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Early Paleogene planktic foraminifera in thin-sections : an experiment on isolated specimens from the Fore-Magura Thrust Sheet (Polish Outer Carpathians)

Baliniak W., Malata E.

Geological Quarterly

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2017

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Vol. 61, No. 3

655--681

EN

This paper describes results of an experiment aimed mainly at obtaining random thin-sections of isolated specimens of planktic foraminifera determined to a species level. Twenty species of uppermost Paleocene-Middle Eocene planktic foraminifera from pelagic variegated marls of the Fore-Magura Thrust Sheet have been chosen for this experiment. These planktic foraminifera belong to the genera Chiloguembelina, Turborotalia, Acarinina, Morozovella, Muricoglobigerina, Subbotina and Parasubbotina. Their SEM images, stereomicroscope photos of isolated specimens, and the experimental thin-sections along with their systematics and stratigraphic ranges are presented.

2

Mélanges and broken formations at the boundary zone of the Magura and Silesian nappes (Gorlice area, Polish Outer Carpathians) : a result of sedimentary and tectonic processes

Starzec K., Malata E., Wronka A., Malina L.

Geological Quarterly

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2015

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Vol. 59, No. 1

169--178

EN

Based on geological ﬁeld mapping, analyses of cores from explanatory wells, and foraminiferal age control data, we have differentiated a few types of mélanges and broken formations at the bordering zone between the Magura and Silesian nappes (Gorlice area in the Polish Outer Carpathians). These mélanges and broken formations differ in composition and structure due to different settings and processes of their formation. Several levels of broken formation within the uppermost part of the Krosno Beds were formed as mass-transport deposits at the southern slope of the Silesian Basin. They may record tectonic pulses related to advancing accretionary wedge within Magura area and directly predate the stage of the larger-scale sedimentary mélange formation at the front of the wedge. This mélange is composed mainly of the material representing the Magura succession (Siary Subunit) and the Krosno type sediments of the Silesian succession. It was emplaced within the Silesian basin in the Early Miocene time. The so-called “Harklowa peninsula”, whose geological structure has been the subject of discussions and various interpretations in the past years, is built of this type of mélange. The other recognized type of broken formation and mélange represents the chaotic bodies formed at the base of the Magura Nappe.The results of our studies contribute to better understanding of the structural evolution of this part of the Outer Carpathians

3

Preliminary remarks on enigmatic "white casing limestone" from Saqqara archaeological site in Egypt

Welc F, Malata E., Marks L., Studencka B., Olszewska B.

Studia Quaternaria

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2013

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Vol. 30, Nr 2

115--123

EN

Saqqara is one of the famous archaeological sites in the world. There is the oldest stone pyramid built by pharaoh Djoser from the Third Dynasty (around 4600 yrs BP). The components of his funerary complex were constructed of a characteristic creamish-white limestone of relatively great solidity, connected in archaeological literature with the white casing limestone from Saqqara. A source of this stone has remained so far a mystery. An extensive geological survey and other research has failed to identify any outcrops of such limestone in the vicinity of Saqqara. Preliminary results of examination of fossils from relevant rock samples of the white Saqqara limestone are presented, supplemented with discussion of current opinions concerning its origin and probable stratigraphic setting.

4

Cretaceous (Aptian/Albian-?Cenomanian) age of “black flysch” and adjacent deposits of the Grajcarek thrust-sheets in the Male Pieniny Mts. (Pieniny Klippen Belt, Polish Outer Carpathians)

Oszczypko N., Olszewska B., Malata E.

Geological Quarterly

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2012

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Vol. 56, No 3

411--440

EN

Several sections record the relation between the “black flysch” and Upper Cretaceous red shales in the Grajcarek thrust-sheets. In all the sections studied the “black flysch” appears in the core of imbricated folds or thrust-sheets, whereas the limbs are composed of Upper Cretaceous deposits. The transitional beds between the “ black flysch” and the Upper Cretaceous red shales are composed of green and black bituminous shales, green and red radiolarites and cherty limestones. Biostratigraphical investigations have revealed a similar type and sequence of microfauna assemblages in all the sections studied and significant redeposition of Jurassic calcareous benthic foraminifera, calcareous nannoplankton, molluscs, sponge spicules and crinoid elements. The Cretaceous age (Aptian/Albian-?Cenomanian) of the “black flysch” is shown by the presence of agglutinated foraminifera and microfacies data. These deposits are underlain by a Kimmeridgian-Aptian radiolarite/limestone condensed succession and overlain by Turonian-Campanian hemipelagic red shales and Maastrichtian/Lower Paleocene conglomerates and thick-bedded silicilastic turbidites of the Jarmuta Formation. Such a sequence of deposits is typical of the Outer Carpathian basins and records the global Mid/Late Cretaceous phenomena in the world ocean, followed by the Cretaceous Oceanic Red Beds.

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Late Jurassic - Early Cretaceous volcanism in the Ukrainian part of the Carpathians

Krobicki M., Golonka J., Malata E., Oszczypko N., Słaby E., Słomka T.

Volumina Jurassica

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2006

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Vol. 4, no. 1

52-53

EN

Today the Ukrainian Mesozoic volcanic rocks are located in the relatively small area. They are concentrated near the Rachiv Massif and Chivchin Ridge, generally in the front of the Rahiv and Maramuresh (=Marmaros) nappes (Outer Flysch Carpathians) and in the Pieniny Klippen Belt. Several outcrops in these regions were studied in details by present authors. Rachiv nappe contains basaltic flows with numerous pillow lava horizons, ophicalcite(?) and with lava breccias on the top of volcanic sequence (Trostianets stream), as well as basaltic and tuffitic breccias (Lemskij stream). Maramuresh nappe contains andesites, basalts and tuffitic breccias often associated with light-grey micritic and coral limestones of Âtramberk-type facies (Kamennyj Potok stream). Most spectacular region of distribution of magmatic rocks belongs to Maramuresh unit and is located between Margetul, Radomir and Kwasnyj streams. These rocks are represented mainly by massive and pillow basalts, basaltic and tuffitic breccias and diabases as well as porphyritic conglomeratic/breccias. Usually they build huge klippes up to 50 meters and more. The contacts between huge pillow basaltic flows and surrounding deposits are usually covered by debris or vegetation but in Margetul stream the relationship between pillow lavas and pelagic, micritic limestones with cherts (Cieszyn Limestone Formation type) is very well visible. In the lower part of section small lenses of basaltic rocks occur within these limestones and basaltlimestone ratio increases upwards. Latest Jurassic - earliest Cretaceous age of these limestones was established helping to determine crucial age of a magmatic event to understand most important wide geodynamic processes. The basaltic rocks with pillow lavas are exposed in Veliky Kamenets quarry within Ukrainian part of the Pieniny Klippen Belt. These basalts cover the Middle Jurassic - lowermost Creataceous carbonate sequence, the contact is sharp and basaltic dykes also penetrate underlying Calpionella limestones. Above these basalts, there are younger limestones rich both in ammonites and benthic fauna (brachiopods, bivalves and crinoids) and they are overlain by 1 meters thick tuffites. The youngest deposits in the Veliky Kamenets section are yellowish limestone breccias showing presence of abundant Berriasian calpionellids. Sedimentological features of this breccia indicate submarine erosion connected with synsedimentary movements of the sea bottom causing redeposition of older rocks - in this case Calpionella limestones and basaltic fragments. These sediments correspond very well with Walentowa Breccia Member of the Dursztyn Limestone Formation which originated after strong Neo-Cimmerian uplift of the Czorsztyn Ridge. Additionally, in Vulhovchik stream, just below Veliky Kamenets hill, Jurassic/Cretaceous trachydolerites occur. These magmatic events correspond very well with major plate reorganization, which happened during the Tithonian time within western Tethyan Ocean. In the same time the Outer Carpathian rifts were developed with the extensional type of volcanism (teschenites) and the Silesian Basin originated as a result of such rifting process. The presumable triple-junction zone comprises the Rahiv-Sinaia zone (first arm), Silesian (second one) and its extension into the Pieniny Klippen Belt/Magura Basin (third arm). The origin of this triple junction is perhaps related to the opening of the Central Atlantic-Ligurian-Penninic oceanic system.

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Lithostratigraphy and biostratigraphy of the Upper Albian-Lower/Middle Eocene flysch deposits in the Bystrica and Rača subunits of the Magura Nappe (Beskid Wyspowy and Gorce Ranges; Poland)

Oszczypko N., Malata E., Bąk K., Kędzierski M., Oszczypko-Clowes M.

Annales Societatis Geologorum Poloniae

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2005

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Vol. 75, No. 1

27--69

EN

LithostratigraphyandbiostratigraphyoftheBystricaandRaèasubunitsoftheMaguraNappehavebeen studied in the southern part of the Beskid Wyspowy Range and on the northern slopes of the Gorce Range (Polish part of the Western Flysch Carpathians). Six new lithostratigraphic units (Jasień Formation, Białe Formation, Jaworzynka Formation, Szczawina Sandstone Formation, Krzysztonów Member, and Ropianka Formation) of the UpperAlbian–Palaeocene age have been established, and five other units (Malinowa Shale Formation, Hałuszowa Formation, Łabowa Shale Formation, Beloveza Formation, Bystrica Formation) have been additionally described. The newly created formations as well as the Malinowa Shale Formation and the Hałuszowa Formation have been included to a new Mogielica Group of units (Upper Albian–Palaeocene). This group of units passes upwards into the Beskid Group (Eocene–Oligocene).The Mogielica Group, spanning over 40 myrs, represents the turbidite depositional system, separated by highstand variegated clays which can be correlated with minor sequences in terms of sequence stratigraphy. The following biostratigraphic zones have been recognised in the Cretaceous–Lower/Middle Eocene deposits: Plectorecurvoides alternans, Bulbobaculites problematicus, Uvigerinammina jankoi, U. jankoi-C. gigantea, Caudammina gigantea, Remesella varians, Rzehakina fisistomata, Glomospira div. sp., and Saccamminoides carpathicus. A few lithostratigraphic units consisting of calcareous sediments have been correlated with the standard calcareous nannoplankton zonation and the chronostratigraphy.

PL

Płaszczowina magurska, największa jednostka tektoniczna zewnętrznych Karpat Zachodnich (Fig. 1), jest całkowicie odkorzeniona od swego podłoża. Utwory serii magurskiej starsze od turonu znane są jedynie z jednostki Grajcarka (sukcesja magurska pienińskiego pasa skałkowego), wiercenia Obidowa IG-1 oraz z kilku niewielkich odsłonięć przy południowym obrzeżeniu okna tektonicznego Mszany Dolnej (Fig. 2, por. Birkenmajer & Oszczypko, 1989). W jednostce Grajcarka, ponad głębokowodnymi utworami jury górnej i neokomu, występuje “czarny flisz” formacji wronińskiej (alb-cenoman) oraz zielone łupki radiolariowe cenomanu (formacja hulińska) (Birkenmajer, 1977, por. Oszczypko et al., 2004). Szaro-zielone łupki plamiste albu-cenomanu, znane z południowego obrzeżenia okna tektonicznego Mszany Dolnej, zdefiniowane zostały w pracy jako formacja łupków z Jasienia. Formacja ta, o miąższości niemniejszej od kilkunastu metrów, zazębia się w stropie z łupkami czerwonymi formacji z Malinowej. W Beskidzie Wyspowym i Gorcach ponad łupkami pstrymi formacji z Malinowej (turon-santon/kampan) oraz poniżej łupków pstrych formacji z Łabowej (eocen dolny i środkowy) występują zróżnicowane facjalnie osady fliszowe, zaliczane dotychczas do różnych nieformalnych jednostek litostratygraficznych, takich jak: warstwy z Kaniny, piaskowce ze Szczawiny (strefa bystrzyck i raczańska) oraz warstwy z Jaworzynki (strefa raczańka i strefa Siar). Najwyższą pozycję stratygraficzną zajmują utwory tradycyjnie nazywane “warstwami inoceramowymi” lub ropianieckimi. Na podstawie szczegółowych badań lito- i biostratygraficznych wyżej wymienionych utworów kredy górnej i paleocenu, zaproponowano cztery nowe formalne jednostki litostratygraficzne w randze formacji: formację z Białego (dotychczasowe warstwy z Kaniny), formację piaskowców ze Szczawiny (dotychczasowe piaskowce ze Szczawiny), formację z Jaworzynki (dotychczasowe warstwy z Jaworzynki) oraz formację ropianiecką (dotychczasowe warstwy ropianieckie). Ponadto badano pięć innych górnokredowo-eoceńskich formacji: łupków z Malinowej, z Hałuszowej, łupków z Łabowej, beloweskiej i bystrzyckiej, które dodatkowo opisano. Wszystkie nowo zdefiniowane formacje oraz formacje: łupków z Malinowej oraz z Hałuszowej, włączono do nowo wydzielonej grupy Mogielicy (górny alb-paleocen). Grupa ta przechodzi w stropie w grupę beskidzką (eocen-oligocen) opisaną przez Bir- kenmajera & Oszczypkę (1989). Grupa Mogielicy, obejmująca okres czasowy liczący ponad 40 mln lat, reprezentowana jest przez turbidytowy system depozycyjny, ograniczony w stropie i spągu przez osady łupków pstrych, związanych z okresem wysokiego względnego poziomu morza. Wśród zespołów mikrofauny otwornicowej albu - dolnego/ środkowego eocenu, znalezionych w badanych utworach płaszczowiny magurskiej, rozpoznano większość poziomów biostratygraficznych opracowanych dla polskich Karpat zewnętrznych przez Gerocha & Nowaka (1984) oraz przez Olszewską (1997). Do tego schematu włączono również poziomy charakterystyczne dla utworów płaszczowiny magurskiej. Poziom Plectorecurvoides alternans (poziom interwałowy IZ) Definicja: dolna granica - pojawienie się gatunku Plectorecurvoides alternans Noth (w badanym materiale dolna granica nie jest uchwycona, odpowiada początkowi profilu sukcesji magurskiej), górna granica - pojawienie się Bulbobaculites problematicus (Neagu);

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Sedimentary conditions in the Siary zone of the Magura basin (Carpathians) in the late Eocene-early Oligocene

Leszczyński S., Malata E.

Annales Societatis Geologorum Poloniae

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2002

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Vol. 72, No 3

201-239

EN

The sediments of the upper Eocene (Priabonian)-lower Oligocene (Rupelian) of the Siary zone in the Magura nappe (basically Magura Beds in glauconitic facies) display features indicating their origination in sedimentary conditions quite different from those in which coeval sediments from the other parts of the Carpathians were deposited. This paper aims at interpreting the sedimentary conditions on the basis of lithofacies, their vertical and lateral distribution, foraminifera assemblages, CaCO3 and organic matter content determined in six transects through the entire Siary zone, the contents of main and trace elements determined in 11 samples from one section and different published data. Lithofacies and the present day shape of the Siary zone suggest sedimentation of the entire succession in a strongly elongated confined basin. Facies distribution indicates deposition on a submarine ramp that gradually expanded to NE and E along the slopes of the outer basin margin. Assemblages of foraminifera suggest location of the basin bottom below the foraminiferal lysocline. Moreover, foraminifera together with bioturbation structures and sediment geochemistry indicate sedimentation mainly in weakly oxic, close to dysoxic bottom waters. The differences in facies in relation to the coeval deposits of the other parts of the Carpathians are interpreted as resulting mainly from intense resedimentation in the Siary zone during the Priabonian-Rupelian, and in part from the relatively low calcium carbonate supply. Gradual expansion of resedimentation towards NE, followed by a decrease in the supply of coarse-grained material is regarded as due to lithosphere rollback beneath the evolving Carpathians. This process is interpreted as of superior significance in controlling sedimentation during the Priabonian-Rupelian not only in the Siary zone but also in the entire Magura basin. This was the factor responsible for forcing the subsidence of the Magura basin, accretionary wedge development in its inner part, and fore-bulging of the area at some distance in front of the zone of the rolling back lithosphere, i.e. in the source area of the sedimentary succession in question. Finally, this process also caused drowning and burying of the source area.

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Budowa geologiczna Krynicy (płaszczowina magurska)

Oszczypko N., Malata E., Oszczypko-Clowes M., Duńczyk L.

Przegląd Geologiczny

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1999

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Vol. 47, nr 6

549-559

PL

Krynica jest usytuowana w południowo-wschodniej części płaszczowiny magurskiej na styku podjednostki sądeckiej (bystrzyckiej) i krynickiej (ryc. 1). W strefie sądeckiej (NE ) występują wyłącznie utwory formacji magurskiej wieku środkowo-górno-eoceńskiego. Należy do nich ogniwo z Maszkowic (piaskowce gruboławicowe), ogniwo łupków z Mniszka (łupki pstre i cienkoławicowy flisz) oraz ogniwo piaskowców popradzkich ("piaskowce zuberowskie"). Do strefy krynickiej należą paleoceńsko-środkowo-eoceńskie utwory formacji szczawnickiej (cienko- i średnioławicowy flisz), zarzeckiej (cienkoławicowy flisz z ogniwem piaskowców krynickich) oraz formacja magurska (piaskowce gruboławicowe). Podjednostki sądecka (bystrzycka) oraz krynicka kontaktują ze sobą wzdłuż prawie pionowego uskoku inwersyjnego, zapadającego na NE. Uskoki poprzeczne o kierunku NE-SW dzielą obie podjednostki na kilka bloków. Między Czarnym Potokiem a Słotwinami wąski półrów tektoniczny towarzyszy uskokowi słotwińskiemu.