewicz1 Received: 4 January 2017 / Accepted: 21 December 2017 / Published online: 16 January 2018 Ó The Author(s) 2018. This article is an open access publication Abstract The Pieniny Klippen Belt (PKB) is a narrow structure delineating the boundary between the Central and Outer Carpathians. It is built of nappes stacked during the Cretaceous and Paleocene and then re-folded in the Miocene during the formation of the Outer Carpathian overthrusts. The internal structure of the PKB at the Polish/Slovakian border first formed during northward nappe thrusting processes, which were most intense at the turn of the Cretaceous to the Paleocene. A secondary factor is the change in strike of the PKB turning from W–E to WNW–ESE, associated with dextral strike-slip faulting in the Carpathian basement (North-European Platform). These NNW-SSE oriented strike-slip fault zones, broadly parallel to the Teisseyre-Tornquist Zone, are responsible for the segmentation of the down-going plate, which influenced the sub- duction and collision between the North-European Platform and the Central Carpathian Block. Among them, the most important role was played by the Krako´w—Myszko´w Fault Zone separating the Małopolska and Upper Silesian blocks in the Carpathian foreland. Shifts and interactions between the neighboring Pieniny and Outer Carpathian basins—during contemporaneous sedimentation and deformation—resulted in a difficult-to-define, transitional zone.
    [Show full text]
  • Kaczawa Klippen Belt – Geotouristic Attraction in the Sudety Mountains, SW Poland
    Acta Geoturistica volume 9 (2018), number 1, 30-35 doi: 10.1515/agta-2018-0004 Kaczawa Klippen Belt – geotouristic attraction in the Sudety Mountains, SW Poland * JAN GOLONKA , MARIA BARMUTA AND JAN BARMUTA Faculty of Geology, Geophysics and Environmental Protection, AGH University of Science and Technology, Mickiewicza 30, 30-059, Krakow, Poland (*corresponding author e-mail: [email protected]) ABSTRACT In the paper authors present some geological sites from Kaczawa Unit, Sudetes, Poland, and their interpretation in a geotectonic context. All described geosites are important for understanding the evolution of so called Kaczawa Accretionary Prism as well as whole Sudetes. Presented outcrops are easily accessible, well exposed and exhibits high education value. Special attention was given to the Wojcieszów Limestones and their relationship to the surrounding rocks Keywords: geoturism, geotectonic, Sudetes, Kaczawa Unit, olistolith. INTRODUCTION AND OBJECTIVES special attention given to the Wojcieszów Limestones. Noticeable increase of different geoturistic initiatives have been recently recognized in Poland. Few geoparks and GEOLOGICAL SETTINGS geoeducational centers have been already established and some more are in the Geographically, the Kaczawa Unit is project phase. Numerous geological sites located in the south western part of Poland. have been described and prepared for Geologically, it belongs to the Western tourism and numerous publications an Sudetes and occupies most external, geoturistic maps are available. However, it northeastern part of the Bohemian Massif. has been noticed that not enough attention From the south - west the Kaczawa Unit is is given to processes which are responsible bordered by the Karkonosze Massif, which for rock formation. Also an information is consider as a eastern part of the about geotectonical environment in which Saxothuringian Terrane.
    [Show full text]
  • Western Carpathians, Poland)
    Geological Quarterly, 2006, 50 (1): 169–194 Late Jurassic-Miocene evolution of the Outer Carpathian fold-and-thrust belt and its foredeep basin (Western Carpathians, Poland) Nestor OSZCZYPKO Oszczypko N. (2006) — Late Jurassic-Miocene evolution of the Outer Carpathian fold-and-thrust belt and its foredeep basin (Western Carpathians, Poland). Geol. Quart., 50 (1): 169–194. Warszawa. The Outer Carpathian Basin domain developed in its initial stage as a Jurassic-Early Cretaceous rifted passive margin that faced the east- ern parts of the oceanic Alpine Tethys. Following closure of this oceanic basin during the Late Cretaceous and collision of the Inner Western Carpathian orogenic wedge with the Outer Carpathian passive margin at the Cretaceous-Paleocene transition, the Outer Carpathian Basin domain was transformed into a foreland basin that was progressively scooped out by nappes and thrust sheets. In the pre- and syn-orogenic evolution of the Outer Carpathian basins the following prominent periods can be distinguished: (1) Middle Juras- sic-Early Cretaceous syn-rift opening of basins followed by Early Cretaceous post-rift thermal subsidence, (2) latest Creta- ceous-Paleocene syn-collisional inversion, (3) Late Paleocene to Middle Eocene flexural subsidence and (4) Late Eocene-Early Miocene synorogenic closure of the basins. In the Outer Carpathian domain driving forces of tectonic subsidence were syn-rift and thermal post-rift processes, as well as tectonic loads related to the emplacement of nappes and slab-pull. Similar to other orogenic belts, folding of the Outer Carpathians commenced in their internal parts and progressed in time towards the continental foreland. This process was initi- ated at the end of the Paleocene at the Pieniny Klippen Belt/Magura Basin boundary and was completed during early Burdigalian in the northern part of the Krosno Flysch Basin.
    [Show full text]
  • Original Orientation of Neptunian Dykes in the Pieniny Klippen Belt (Western Carpathians): the first Results
    Contributions to Geophysics and Geodesy Vol. 31/3, 2001 Original orientation of neptunian dykes in the Pieniny Klippen Belt (Western Carpathians): the first results R. Aubrecht Department of Geology and Paleontology, Faculty of Natural Sciences, Comenius University1 I. Túnyi Geophysical Institute of the Slovak Academy of Sciences2 A b s t r a c t : Measurements of neptunian dykes and their evaluation with utilizing of paleomagnetic correction for the first time provided data that enable to estimate orien- tation of the hypothetic Czorsztyn Swell. This ridge was individualized during Jurassic rifting and formed an axis of the so called Pienidic Domain. This domain was destroyed in the Alpine orogenic cycle. The basement of this zone was consumed, but the overly- ing sediments were preserved and now form the majority of the so called klippen in the Pieniny Klippen Belt which is now the most complex zone of the Western Carpathians. The klippen are tectonic blocks and lenses of mostly Jurassic limestones in softer, mostly Cretaceous envelope. As these remnants of Jurassic limestones are of different orientation, paleomagnetic corrections are necessary to complement any structural measurements in this zone. Callovian to Oxfordian neptunian dykes occurring in the Czorsztyn Unit, the sediments of which deposited in the shallowest parts of the Czorsztyn Swell, were taken as a direct indicator of the Jurassic extension. Four sites in western Slovakia were ex- amined, possessing larger networks of neptunian dykes: Babiná, Mesteèská skala, Vr¹atec and Bole¹ovská dolina. The mean orientation of the neptunian dykes was NE{SW (with N{S to ENE{WSW variations), which indicates also the most probable orientation of the Czorsztyn Swell.
    [Show full text]
  • Devonian Exotics in the Pieniny Klippen Belt Flysch And
    92 GeoLines 17 (2004) GeoLines 17 (2004) 93 tain numerous clasts cut by inherited joints filled by these veins. sandstone beds, and this handicaps the analysis of the faults. On The organization of inherited joints is very poor (Tokarski and the other hand, the offset is evident on the faulted clasts. Świerczewska, 2003). However, within the Witów series we have observed only very few veined clasts. It appears that the References long sedimentary transport resulted in decomposition of veined clasts and consequent absence of inherited joints. We conclude BRUD S. and WOROBIEC G., 2003. Results of investigations that the longer the sedimentary transport is, the better organiza- of macroscopic plant remains from the Witów series (south- tion of clast-scale joints can be visible. ern Poland) (in Polish). Przegląd Geol., 51: 392-401. (4) Most of the studied clast-scale joints are orientated sub- TOKARSKI A. K. and ŚWIERCZEWSKA A., 2003. Quater- perpendicular to perpendicular to the AB planes of the clasts, not- nary tectonic activity of the Bystrica overthrust in the Nowy withstanding orientation of the planes. This suggests that joints Sącz area (Outer Carpathians, Poland). In: W. ZUCHIE- form subperpendicular to the existing lithological boundaries, WICZ (Editor), Mater. V Ogólnopolskiej Konferencji “Neo- notwithstanding the orientation of the latter. tektonika Polski - Neotektonika a morfotektonika: metody (5) Within the Witów series, the direction of offset is only badan”, Kraków, 26-27.09.2003. Komisja Neotektoniki exceptionally visible on the metre-scale strike-slip faults that cut Kom. Bad. Czwart. PAN, ING UJ, Galicia T. Group, Kra- ków: Kraków: 67-69.
    [Show full text]
  • Pieniny Klippen Belt, Western Carpathians)
    Mineralia Slovaca, 43 (2011), 31 – 38 Web ISSN 1338-3523, ISSN 0369-2086 Lower Turonian radiolarians from the Červená skala section (Pieniny Klippen Belt, Western Carpathians) MIROSLAVA SMREČKOVÁ Department of Geography, Geology and Landscape Ecology, Matej Bel University, Tajovského 40, SK-974 01 Banská Bystrica, Slovak Republic; [email protected] Abstract The Cenomanian–Turonian deposits studied in the Červená skala section (Czorsztyn Succession of the Pieniny Klippen Belt) comprise pelagic facies belonging to the siliceous bed, in which abundant radiolarian and foraminiferal fauna was indentified. They indicate the deeper development of the Czorsztyn elevation of the Pieniny Klippen Belt. The radiolarians Alievium superbum (SQUINABOL), Crucella cachensis PESSAGNO, Patellula ecliptica O´DOGHERTY and Acanthocircus tympanum O´DOGHERTY have been used as marker fossils for the Cenomanian– Turonian boundary interval. On the basis of the ratio of Spumellaria and Nassellaria abundance, the siliceous bed may represent unstable environmental conditions connected with the eutrophication. Key words: radiolarians, Púchov Marls, Cretaceous, Czorsztyn Succession, Pieniny Klippen Belt, OMZ, Western Carpathians Introduction (1977). This paper brings the new taxonomical results concerning radiolarians selected from the Púchov Marls The Cenomanian–Turonian stratigraphic interval of the studied in the locality mentioned above. The qualitative Púchov Marls of the Czorsztyn Succession in the Pieniny and quantitative evaluations of these associations
    [Show full text]
  • Biostratigraphy of Deep-Water Agglutinated Foraminifera in Scaglia Rossa- Type Deposits of the Pieniny Klippen Belt, Carpathians
    15 Biostratigraphy of deep-water agglutinated Foraminifera in Scaglia Rossa­ type deposits of the Pieniny Klippen Belt, Carpathians, Poland KRZYSZTOF BilK ;:1Stitute of Geography, Cracow Pedagogical University, Podchorqiych 2, 30-084 Krak6w, Poland ABSTRACT A local biostratigraphical zonation based on agglutinated foraminifera, for Upper Cretaceous red deep-water pelagic deposits in the Polish part of the Pieniny Klippen Belt, is presented here. Studies were carried out based on 16 sections, to compare with results of earlier research. A standard zonal scheme of Geroch & Nowak (1984) was applied, with minor modifications. The Scaglia Rossa-type deposits in the Pieniny Klippen Belt represent the Plectorecurvoides alternalls (from Lower Cenomanian) through Goesella rugosa (through Upper Maastrichtian) zones. A correlation with the standard planktonic foraminiferal zones was established, enabling calibration of the OWAF to the standard chronostratigraphy. ~TRODUCTION Similar to the latter sections, red pelagic sedi­ C pper Cretaceous red marls and marly limestones ments occur in the Pieniny Klippen Belt (the often intercalated with thin-bedded greenish and Carpathians), representing facies deposited in a bluish, calcareous mudstones and sandstones are part of the Penninic Ocean - the northern part of the known from the Alps, Appenines and Penibetic Zone Western Tethys (Fourcade et aI., 1993). These facies as "Couches Rouge", "Scaglia Rossa" and "Capas are called the "Puchov beds" in the Ukrainian Rojas" facies. These sediments have a wide geo­ Carpathians (Glusko & Kruglov, 1971) or the graphic distribution in the Tethyan realm, charac­ "Kysuca beds" in the Slovak part of the Pieniny terizing pelagic deposition in the bathyal zones Klippen Belt (Scheibner & Scheibnerova, 1958).
    [Show full text]
  • Genesis of the Pieniny Klippen Belt in the Carpathians
    C. R. Geoscience 348 (2016) 15–22 Contents lists available at ScienceDirect Comptes Rendus Geoscience ww w.sciencedirect.com Tectonics, Tectonophysics Genesis of the Pieniny Klippen Belt in the Carpathians: Possible effects of a major paleotransform fault in the Neo-Tethyan domain Jean Chorowicz CNRS Institut des sciences de la Terre de Paris (iSTeP), Sorbonne universite´s, UPMC universite´ Paris 06, 4, place Jussieu, 75005 Paris, France A R T I C L E I N F O A B S T R A C T Article history: The Pieniny Klippen Belt (PKB) is a narrow, discontinuous zone rich in olistostromes and Received 29 May 2015 olistoliths (Klippen) in the western Carpathians. This paper, based on prior works Accepted after revision 14 October 2015 including tectonic and stratigraphic evidences, suggests that the PKB rocks were deposited Available online 25 November 2015 from the Triassic to the Early Paleogene along the eastern footwall of a major Split– Karlovac-Initial PKB-Crustal-Zone (SKICZ) paleotransform fault zone. This transform fault Keywords: was then separating the continental crust of the Austro-Alpine zone in the west and a Alps Carpathian Embayment Ocean in the east. It was only during the Late Paleogene–Early Carpathians Miocene that the PKB rocks were integrated into the accretionary prism that formed at the Dinarides front of the eastward-extruded ALCAPA units. This interpretation therefore supports the Paleotransform existence of a major paleotransform fault zone in the Neo-Tethys during the Triassic–Early Pieniny Klippen Belt Paleogeography Paleogene. This paleotransform had been previously suggested to explain the observed reversal in obduction and subduction at the junction between the eastern–southern Alps and the Carpathians–Dinarides.
    [Show full text]
  • Tectonics of the Klippen Belt and Magura Nappe in the Eastern Part of the Pieniny Mts. (Western Carpathians, Poland and Slovakia) – New Approaches and Results
    Tectonics of the Klippen Belt and Magura Nappe in the eastern part of the Pieniny Mts. (western Carpathians, Poland and Slovakia) – new approaches and results Oszczypko N.1, Jurewicz E.2 and Plašienka D.3 1Institute of Geological Sciences, Jagiellonian University, Oleandry 2a, PL-30-063, Kraków, Poland, [email protected] 2Faculty of Geology, University of Warsaw, Żwirki i Wigury 93, PL-02-089 Warszawa, Poland, [email protected] 3Department of Geology and Palaeontology, Faculty of Natural Sciences, Comenius University, Mlynská dolina, SK-842 15 Bratislava, Slovakia, [email protected] The Pieniny Klippen Belt (PKB) is a suture zone, which separates the Central Carpathians from the Outer Carpathians. The PKB successions are built up of the Lower/Middle Jurassic to Upper Cretaceous, dominantly pelagic and flysch deposits. The traditional multi-stage tectonic model of the PKB assumes that during the Palaeocene, retro- thrusting followed by subsidence and deposition of the “Magura Autochthonous Palaeogene” took place. Recently, we have studied the structural relationship of these deposits in the PKB, and we came to the conclusion that they belong to two formations with different tectonic positions. The Kremná Formation (?Oligocene – Lower Burdigalian) belongs to the Magura succession and appears in a tectonic window, beneath the Grajcarek thrust-sheet and the Czorsztyn (Sub-Pieniny) Nappe, while position of the Złatne Beds, which occur inside the Pieniny Nappe, is not clear. In the Slovak part the calcareous flysch sediments of the Jarmuta- Proč Formation described earlier as a “klippen mantle” form the youngest sedimentary member of the lowermost tectonic unit of the PKB, named here as the Fakľovka Unit.
    [Show full text]
  • Exotic Triassic Pelagic Limestone Pebbles from the Pieniny Klippen Belt of Poland: a Further Evidence for Early Mesozoic Rifting in West Carpathians
    Annates Societatis Geologorum Poloniae (1990), vol. 60: 003-044 EXOTIC TRIASSIC PELAGIC LIMESTONE PEBBLES FROM THE PIENINY KLIPPEN BELT OF POLAND: A FURTHER EVIDENCE FOR EARLY MESOZOIC RIFTING IN WEST CARPATHIANS Krzysztof Birkenmajer1, Heinz Kozur2 & Rudolf Mock3 1 Institute of Geological Sciences, Polish Academy of Sciences, Senacka 3, 31-002 Krakow, Poland 2 Rezsu u. 83, 1029 Budapest, Hungary 3Institute of Geology, J. A. Comenius University, Mlynskd dol. 3-2, 82-109 Bratislava, Czechoslovakia Birkenmajer, K., Kozur, H. & Mock, R., 1990. Exotic Triassic pelagic limestone pebbles from the Pieniny Klippen Belt of Poland: a further evidence for Early Mesozoic rifting in West Carpathians. Ann. Soc. Geol. Polon., 60: 003-044. Abstract: Exotic Triassic limestone pebbles from Upper Cretaceous conglomerates yielded microfaunal (mainly conodont and holothurian) evidence for pelagic conditions of sedimentation in the Pieniny Klippen Belt Basin, Carpathians, Poland, during the Carnian and Norian stages, the topmost Norian (topmost Sevatian) Misikella hernste- ini — Parvigondolella andrusovi Assemblage Zone inclusively. These Triassic rocks are developed in grey spotty limestone facies, lithologically very similar to the Fleckenkalk - Fleckenmergel facies of Lower-Middle Jurassic in Tethyan realm. This may suggest per­ sistence of open-sea carbonate sedimentation conditions in the axial part of the Klippen Belt Basin right through the Triassic (Rhaetian) — Liassic (Hettangian) boundary. To­ gether with earlier published data from the Pieniny Klippen
    [Show full text]
  • Geology of the Pieniny Klippen Belt of Poland: a Review of Latest Researches 1-36 ©Geol
    ZOBODAT - www.zobodat.at Zoologisch-Botanische Datenbank/Zoological-Botanical Database Digitale Literatur/Digital Literature Zeitschrift/Journal: Jahrbuch der Geologischen Bundesanstalt Jahr/Year: 1960 Band/Volume: 103 Autor(en)/Author(s): Birkenmajer Krysztof Artikel/Article: Geology of the Pieniny Klippen Belt of Poland: a review of latest researches 1-36 ©Geol. Bundesanstalt, Wien; download unter www.geologie.ac.at Jb. Geol. B. A. Bd. 103 S. 1—36 Wien, Sept. 1960 Geology of the Pieniny Klippen Belt of Poland by K. BIRKENMAJEE, Krakow, Poland (A review of latest researches) (Plate I, fig. 1—5) Contents Seite .Zusammenfassung, Abstract 1 Introduction 2 I. Klippen Series and Klippen Mantle 4 II. History of the Klippen Series geosyncline 7 II a. Primary substratum 7 II b. Triassic shelf deposits and early-Cimmerian synorogenic movements . 8 II c. Early stages of the Jurassic transgression 9 II d. Aalenian transformations of the geosynclinal trough and the evidence of the Central Cordillera 10 II e. Influence of the northern coast of the geosynclinal trough on the sedi­ mentation in the Bajocian and Bathonian 11 II f. Bathyal and abyssal deposits in the Dogger and in the Malm 12 II g. Upper Malm—Lower Neocomian sedimentation and the neo-Cimmerian synorogenic movements 13 II h. Influence of the Upper Neocomian synorogenic movements on the sedimentation of the Klippen Series 15 II i. Pelagic facies of the Middle Cretaceous and pre-orogenic flysch facies 16 II j. Orogenic movements of the sub-Hercynian phase and the nappe formation of the Pienids 18 III. Stratigraphy of the Exotic Massif situated between the Pienids and the Tatrids 19 IV.
    [Show full text]
  • The Middle Jurassic Succession in the Central Sector of the Pieniny Klippen Belt (Sprzycne Creek): Implications for the Timing of the Czorsztyn Ridge Development
    GEOLOGICA CARPATHICA, AUGUST 2015, 66, 4, 285—302 doi: 10.1515/geoca-2015-0026 The Middle Jurassic succession in the central sector of the Pieniny Klippen Belt (Sprzycne Creek): implications for the timing of the Czorsztyn Ridge development TOMASZ SEGIT1, BRONISŁAW A. MATYJA1 and ANDRZEJ WIERZBOWSKI2 1Institute of Geology, University of Warsaw, Żwirki i Wigury 93, 02-089 Warszawa, Poland; [email protected]; [email protected] 2Polish Geological Institute – National Research Institute, Rakowiecka 4, 00-975 Warszawa, Poland; [email protected] (Manuscript received November 22, 2014; accepted in revised form June 23, 2015) Abstract: In this study, we revisit the stratigraphic age and discuss sedimentary characteristics of the lower Middle Jurassic turbidite deposits (“black flysch”) of the Szlachtowa Formation, as well as the under- and overlying members of the Sprzycne Creek section situated in the central sector of the Pieniny Klippen Belt (Poland). We show that the succession captures the lower Middle Jurassic marine sediments of the pre-Late Albian Magura Basin, located to the north of an ancient submarine swell (Czorsztyn Ridge). The turbidite deposits of the Szlachtowa Formation and marly shales of the Opaleniec Formation yield dinoflagellate cysts indicative of the latest Aalenian or learliest Bajocian to Early Bathonian. The character of these deposits, and their location below the overthrusted Subpieniny Nappe show that this succession does not belong to the successions of the Oravicum domain, located on the southern side of the Czorsztyn Ridge. The Szlachtowa Formation is underlain by the Skrzypny Formation, which is reported for the first time outside the Oravicum domain.
    [Show full text]