12-14 September 2022 LJUBLJANA, SLOVENIA 15TH Emile Argand Conference on Alpine Geological Studies ABSTRACT BOOK & FIELDTRIP GUIDE 15TH Emile Argand Conference on Alpine Geological Studies 12-14 September 2022, Ljubljana, Slovenia Abstract book & fieldtrip guide 15th Emile Argand Conference on Alpine Geological Studies Congress organisers: 12-14 September 2022, Ljubljana, Slovenia Faculty of Natural Sciences and Engineering, Abstract book and fieldtrip guide Electronic edition Geological Survey of Slovenia and © 2022, Faculty of Natural Sciences and Engineering, Ljubljana https://www.alpshop2022.eu/ Slovenian Geological Society Chief editor: Boštjan Rožič Editors: Boštjan Rožič, Petra Žvab Rožič Organising Committee: Boštjan Rožič (chair), Marko Vrabec (vice chair), Rok Brajkovič, Luka Graphic design concept: Gale, Matevž Novak, Tomislav Popit, Andrej Šmuc, Petra Žvab Rožič Maja Kotar, Karin Moder, Maša Planinc (within the course Typeface Design, academic program Graphic and Interactive Communication, Scientific committee: academic year 2020/2021, mentors Nace Pušnik, Gregor Franken) Alfons Berger (University of Bern, Switzerland) László Fodor (Eötvös Loránd University, Hungary), Cover picture: István Főzy (Hungarian Natural History Museum, Hungary) Mangart Saddle, photographed in direction to the south (author: Nikolaus Froitzheim (University of Bonn, Germany) Tomislav Popit) Mark Handy (Freie Universität Berlin, Germany) György Hetényi ( University of Lausanne , Switzerland) Issued and published by: Hazim Hrvatović (Geological survey of Federation of Bosnia and University of Ljubljana, Faculty of Natural Sciences and Engineering, Herzegovina, BiH) Department of geology, Aškerčeva 12, 1000 Ljubljana Michał Krobicki (AGH University of Science and Technology, Poland) Represented by: Boštjan Rožič Paola Manzotti (Stockholm University, Sweden) Othmar Müntener (University of Lausanne , Switzerland) All abstracts are peer-reviewed. Franz Neubauer (University of Salzburg , Austria) Authors are responsible for the language and content of the abstracts. Dušan Plašienka (Comenius University Bratislava, Slovakia) Jan Pleuger (Freie Universität Berlin, Germany) Claudio Rosenberg (Sorbonne Université, France) Boštjan Rožič (University of Ljubljana, Slovenia) Kataložni zapis o publikaciji (CIP) pripravili v Narodni in univerzitetni Stefan Schmid (ETH Zürich, Switzerland) knjižnici v Ljubljani Ralf Schuster (Geological Survey of Austria, Austria) COBISS.SI-ID 119335683 Christian Sue (University of Franche-Comté, France) ISBN 978-961-6047-96-8 (PDF) Kristina Šarić (University of Belgrade, Serbia) Andrej Šmuc (University of Ljubljana, Slovenia) Bruno Tomljenović (University of Zagreb, Croatia) Kamil Ustaszewski (Friedrich-Schiller University Jena, Germany) Marko Vrabec (University of Ljubljana, Slovenia) 15th Emile Argand Conference on Alpine Geological Studies is part of EGU conference series. 15TH WORKSHOP 15th Emile Argand Conference on Alpine Geological Studies, 12-14 September 2022, Ljubljana, Slovenia. Content Abstract book Kishan Aherwar, Michal Šujan, Rastislav Vojtko, Régis Braucher, Andrej Chyba, Jozef Hók, Barbara Rózsová and Aster Team Dating a long-lived lake in an intermontane basin: Late Miocene Lake Turiec in the Western Carpathians ....................................11 Gianni Balestro, Alessandro Borghi, Sara De Caroli, Eedoardo Barbero and Andrea Festa Multistage tectono-stratigraphic evolution of the Canavese Zone (Western Alps) ...........................................................................12 Philipp Balling, Bruno Tomljenović and Kamil Ustaszewski The inversion of a passive continental margin portrayed by a 2D balanced kinematic forward model across the Velebit Mt. in the northern external Dinarides fold and thrust belt ...................................................................................................................13 Šime Bilić, Vesnica Garašić, and Alan B. Woodland Two types of peridotites in the area of Banovina, Croatia and their Petrogenesis ...........................................................................14 Olga Brunsmann, Marisa Germer, Alexandra Pohl, Victoria Kohn, Vincent Könemann, Xin Zhong, Jan Pleuger and Timm John Barometric studies on different rock types from the Adula Nappe (Central Alps) by Raman spectroscopy of quartz inclusions in Garnet ........................................................................................................................................................................15 Quentin Brunsmann, Claudio Rosenberg, Nicolas Bellahsen and Giancarlo Molli The arc of the western Alps: a review and new kinematic model....................................................................................................16 Ruihong Chang, Franz Neubauer, Johann Genser, Yongjiang Liu, Sihua Yuan, Qingbin Guan and Qianwen Huang Hf isotopic constraints for Austroalpine basement evolution of Eastern Alps: review and new data ...............................................17 Stefania Corvò, Matteo Maino, Sandra Piazolo, Andrew Kylander-Clark, Silvio Seno and Antonio Langone Multiscale lithological and structural heterogeneity control on the nucleation of a crustal shear zone: petro-structural investigation and U-Pb titanite dating from the Anzola shear zone (Ivrea-Verbano Zone, Southern Alps) ......................................18 László Fodor, Attila Balázs, Gábor Csillag, István Dunkl, Gábor Héja, Péter Kelemen, Szilvia Kövér, András Németh, Anita Nyerges, Dániel Nyíri, Éva Oravecz, Ildikó Selmeczi, Balázs Soós, Lilla Tőkés, Marko Vrabec and Csilla Zadravecz Migration of basin formation and contrasting deformation style in the south-western Pannonian Basin (central Europe) .............19 Hans-Jürgen Gawlick Middle-Late Jurassic ophiolite obduction and formation of sedimentary mélanges in the Western Tethys Realm ...........................20 David Gerčar, Nina Zupančič, Anna Waśkowska, Jernej Pavšič and Boštjan Rožič Upper Campanian bentonites of volcaniclastic origin in the Scaglia-type limestones of the Adria continental margin ...................21 Stefano Ghignone, Emanuele Scaramuzzo, Mattia Gilio, Marco Bruno, Franz Livio, and Matteo Alvaro First evidence of UHP in the Lago Superiore Unit (Monviso, Western Alps) ...................................................................................22 Mattia Gilio, Hugo W. van Schrojenstein Lantman, Alice Girani, Ross J. Angel, Marco Scambelluri and Matteo Alvaro The prograde history of three Mn-rich garnets from the UHP Lago di Cignana Unit (Italy) ............................................................23 Edwin Gnos, Josef Mullis, Emmanuelle Ricchi, Christian Bergemann, Emilie Janots, and Alfons Berger Episodes of open fissure formation in the Alps ................................................................................................................................24 Jacek Grabowski, Jolanta Iwańczuk, Daniela Rehakova, Boštjan Rožič, Petra Žvab Rožič, Andrzej Chmielewski, Lucjia Slapnik and David Gerčar Magnetic susceptibility and chemostratigraphy of the Jurassic/Cretaceous boundary interval – new data from the Slovenian Basin ...............................................................................................................................................................................................25 Andrew Greenwood, György Hetényi, Luca Ziberna, Mattia Pistone, Alberto Zanetti, Othmar Müntener and Project DIVE Team Project DIVE (Drilling the Ivrea-Verbano zonE): A joint petrological, geochemical, and geophysical exploration of the lower continental crust .............................................................................................................................................................................26 Christoph Grützner, Mattis Grenier, Jakob Stubenrauch, Markus Hermann, Klaus Reicherter and Kamil Ustaszewski Remote sensing of active tectonics in NE Italy, eastern Southern Alps ............................................................................................27 Istvan Gyorfi, Laura Petrescu and Felix Borleanu Alpine-Carpathian-Pannonian Geodynamics: the McKenzie and Royden models and the limitations of their applicability .............28 3 15TH WORKSHOP 15th Emile Argand Conference on Alpine Geological Studies, 12-14 September 2022, Ljubljana, Slovenia. Mark R. Handy and the members of 4D-MB and the AlpArray Working Group How AlpArray is guiding us to a new model of Alpine orogenesis ..................................................................................................29 Gábor Héja, Katalin Lőrincz, László Bereczki, Gábor Markos, Gyula Maros, and Márton Palotai A buried fold and thrust belt: the structural geometry of the central part of the Tisza Unit, East Hungary ....................................30 Eva Hoppanová, Štefan Ferenc, Viera Šimonová, and Richard Kopáčik New knowledge about U-Cu mineralization in the Kozie Chrbty Mts. and its relationship to the late (Neotectonic) structures (Hronic Unit, Western Carpathians, Slovakia) ................................................................................................................31 Bastien Huet, Nicolas Bellahsen, Nicolas Loget, Eric Lasseur, and Justine Briais Palaeoenvironmental and drainage network reconstitution of the Oligocene Western Alpine Foreland Basin ................................32 Jolanta Iwańczuk, Mathieu Martinez and Kinga Bobek Recording of cyclicity in the sediments of the Bajocian and Lower Bathonian on the basis of magnetic susceptibility (Carpathians, Poland) .....................................................................................................................................................................33 Viktor Karádi On the way to building the Norian conodont biozonation of the Circum-Pannonian Region ..........................................................34 Emanuel Kästle and the AlpArray Working Group Crustal structure in the eastern Alps from ambient-noise Tomography ...........................................................................................35 Miklos Kazmer and Krzysztof Gaidzik Seismic activity along the Periadriatic and Sava Faults in the past two millennia – an archaeoseismological assessment ...............36 Anja Kocjančič, Boštjan Rožič, Luka Gale, Primož Vodnik, Tea Kolar-Jurkovšek and Bogomir Celarc Facies analysis of Ladinian and Carnian beds in the area of Rute Plateau (External Dinarides, Central Slovenia) ..........................37 Michał Krobicki Origin of submarine swell (Czorsztyn Ridge of the Pieniny Klippen Belt, Polish/Ukrainian Carpathians) and it’s geotectonic consequences by biostratigraphy/volcano-sedimentary record .......................................................................................................38 Eline Le Breton, Mark R. Handy, Peter McPhee, Azam Jozi-Najafabadi and Christian Haberland Variation in style of Adriatic lower crust indentation west and east of the Giudicarie Fault ............................................................39 Georg Löwe, Dejan Prelević, Blanka Sperner, Susanne Schneider, Jörg A. Pfänder, Philipp Balling, Sami Nabhan, Albrecht von Quadt Wykradt-Hüchtenbruck and Kamil Ustaszewski Exhumation of metamorphic core complexes of the internal Dinarides was triggered by the opening of the Pannonian Basin ......40 Matteo Maino, Filippo Schenker, Leonardo Casini, Stefania Corvò, Michele Perozzo, Antonio Langone and Silvio Seno Challenges in the interpretation of the structural and metamorphic record in the Adula and Cima Lunga units (Central Alps) ....41 Paola Manzotti, Federica Schiavi, Francesco Nosenzo, Pavel Pitra and Michel Ballèvre A journey towards the forbidden zone: a new, cold, UHP unit in the Dora-Maira Massif (Western Alps) .......................................42 Emö Márton, Vlasta Ćosović, Katica Drobne, Alan Moro, Damir Bućković and Gábor Imre Tectonic implications of paleomagnetic results from the Northern Adriatic area: an overview .......................................................43 Hans-Joachim Massonne and Botao Li Pressure-temperature-time evolution of Austroalpine metamorphic rocks from the southeastern Pohorje Mountains ....................44 John Milsom and Jenny Anne Barretto Anagolay: the shape of the Philippines and the Luzon Syntaxis ......................................................................................................45 Giulia Mingardi, Mattia Gilio, Francesco Giuntoli, Kira A. Musiyachenko and Matteo Alvaro Quartz and zircon in garnet elastic geobarometry of HP rocks from the Sesia Zone .......................................................................46 Ana Mladenović How active is recent tectonics in the central Balkans: Evidence from the Serbian Carpatho-Balkanides .........................................47 Milica Mrdak, Hans-Jürgen Gawlick, Nevenka Đerić, Martin Đaković and Milan Sudar Partial drowning or backstepping of the Early Norian Dachstein Carbonate Platform in the Dinarides (Poros, Montenegro) .........48 Mark Mücklisch, Christoph Grützner, Erick Prince, Sumiko Tsukamoto and Kamil Ustaszewski New data on the Late Pleistocene evolution of the Klagenfurt Basin, Austria .................................................................................49 4 15TH WORKSHOP 15th Emile Argand Conference on Alpine Geological Studies, 12-14 September 2022, Ljubljana, Slovenia. Francesco Nosenzo, Michel Ballèvre, and Paola Manzotti Nappe stacking and syn-nappe folding in the northern Dora-Maira Massif (Western Alps) ............................................................50 Veleda Astarte Paiva Muller, Christian Sue, Pierre Valla, Pietro Sternai, Thibaud Simon-Labric, Cécile Gautheron, Joseph Martinod, Matias Ghiglione, Lukas Baumgartner, Fréderic Hérman, Peter Reiners, Djordie Grujic, David Shuster, Jean Braun, Laurent Husson and Matthias Bernet Exhumation response to climate and tectonic forcing in the southern Patagonian Andes (Torres del Paine and Fitz Roy plutonic complexes) ........................................................................................................................................................................51 Michele Perozzo, Matteo Maino, Filippo Schenker and Silvio Seno Discovery of sheath folds in the Adula nappe and implications for the tectonic evolution (Central Alps) .......................................52 Dušan Plašienka, Marína Molčan Matejová, and Tomáš Potočný Lower to Middle Jurassic clastic formations of the Western Carpathian Klippen Belt: testimony to the rifting-breakup-drifting Processes .............................................................................................................................................53 Hannah Pomella, Thomas Klotz, Anna-Katharina Sieberer, Martin Reiser, Peter Tropper and Ralf Schuster The thermotectonic evolution in front of the Dolomites Indenter ...................................................................................................54 Tomáš Potočný and Dušan Plašienka Calcite microstructures recording polyphase deformation history of the Meliata Unit ....................................................................55 Erick Prince, Sumiko Tsukamoto, Christoph Grützner, Marko Vrabec and Kamil Ustaszewski Finding Quaternary Seismogenic Activity Along the Eastern Periadriatic Fault System: Dating of Fault Gouges via Electron Spin Resonance ...............................................................................................................................................................................56 Luca Reato, Monika Huraiová, Patrik Konečný and Vratislav Hurai Formation of esseneite and kushiroite in calc-silicate skarnoid xenoliths from Southern Slovakia..................................................57 Martin Reiser, Christoph Iglseder, Ralf Schuster, David Schneider and Daniela Gallhofer Age and structure of the Stubai Alps (Ötztal-Nappe, Tyrol/Austria) ...............................................................................................58 Boštjan Rožič, Anja Kocjančič, Luka Gale, Tomislav Popit, Petra Žvab Rožič, Primož Vodnik, Nina Zupančič, Rok Brajkovič and Tea Kolar-Jurkovšek Architecture and sedimentary evolution of the Ladinian Kobilji curek Basin of the External Dinarids (Rute Plateau, central Slovenia) .........................................................................................................................................................................................59 Emanuele Scaramuzzo, Franz A. Livio and Maria Giuditta Fellin From Permian to rift-inception: new insight from the Western Southern Alps (Varese Area) ..........................................................60 Benjamin Scherman, Boštjan Rožič, Ágnes Görög, Szilvia Kövér and László Fodor Platform to basin transitions: mapping observations at the Krvavica Mountain, and Čemšeniška Planina, in the Sava Folds Region .............................................................................................................................................................................................61 Ralf Schuster, Christoph Iglseder, Martin Reiser and Daniela Gallhofer Geological history of the Troiseck-Floning Nappe (Austroalpine unit, Styria/Austria) ....................................................................62 Anna-Katharina Sieberer, Ernst Willingshofer, Thomas Klotz, Hugo Ortner and Hannah Pomella Internal deformation and tectonic evolution of the Dolomites Indenter, eastern Southern Alps: A combined field and analogue modelling study ...............................................................................................................................................................63 Duje Smirčić, Matija Vukovski, Damir Slovenec, Duje Kukoč, Mirko Belak, Tonći Grgasović, Branimir Šegvić and Luka Badurina Differentiation and genesis of the Middle Triassic mafic volcanic and volcaniclastic facies in NW Croatia - case study from Vudelja quarry .................................................................................................................................................................................64 Christian Sue, Andrea Walpersdorf, Dorian Bienveignant, Lina Al Najjar, Estelle Hannouz, Anne Lemoine and Stephane Baize Tectonic Transfer from the Western Alpine Front to the French Rhône Valley in its 3D-Structural Context ....................................65 Samir Ustalić, Marián Putiš, Ondrej Nemec, Peter Ružička, Elvir Babajić and Petar Katanić Petrography of ultrabasic and basic rocks from the Ozren ophiolite complex (Bosnia and Herzegovina) .......................................66 Matija Vukovski, Duje Kukoč, Tonći Grgasovic, Ladislav Fuček, and Damir Slovenec Jurassic pelagic succession of NW Croatia – a key to better understanding tectonic setting of the Southern Alps – Dinarides transition zone ................................................................................................................................................................................67 5 15TH WORKSHOP 15th Emile Argand Conference on Alpine Geological Studies, 12-14 September 2022, Ljubljana, Slovenia. Marija Vuletić, Hans-Jürgen Gawlick, Nevenka Đerić, László Bujtor, Katarina Bogićević and Draženko Nenadić The Albian/Cenomanian Boundary Event (OAE1d) reflected in ammonite-rich layers in central Serbia (Topola area) ..................68 Iris Wannhoff, Jan Pleuger, Timm John, Xin Zhong, and Moritz Liesegang Peak pressure estimates of Koralpe-Saualpe-Pohorje Complex based on Raman Spectroscopy .......................................................69 Davide Zanoni, Marco Filippi, Manuel Roda, Alessandro Regorda, and Maria Iole Spalla Tectonic and metamorphic record in the Badstub Formation, Carboniferous of Nötsch, Austroalpine ............................................70 Fieldtrip guide Boštjan Rožič, Matevž Novak, Luka Gale, Andrej Šmuc, Duje Kukoč and Stanka Šebela Adria margin of the Alpine-Dinaric transition area – sedimentary view and a structural glimpse ...................................................75 László Fodor, Kristina Invančič, Marian Janák, Marko Vrabec, Mirijam Vrabec Metamorphism, deformation, exhumation, and basin formation in NE Slovenia, in the Pohorje-Kozjak Mts. .................................97 Luka Gale, Marko Vrabec, Tomaž Hitij Marine reptile-bearing Anisian limestone of the Velika planina mountain pasture .......................................................................121 Rok Brajkovič, Petra Žvab Rožič, Luka Gale Lower to Middle Jurassic limestone succession at the margin of the Ljubljana Moor: From microfacies to the Romans ...................128 Matevž Novak Geological tour of Ljubljana ..........................................................................................................................................................133 Index of authors 6 15TH WORKSHOP 15th Emile Argand Conference on Alpine Geological Studies, 12-14 September 2022, Ljubljana, Slovenia. 7 15TH WORKSHOP Abstract book & Fieldtrip guide. 15th Emile Argand Conference on Alpine Geological Studies, 12-14 September 2022, Ljubljana, Slovenia. Thick carbonate succession of the Julian Alps. From left to right: Mt. Planja (2453 m), Mt. Razor (2601) and Mt. Stenar (2501 m) (Author: Marko Vrabec) 8 15TH WORKSHOP Abstract book & Fieldtrip guide. 15th Emile Argand Conference on Alpine Geological Studies, 12-14 September 2022, Ljubljana, Slovenia. Abstract book 15TH Emile Argand Conference on Alpine Geological Studies 12-14 September 2022, Ljubljana, Slovenia 9 15TH WORKSHOP Abstract book. 15th Emile Argand Conference on Alpine Geological Studies, 12-14 September 2022, Ljubljana, Slovenia. 10 15TH WORKSHOP Abstract book. 15th Emile Argand Conference on Alpine Geological Studies, 12-14 September 2022, Ljubljana, Slovenia. Dating a long-lived lake in an intermontane basin: Late Miocene Lake Turiec in the Western Carpathians Kishan Aherwar1, Michal Šujan1, Rastislav Vojtko1, Régis Braucher2, Andrej Chyba3, Jozef Hók1, Barbara Rózsová1 and Aster Team2 1Department of Geology and Paleontology, Faculty of Natural Sciences, Comenius University in Bratislava, Slovakia (aherwar1@uniba.sk) 2CNRS-IRD-Collège de France-INRAE, CEREGE, Aix-Marseille University, Aix-en-Provence, France 3Institute of Chemistry, Slovak Academy of Sciences, Bratislava, Slovakia Lake Turiec existed from Late Middle Miocene to Pliocene in the the suitability of the Veľký Čepčín initial ratio is its rapid depo-heart of the Western Carpathians in the intermontane Turiec Ba- sition settings, preventing it from alteration by post-depositional sin. Despite the long-lasting lacustrine deposition, which formed processes and interaction with ground water, in contrary to the a muddy succession up to 900 m thick. The specific history of remaining intial ratio sites. Weighted mean depositional ages this basin in Western Carpathians has been a puzzle due to the calculated using N0 from Veľký Čepčín imply that the Lake missing geochronological proxies. Authigenic 10Be/9Be dating Turiec existed from ~9.96 Ma for more than ~3.25 Myr and method was applied to determine the existence duration and regression of the lake begun nearly ~6.71 Ma. regression of the long-lived Lake Turiec. Altogether 35 samples were collected from 11 different localities of the basin repre- Determining the precise timing of the lake existence has im-senting different sedimentary environments such as lacustrine, portant implications for geodynamic phases of the Western fan delta, alluvial fan and braided river. Four different localities, Carpathians, since it mirrors rapid increase of accommodation the Late Pleistocene alluvial fans Veľký Čepčín and Malý Čepčín, followed by intense increase of sediment supply during regres-and the Holocene river floodplains Košťany and Kalamová were sion. The presented application of authigenic 10Be/9Be yielded a considered for determining the initial ratio. The initial ratio first radiometric age of the long-living Lake Turiec as compared from the Veľký Čepčín alluvial fan was used for all other local- to roughly estimated ages described in previous studies of the ities representing lacustrine, fan delta, alluvial fan and braided Turiec Basin. This novel method also appeared as a promising river to determine ages, because it is the only N0 in agreement dating tool to determine the beginning of regression of the lake with the independent age proxies indicating that the lacustrine in an intermontane settings with complicated tectonic and sedi-deposits cannot be older than 11.6 Ma. Another explanation of mentary history. 11 15TH WORKSHOP Abstract book. 15th Emile Argand Conference on Alpine Geological Studies, 12-14 September 2022, Ljubljana, Slovenia. Multistage tectono-stratigraphic evolution of the Canavese Zone (Western Alps) Gianni Balestro1, Alessandro Borghi1, Sara De Caroli2, Eedoardo Barbero3 and Andrea Festa1,3 1Earth Sciences Department, University of Torino, Torino, Italy (gianni.balestro@unito.it) 2School of Earth and Environmental Sciences, Cardiff University, Cardiff, Wales, UK 3Institute of Geosciences and Earth Resources, National Research Council of Italy, Torino, Italy The Canavese Zone (CZ) in the Western Alps represents the of both mafic to acidic composition. The Late-Carboniferous to remnant of the distal passive margin of the Adria microplate, Cretaceous sedimentary succession starts with continental flu-which was stretched and thinned up to mantle rocks exhuma- vial deposits (Upper Carboniferous Basal Conglomerate Auct. ) tion during the Jurassic opening of the Alpine Tethys. Through unconformably overlain by Permian volcanic and volcanoclastic detailed geological mapping, structural analysis, stratigraphic rocks (Collio Formation), and it continues upward with Upper and petrographic observations, and documentation of rela- Permian to Lower Triassic conglomerates and sandstones (Ver-tionships between tectonics and sedimentation, we redefine rucano Auct. and Servino Formation), which are followed by the multistage tectono-stratigraphic evolution of the CZ, pre-rift Middle Triassic dolostone. The latter is overlain by Low-which consists of a Variscan basement, post-Variscan magmatic er to Middle Jurassic synrift sediments (Muriaglio Formation) bodies and a Late-Carboniferous to Cretaceous sedimentary and by Middle Jurassic to Early Cretaceous post-rift sediments, succession (Festa et al., 2020, and references therein). The consisting of Radiolarites, Maiolica micritic limestones and Variscan basement includes a Lower Unit, wherein micaschist Palombini shale. We point out that (i) the whole CZ succession, and orthogneiss were metamorphosed under amphibolite-fa- since the Late Carboniferous, shows significant thickness and cies conditions and partly transformed into migmatitic gneiss facies variations, documenting long-lived tectonic control on during a post-Variscan high-temperature metamorphic event, sedimentation, and (ii) Late Paleozoic – Triassic structural in-and an Upper Unit, consisting of a metasedimentary succession heritances playing a significant role in the localization of faults metamorphosed under greenschist- to amphibolite-facies con- that accommodated both the Jurassic rifting of the Alpine ditions during the Variscan orogeny. The two basement units Tethys and the subsequent convergent tectonics. were intruded by post-Variscan plutons and hypabyssal dykes Festa, A., Balestro, G., Borghi, A., De Caroli, S. & Succo, A. (2020). The role of structural inheritance in continental break-up and exhumation of Alpine Tethyan mantle (Canavese Zone, Western Alps). Geosciences Frontiers, 11, 167–188. 12 15TH WORKSHOP Abstract book. 15th Emile Argand Conference on Alpine Geological Studies, 12-14 September 2022, Ljubljana, Slovenia. The inversion of a passive continental margin portrayed by a 2D balanced kinematic forward model across the Velebit Mt. in the northern external Dinarides fold and thrust belt Philipp Balling1, Bruno Tomljenović2, and Kamil Ustaszewski1 1Friedrich-Schiller-Universität Jena, Jena, Germany (philipp.balling@uni-jena.de) 2University of Zagreb, Zagreb, Croatia The Dinarides fold and thrust belt resulted from the collision a pre-deformed lithostratigraphic template scaled to reported of the Adriatic Microplate with Eurasia and shows an overall stratigraphic thicknesses enabled us to test various geometries SW-vergent and in-sequence structural architecture. In the and temporal successions of fault activity not only for the Mid Paleocene the ophiolite-bearing internal Dinarides were Eocene – Oligocene contraction, but also for the Mesozoic exclusively affected by crustal shortening. The outward SW passive margin extension. Through an iterative trial-and-error propagation of the deformation front reached the eastern Adri- method, we were able to reproduce the present-day deformed atic passive continental margin mainly composed of Mesozoic reference section across the Velebit Mt. and the Lika Plateau in carbonate platform rocks in Mid-Eocene times. This led to high its northeastern hinterland. crustal Mid Eocene to Oligocene shortening and the formation of the external Dinarides. Two balanced crosssections across Our best-fit balanced kinematic model suggests that the reacti-the external Dinarides show an along-strike contrasting defor- vation of Middle Triassic and Upper Jurassic basement-rooted mation style observed in two orogenic segments separated by half grabens played a key role in the initiation of the back-the 250 km long dextrally transpressive Split-Karlovac Fault: the thrusts. These half grabens were mainly reactivated by hanging southern segment dominated by SW-vergent forethrusts, and the wall shortcuts. This inversion of normal faults led to predeter-northern segment dominated by NE-vergent backthrusts, located mination of the thin-skinned NE-vergent back thrusts, forming to the SE and NW from the Split-Karlovac Fault, respectively. So the upper part of a complex 68 km wide triangle structure. The far, it is not known why the regionally rather uniform Mesozoic structurally lower part comprised of a SW-vergent antiformal Adriatic carbonate platform sequence had undergone such con- stack involving Paleozoic basement. We assessed a crustal trasting along-strike deformation. To improve the understanding shortening for the triangle structure of 47 km and a shortening of the initiation of the NE-vergent backthrusts and to assess the of 98 km for the entire cross-section. Our results show that the amount of crustal shortening in the NW segment, a 2D kinemat- differences in both the lithostratigraphic and Mesozoic half ic forward model across the central Velebit Mt. was set up. The grabens along the eastern Adriatic passive margin played a Velebit Mt. extends for about 130 km along the eastern Adriatic crucial role in the Mid Eocene – Oligocene deformation of the coast and form a SW-dipping monocline with topographic ele- external part of the Dinarides fold and thrust belt, which led to vations reaching close to 1800 m. This faultrelated monocline the contrasting along strike deformation styles to the NW and is formed in the hanging wall of a NE-vergent backthrust SE of the Split-Karlovac Fault. system. The 2D kinematic forward model approach applied to 13 15TH WORKSHOP Abstract book. 15th Emile Argand Conference on Alpine Geological Studies, 12-14 September 2022, Ljubljana, Slovenia. Two types of peridotites in the area of Banovina, Croatia and their Petrogenesis Šime Bilić1, Vesnica Garašić1, and Alan B. Woodland2 1University of Zagreb, Faculty of Mining, Geology and Petroleum Engineering, Croatia (sbilic@rgn.hr) 2Goethe-Universität Frankfurt, Institute for Geosciences petrology and geochemistry Numerous outcrops of ultramafic rocks consisting mostly of a significantly higher Cr# (12.7 – 50.7) then those from the peridotites occur in the area of Banovina, in Croatia. These S-belt spinel lherzolites (7.7 – 10.8). Two types of dunites, rocks were formed as parts of the former Earth’s mantle and which were found only within S-belt peridotites, have very belong to the Central Dinaride Ophiolite Belt (CDOB), which different petrographic and chemical characteristics. Pyroxene is direct proof of the existence and closure of the Neothetys rich dunite is characterized by a coarse-grained protogran-ocean in the northern part of the Balkan area. Previous studies ular to porphyroclastic texture, high modal pyroxenes (up to have considered these peridotites as fertile, subcontinental 10 vol. %) and spinels enriched in MgO, Al O and NiO. The 2 3 parts of the mantle with complex chemistry. This research second type of dunite has smallgrained equigranular texture, presents a more detailed petrographic and chemical analysis, contains amphibole (up to 1 vol. %), pyroxene (< 1 vol. %) with the intention to sort between different types of Banovina and spinels enriched in Cr O and FeO . Geochemical analysis 2 3 T peridotites and offer the model for their petrogenesis. of all peridotites indicate that the S-belt peridotites represent a subcontinental mantle which have been formed through the Detailed field work, mapping and petrographic analyses have initial rifting phase during which they ascended to the upper revealed that Banovina peridotites occur as two texturally, crust. Peridotites from the S-belt are classified as orogenic per-lithologicaly and mineralogicaly different types, that crop out idotites. The geochemical characteristics of N-belt peridotites in two geographically different belts, the northern (N-belt) and indicate their origin from a suboceanic mantle formed within the southern (S-belt). The N-belt contains mostly serpentinite mid ocean ridge environment and are classified as ophiolitic breccias and serpentinized, depleted and mostly porphyroclas- peridotites. Dunites show different geochemical characteristics tic spinel lherzolites that occur in the form of mélange, while and may have been formed by different geological processes. S-belt comprises larger masses of peridotites which consist The diverse lithology of ultramafics in the limited space of the predominantly of fertile spinel lherzolites with equigranular to S-belt indicates very heterogeneous nature of the subcontinen-porphyroclastic textures. Bulk rock analyses have shown that tal mantle. As a part of the CDOBs, peridotites from Banovina spinel lherzolites from the S-belt have lower Cr# and Mg# indicate that the CDOB record three different phases of ocean and higher content of Al O , CaO, Na O, TiO and REE than evolution, the early phase of the initial rift and opening of the 2 3 2 2 spinel lherzolites from N-belt, and same relations, excluding ocean (S-belt peridotites), later phase of the already developed the REE, can be seen in the chemistry of clinopyroxenes and ocean (N-belt peridotites) and also the phase of ocean closure orthopyroxenes. Spinels from the N-belt spinel lherzolites have which is evident from the mélange occurrences. 14 15TH WORKSHOP Abstract book. 15th Emile Argand Conference on Alpine Geological Studies, 12-14 September 2022, Ljubljana, Slovenia. Barometric studies on different rock types from the Adula Nappe (Central Alps) by Raman spectroscopy of quartz inclusions in Garnet Olga Brunsmann1, Marisa Germer1, Alexandra Pohl1, Victoria Kohn1,2, Vincent Könemann1, Xin Zhong1, Jan Pleuger1 and Timm John1 1Freie Universität Berlin, Institut für Geologische Wissenschaften, Berlin, Germany (jan.pleuger@fu-berlin.de) 2Department of Lithospheric Research, Vienna University, Josef-Holaubek-Platz 2, 1090 Wien The Adula nappe in the Swiss-Italian Central Alps is a conti- minimum peak pressures. The advantages of this method are nental basement nappe from the former European margin that its independence of a chemical equilibrium and the ability to was subducted to depths indicating (ultra)-high-pressure con- yield reliable pressure constraints even if the high-pressure ditions. Many studies were performed to understand the pres- mineral assemblage has been retrogressed. The Variscan and sure-temperature-time evolution of the Adula nappe. However, Alpine garnet domains were carefully identified using the Elec-the pressure data derived from classical thermobarometry from tron Microprobe (EMP) and the Scanning Electron Microscopy eclogite and garnet peridotite lenses cannot be correlated with (SEM). Temperatures were determined by means of Zr-in-rutile the tectonic record without several difficulties. The pressure thermometry by measuring the Zr content with EMP. gradient is very high, the structural record for the often sug- gested extrusion model is missing and the directly surrounding As a result, the obtained temperatures exhibit a gradient nappes show consistently lower pressures. Furthermore, it was increasing from the north at ca. 500-550 °C to the south at discovered that at least parts of the Adula nappe underwent around 700 °C. The minimum peak pressures in the northern eclogite-facies metamorphism during the Variscan and the and central Adula nappe range between 2.09 GPa and 2.17 GPa Alpine orogenic cycles. These two cycles were distinguished for metasediments and 1.41 GPa and 2.02 GPa for metabasites. by age dating and the chemical zonation patterns of garnet, 1.53 GPa were determined for an orthogneiss from the central part although in some cases it can be ambiguous. Otherwise, the of the nappe. Lower pressures between 1.14 GPa and 1.31 GPa in Variscan and Alpine parageneses are hardly, if at all, possible the southern Adula nappe were potentially caused by viscous to tell apart. Therefore, existing pressure and temperature relaxation of the quartz inclusions during the high-temperature data that were obtained using classical geobarometers rely on Lepontine metamorphism. Our new pressure data imply a very mineral equilibria, which may not have yielded true Alpine weak pressure gradient. Therefore, it is in contrast to the results metamorphic conditions. For this study, around fifty felsic and of previous works, in which barometers based on a chemical metabasic samples were collected from different lithologies on equilibrium were applied. Additionally, no systematic difference a N-S transect through the Adula nappe parallel to the direc- in minimum peak pressures is observable for the different lithol-tion of subduction. Raman spectroscopy on quartz inclusions ogies. (RSQI) in garnet was used as a geobarometer to measure 15 15TH WORKSHOP Abstract book. 15th Emile Argand Conference on Alpine Geological Studies, 12-14 September 2022, Ljubljana, Slovenia. The arc of the western Alps: a review and new kinematic model Quentin Brunsmann1, Claudio Rosenberg1, Nicolas Bellahsen1 and Giancarlo Molli2 1Sorbonne Université, Paris, ISTeP, Paris, France (claudio.rosenberg@upmc.fr) 2Università di Pisa, Italy The arc of the western Alps forms the western termination of External Zone is abrupt, taking place along the Var Valley. No the Alpine Chain. The E-W striking Austro-Italian-German and progressive rotations of structures are observed there, instead Swiss Alps turn into a N-S direction along the western margin N-S striking folds and thrusts appear to be interrupted by the of the Po plain, finally rotating back to an E-W strike along the E-W striking ones which continue all along the southern coast Italian-French Mediterranean coast. The origin of this enigmat- of France until the Pyrenees. In several localities, stratigraphic ic shape was originally attributed to a variscan inheritance (Ar- and structural evidences show that these E-W structures were gand, 1916), but the vast majority of the present-day literature initiated before the onset of Alpine collision, and amplified suggests that it results from the indentation of Adria during during Alpine collision. collision, as a result of a significant W-directed component of convergence. We briefly review previous interpretations and Our field-based structural data and compiled ones point to suggest a new kinematic model based on retrodeformation the occurrence of a large-scale widely distributed system of of syncollisional shortening, on paleomagnetic results, on sinistral shear zones, striking ENE-WSW, which affect the area structural analysis of maps on the arc-scale, and on field-based north of the Argentera Massif including part of the Internal structural investigations. Zone. Such structure was often assumed to be the prime site accommodating the west-directed indentation of Adria. In spite Retrodeformation of syn-collisional shortening around the of its significant extent, its newly mapped location within the arc of the Western Alps points to the existence of an arc of Arc precludes such such a 1st order kinematic role of this significant amplitude before the onset of collision. Paleomag- structure during collision. netic results from the External Zone (Dauphinois) suggest that most rotations around vertical axes only affect the Mesozoic To conclude, we suggest that the arc of the Internal Zone (Pen-cover above the Triassic, hence they do not provide an infor- ninic Units) showing a progressive rotation of structures is not mation on the kinematic of the entire crust. In the area of the similarly observed in the External Zone, and we infer that this Argentera Massif, where paleomagnetic data were derived progressive, continuous curvature largely existed or formed from Permian beds, hence allowing to interpret rotations during subduction. The arc of the western Alps as observed in of the entire crustal block, it is shown that no significant ro- the External Zone mainly reflects the existence of such a structations around vertical axes affected the area during Alpine ture at the end of subduction and the transition between the orogeny. Structural analyses of maps indicate that the transi- Alps s.s. and the Pyrenean Chain, reactivated during Miocene tion between the N-S and E-W striking parts of the arc in the time. Argand, E., (1916). “Sur l’arc des Alpes Occidentales”. Eclogae geologicae Helvetiae, 14, 145-192. 16 15TH WORKSHOP Abstract book. 15th Emile Argand Conference on Alpine Geological Studies, 12-14 September 2022, Ljubljana, Slovenia. Hf isotopic constraints for Austroalpine basement evolution of Eastern Alps: review and new data Ruihong Chang1, Franz Neubauer1, Johann Genser1, Yongjiang Liu2,3, Sihua Yuan4, Qingbin Guan2 and Qianwen Huang2 1University of Salzburg, Geography and Geology, Salzburg, Austria (ruihong.chang@stud.sbg.ac.at) 2Ocean University of China, Frontiers Science Center for Deep Ocean Multispheres and Earth System, Key Lab of Submarine Geoscience and Prospecting Techniques, College of Marine Geosciences, China 3Ocean University of China, Laboratory for Marine Mineral Resources, Qingdao National Laboratory for Marine Science and Technology, China 4Institute of Disaster Prevention, College of Earth Science, Hebei Province, China The Alps, as part of the Alpine-Mediterranean Mountain chain, al material during 490–470 Ma period and bears considerably are one of the classical localities for orogenic studies, where more positive εHf(t) values than the underlying Wechsel Gneiss the Mesozoic-Cenozoic tectonic evolution is well known. Many Complex and gives relatively young, depleted mantle model classical models have been proposed to explain the tectonic evo- ages of 700 to 500 Ma. The Waldbach Complex is, therefore, lution from Mesozoic rifting and breakup to Late Mesozoic-Ce- interpreted to be part of a magmatic arc that formed during clo-nozoic subduction, plate collision and exhumation. However, sure of the Prototethys and was metamorphosed during Variscan the pre-Mesozoic tectonic evolution of the pre-Alpine basement orogenic events at ca. 350–330 Ma. The Schladming-Seckau remains poorly known because of the lack of sufficient age data and Wechsel Complexes represent a Cambro-Ordovician mag-due to complex polyphase deformation and multiple metamor- matic arc system formed by Prototethys subduction processes phic overprints. New data from mainly amphibolite-facies pre-Al- with the associated Late Neoproterozoic to Early Ordovician pine basement of the Austroalpine mega-unit indicates that this ophiolitic Speik complex having formed in its back-arc basin or basement is composed of a heterogeneous series of continental as Prototethyan lithosphere. The Plankogel Complex and struc-units, island arcs, ophiolites, subduction mélanges, accretion- turally overlying micaschist and amphibolite units represent ary wedges, and seamounts affected by different metamorphic accreted ocean, ocean island, and continent-derived materials, grades. This study presents new results of LA-ICP-MS U-Pb interpreted to be an accretionary complex formed during the zircon dating and MC-ICP-MS Lu-Hf isotopic tracing of zircons Permo-Triassic closure of the Paleotethys. Many granites with from three key areas of Austroalpine basement, including the: i) Permian ages (e.g., porphyric granite called Grobgneiss and Wechsel Gneiss and Waldbach Complexes, and Wechsel Phyllite other granite gneisses and associated pegmatites) were likely Unit, (ii) Saualpe-Koralpe-Pohorje, and (iii) Schladming areas. formed in an extensional environment that culminated in the We determine the Wechsel Gneiss Complex to be a continental opening of the Middle-Late Triassic Meliata oceanic rift. These magmatic arc formed during 500–560 Ma in the proximity to granites formed by partial remelting of crust with mainly Mid-a continental block with a ‘memory’ of Late Archean to Early dle Proterozoic Hf model ages. Taken all these data together, Proterozoic continental crust. The Wechsel Gneiss Complex has we find that the Austroalpine basement is heterogeneously Hf model ages of 2.1 to 2.2 Ga and 2.5 to 2.8 Ga that indicate composed and includes complexes of different ages, different a close relationship to northern Gondwana, with depleted man- tectonic evolutionary histories and different remolten sources tle Hf model ages as old as 3.5 Ga. The Wechsel Phyllite Unit representing different locations before final accretion. The structurally overlying the Wechsel Gneiss Complex has partly composite of pre-Alpine complexes in the Austroalpine me-different sources, including juvenile crust formed at ca. 530 Ma. ga-unit likely assembled not earlier than Late Permian or Early In contrast, the Waldbach Complex constantly added new crust- Triassic. 17 15TH WORKSHOP Abstract book. 15th Emile Argand Conference on Alpine Geological Studies, 12-14 September 2022, Ljubljana, Slovenia. Multiscale lithological and structural heterogeneity control on the nucleation of a crustal shear zone: petro-structural investigation and U-Pb titanite dating from the Anzola shear zone (Ivrea-Verbano Zone, Southern Alps) Stefania Corvò1,2, Matteo Maino1,2, Sandra Piazolo3, Andrew Kylander-Clark4, Silvio Seno1 and Antonio Langone2 1University of Pavia, Department of Earth and Environment, Pavia, Italy (stefania.corvo01@universitadipavia.it) 2Institute of Geosciences and Earth Resources of Pavia, C.N.R., Pavia, Italy 3School of Earth and Environment, University of Leeds, Leeds, United Kingdom 4Department of Earth Science, University of California, Santa Barbara, United States The Ivrea-Verbano Zone (IVZ, Southern Alps) is a fossil ex- mylonitic rocks developed at the expense of a multi-lithological humed passive margin section of the pre- Alpine middle to sequence showing amphibolite to granulite facies metamorphic lower continental crust that escaped Alpine subduction. Fol- conditions and deformation features related to preshearing lowing the Variscan orogeny, the IVZ was affected by Permian event. Estimated P-T conditions by geothermobarometry indi-post-orogenic extension and Triassic-Jurassic polyphasic rifting cate that mylonitic deformation started at high temperature stages. Rift-related deformation was accommodated by several (~820 °C) with presence of melt and continued as solid-state km-scale shear zones active at different crustal levels (e.g., Bel- deformation down to amphibolite facies (~650 °C). As regard trando et al., 2015). Due to the intrinsic importance of these the timing, we show preliminary petrochronological results tectonic structures, a detailed characterization of their compo- from titanite of the mylonitic amphibolites that recorded resitional, metamorphic and structural patterns, as well as the crystallization event under amphibolite facies at about 185 Ma, timing of activity may provide key information for the models which is coeval to deformation occurred at different crustal of shear development in relation to the evolution of the region- levels in the IVZ (Simonetti et al., 2021). On the basis of our al tectonics. In this contribution, we investigate one of these findings, we argue that the shear zone development was pro-major extensional structures - the Anzola shear zone - with the moted by the rheological contrasts derived from the inherited aim to assess the conditions that promoted the strain locali- compositional and structural patterns. Moreover, we emphasation. We also provide Upb dating on titanite as an attempt size evidence of syn-deformational partial melting and small to constrain the timing of the high-temperature crystal-plastic amounts of free fluids localized in certain layers that enhance deformation occurring within the shear zone. Recent field and the viscosity contrasts within the multi-lithological complex. meso-structural investigations revealed that the Anzola shear Melts/fluids played a key role in both weakening mechanisms zone overprinted basement rocks characterized by inherited controlling the strain localization, as well as the syn-tectonic lithological and structural heterogeneities (Corvò et al., 2022). growth-recrystallization processes of the titanite, resulting in Gabbroic rocks and migmatites define the hanging wall and a strong influence of the U-Pb petrochronology results. Finally, footwall, respectively. According to a detailed petrographical our results are discussed in the framework of the geodynamic and geochemical characterization (EPMA, LA-ICP-MS), (ultra-) evolution of IVZ. Beltrando, M., Stockli, D.F., Decarlis, A., Manatschal, G. (2015). A crustal-scale view at rift localization along the fossil Adriatic margin of the Alpine Tethys preserved in NW Italy. Tectonics, 34, 1927–1951. Corvò, S., Maino, M., Piazolo, S., Seno, S., & Langone, A. (2022). Role of inherited compositional and structural heterogeneity in shear zone development at mid-low levels of the continental crust (the Anzola shear zone; Ivrea-Verbano Zone, Southern Alps). Lithos, article 106745. Simonetti, M., Langone, A., Corvò, S., Bonazzi, M. (2021). Triassic-Jurassic rift-related deformation and temperature- time evolution of the fossil Adriatic margin: A review from Ossola and Strona di Omegna valleys (Ivrea-Verbano Zone). Ofioliti, 46(2), 147-161. 18 15TH WORKSHOP Abstract book. 15th Emile Argand Conference on Alpine Geological Studies, 12-14 September 2022, Ljubljana, Slovenia. Migration of basin formation and contrasting deformation style in the south-western Pannonian Basin (central Europe) László Fodor1,2, Attila Balázs3, Gábor Csillag2,4, István Dunkl5, Gábor Héja6, Péter Kelemen5,7, Szilvia Kövér1,2, András Németh8, Anita Nyerges1, Dániel Nyíri8,1, Éva Oravecz1,2,3, Ildikó Selmeczi6, Balázs Soós8, Lilla Tőkés1, Marko Vrabec9 and Csilla Zadravecz8 1Eötvös Loránd University, Institute of Geography and Earth Sciences, Department of Geology, Budapest, Hungary (lasz.fodor@yahoo.com) 2MTA-ELTE Geological, Geophysical and Space Research Group at Eötvös University 3ETH Zürich, Department of Earth Sciences, Zürich, Switzerland 4Institute for Geological and Geochemical Research, Research Centre for Astronomy and Earth Sciences, Budapest, Hungary 5Geoscience Center, University of Göttingen, Germany 6Supervisory Authority of Regulatory Affairs, Budapest, Hungary 7Department of Petrology and Geochemistry, Institute of Geography and Earth Sciences, Eötvös University, Budapest, Hungary 8MOL Ltd. 1117 Budapest, Hungary 9Department of Geology, University of Ljubljana, Slovenia The Pannonian Basin is a continental extensional basin north-eastward and reached the TR where fault-controlled system with various depocentres within the Alpine–Carpath- basin subsidence lasted until ~8 Ma. 3D thermo-mechanical ian–Dinaridic orogenic belt. Along the western basin margin, forward models analyze this depocenter migration and predict exhumation along the Rechnitz, Pohorje, Kozjak, and Baján the subsidence and heat flow evolution that fits observational detachments resulted in the cooling of variable units of the Al- data. These models consider fast lithospheric thinning, mantle pine nappe stack. This process is constrained by thermochrono- melting, lower crustal viscous flow, and upper crustal brittle logical data between ~25–23 to ~15 Ma (Fodor et al., 2021). deformation. Models suggest ~150–200 km of shift in dep-Rapid subsidence in supradetachment sub-basins indicates the ocenters during ~12 Myr. onset of sedimentation in the late Early Miocene from ~19 or 17.2 Ma. In addition to extensional structures, strike-slip faults Simultaneously with depocenter migration, the southern part mostly accommodated differential extension; branches of the of the former rift system, near or within the MHZ, underwent Mid-Hungarian Shear Zone (MHZ) could also play the role of ~N–S shortening; the early syn-rift basin fill was folded and transfer faults. their boundary faults were inverted. Deformation was dated to ~15–14 Ma („middle” Badenian) and continued locally to During this period, the distal margin of the hanging wall ~9.7 Ma while north of the MHZ the TR was still affected by tilted block of the detachment system, i.e., the pre-Miocene modest extensional faulting. The particularity of this short-rocks of the Transdanubian Range (TR) experienced surface ening is that it happened during the post-rift thermal cooling exposure, karstification, and terrestrial sedimentation. After stage. The low-rate contraction and related uplift rarely ex- ~14.5 Ma faulting, subsidence, and basin formation shifted ceeded this regional thermal subsidence. Acknowledgements: MOL Ltd. largely supported the research. The research is supported by the scientific grant NKFI OTKA 134873 and the Slovenian Research Agency (No. P1-0195). Fodor, L., Balázs, A., Csillag, G., Dunkl, I., Héja, G., Jelen, B., Kelemen, P., Kövér, Sz., Németh, A., Nyíri, D., Selmeczi, I., Trajanova, M., Vrabec, M., Vrabec, M. (2021). Crustal exhumation and depocenter migration from the Alpine orogenic margin towards the Pannonian extensional back-arc basin controlled by inheritence. Global and Planetary Change, 201, article 103475. 31p. https://doi.org/10.1016/j.gloplacha.2021.103475 19 15TH WORKSHOP Abstract book. 15th Emile Argand Conference on Alpine Geological Studies, 12-14 September 2022, Ljubljana, Slovenia. Middle-Late Jurassic ophiolite obduction and formation of sedimentary mélanges in the Western Tethys Realm Hans-Jürgen Gawlick Montanuniversitaet Leoben, Department Applied Geoscience and Geophysics, Leoben, Austria (gawlick@unileoben.ac.at) Component analyses of ancient Neo-Tethys mélanges along the with the Hallstatt mélanges were established, expressed by Eastern Mediterranean mountain ranges allow both, a facies the formation of the up to 900 m thick basin fills comprising reconstruction of the Middle Triassic to Middle Jurassic outer its material mainly from the outer shelf region. In Callovian to passive margin of the Neo-Tethys and conclusions on the pro- Middle Oxfordian times the nappe stack reached the former cesses and timing of the Jurassic orogenesis. This Middle-Late carbonate-platform-influenced outer shelf region and the reef Jurassic mountain building process in the Western Tethyan rim. Newly formed basins received material from this shelf realm was triggered by west- to northwestward-directed ophi- region, occasionally mixed with material from the approaching olite obduction onto the former passive continental margin ophiolite nappes. Ongoing shortening led to the formation of (wider Adria) of the Neo-Tethys. the proximal Hallstatt nappes with concomitant mobilisation of Hallstatt Mélanges. Persistent tectonic convergence caused the Ophiolite obduction onto the former passive continental partial detachment and northwest- to west-directed transport margin started in the Bajocian and trench-like deep-water of the older basin groups and nappes originally formed in a basins formed in sequence within the northwest-/westward more oceanward position onto the foreland. propagating nappe fronts in the footwall of the obducting ophi- olites, i.e. in lower plate position. Deposition in these basins Comparison of mélanges identical in age and component was characterized by coarsening-upward cycles, i.e. forming spectrum in different mountain belts (Eastern Alps/Western sedimentary mélanges as synorogenic sediments, in cases tec- Carpathians/Dinarides/Albanides/Pelso) suggest one Neo-tonically overprinted. In the Middle Jurassic, the oceanic realm Tethys Ocean in the Western Tethyan realm, instead of multi-and the most distal parts of the former passive margin were ocean and multi-continent scenarios. The evolution of several incorporated into the nappe stacking. Bajocian-Callovian ophi- independent Triassic-Jurassic oceans is unlikely considering the olitic and Meliata mélanges were formed as most oceanward fact that re-sedimentation into newly formed trench-like basins preserved relics of trench-like basins in front of the propagat- in front of a west- to northwestward propagating nappe stack ing ophiolitic nappe stack, often with incorporated components including ophiolite obduction is nearly contemporaneous along from the continental slope (Meliata facies zone). In the course the Neotethyan Belt. The Middle to Late Jurassic basin evolu-of ongoing ophiolite obduction, thrusting progressed to the tions with their sedimentary cycles and component spectra are outer shelf region (Hallstatt Limestone facies zone). In Batho- comparable everywhere. nian/Callovian to Early Oxfordian times the Hallstatt nappes 20 15TH WORKSHOP Abstract book. 15th Emile Argand Conference on Alpine Geological Studies, 12-14 September 2022, Ljubljana, Slovenia. Upper Campanian bentonites of volcaniclastic origin in the Scaglia-type limestones of the Adria continental margin David Gerčar1, Nina Zupančič1,2, Anna Waśkowska3, Jernej Pavšič1 and Boštjan Rožič1 1Department of Geology, Faculty of Natural Sciences and Engineering, University of Ljubljana, Aškerčeva 12, Ljubljana, SI-1000, Slovenia (david.gercar@ntf.uni-lj.si) 2Ivan Rakovec Institute of Paleontology, ZRC SAZU, Novi trg 2, Ljubljana, SI-1000, Slovenia 3Faculty of Geology, Geophysics and Environmental Protection, AGH University of Science and Technology, Mickiewicza 30, Kraków, 30-059, Poland Upper Campanian Scaglia-type limestones in the transition marine environment of the Slovenian Basin. The limestones zone between the Internal and External Dinarides (Placer, are composed of (hemi)pelagic mudstones to wackestones and 2008) contain two layers of bentonitic clays. The first 110 cm thin- to medium-grained calcarenites, originating from the ad-thick, and the second 10 cm thick. The geochemical composi- jacent Adriatic Carbonate Platform. Similar Upper Cretaceous tion and characteristics of the bentonites, such as correlation successions containing Campanian bentonitic clay horizons coefficients and scatterplots of immobile trace elements, in- have been described in the Central Apennines (Graziano and dicate a rhyolitic volcanic source within an active continental Adabbo, 1996; Bernoulli et al., 2004). The most likely source margin. According to the mineralogy of the clay, which con- of these volcanoclastics is the bimodal rhyolitic/basaltic mag-tains smectite, calcite, quartz and muscovite/illite, the layers matic activity within the Sava suture zone, located in the pres-can be interpreted as a deposit of volcanic-ash in a marine ent day Dinarides (Ustaszewski et al., 2009; Cvetković et al., sedimentary environment with admixture of carbonates. The 2014; Prelević et al., 2017; Schmid et al., 2020). encompassing carbonate succession was deposited in a deeper Bernoulli, D., Schaltegger, U., Stern, W. B., Frey†, M., Caron, M., & Monechi, S. (2004). Volcanic ash layers in the Upper Cretaceous of the Central Apennines and a numerical age for the early Campanian. International Journal of Earth Sciences, 93(3), 384–399. https://doi.org/10.1007/ s00531-004-0389-4 Cvetković, V., Šarić, K., Grubić, A., Cvijić, R., & Milošević, A. (2014). The Upper Cretaceous ophiolite of North Kozara–remnants of an anomalous mid-ocean ridge segment of the Neotethys? Geologica Carpathica, 65(2), 117–130. Graziano, R., & Adabbo, M. R. (1996). Segnalazione di un livello cineritico nella serie di scarpata senoniana del Gargano meridionale. Bollettino della Societa Geologica Italiana, 115(2), 459–466. Placer, L. (2008). Principles of the tectonic subdivision of Slovenia. Geologija Revija, 51(2), 205–217. Prelević, D., Wehrheim, S., Reutter, M., Romer, R. L., Boev, B., Božović, M., et al. (2017). The Late Cretaceous Klepa basalts in Macedonia (FY-ROM)—Constraints on the final stage of Tethys closure in the Balkans. Terra Nova, 29(3), 145–153. Schmid, S. M., Fügenschuh, B., Kounov, A., Maţenco, L., Nievergelt, P., Oberhänsli, R., et al. (2020). Tectonic units of the Alpine collision zone between Eastern Alps and western Turkey. Gondwana Research, 78, 308–374. https://doi.org/10.1016/j.gr.2019.07.005 Ustaszewski, K., Schmid, S. M., Lugović, B., Schuster, R., Schaltegger, U., Bernoulli, D., et al. (2009). Late Cretaceous intra-oceanic magmatism in the internal Dinarides (northern Bosnia and Herzegovina): Implications for the collision of the Adriatic and European plates. Lithos, 108(1), 106–125. https://doi.org/10.1016/j.lithos.2008.09.010 21 15TH WORKSHOP Abstract book. 15th Emile Argand Conference on Alpine Geological Studies, 12-14 September 2022, Ljubljana, Slovenia. First evidence of UHP in the Lago Superiore Unit (Monviso, Western Alps) Stefano Ghignone1, Emanuele Scaramuzzo2, Mattia Gilio3, Marco Bruno1, Franz Livio2, and Matteo Alvaro3 1Università degli studi di Torino, Earth Science, TORINO, Italy (s.ghignone@unito.it) 2Department of Science and High Technology, University of Insubria, via Valleggio 11, 22100 Como, Italy 3Department of Earth and Environmental Sciences, via Ferrata, 4, University of Pavia, Pavia, Italy The first occurrence of ultra-high-pressure (UHP) metamor- towards higher wavenumbers. The main peak is located at phism in the Western Alps was documented by Chopin in 1984 522 cm–1, and the secondary peaks at 426, 270 and 178 cm–1. (Chopin, 1984) with the discovery of coesite in the southern Coesite inclusions consist of intact single crystals (10-60 μm) Dora Maira massif. Since then, just one additional UHP terrain hosted by garnet, without evidence for re-equilibration fea-was discovered until the end of the 90’s. In recent times, new tures. Typical coesite-related features such as radial cracks in occurrences of coesite have been reported in different units garnet host mineral and palisade texture are present in large of the Western Alpine belt, widening the distribution of UHP polycrystalline quartz inclusions (> 80 μm). Peak metamorphic terrains, with important tectonic implications. Here, we report conditions have been constrained through different techniques the first discovery of coesite in the meta-ophiolitic suite of the (detailed garnet inclusion analysis, elastic geobarometry and Monviso Massif, in the northern Lago Superiore Unit (LSU). thermodynamic modelling). The occurrence of UHP terrains Previous petrographic studies and thermodynamic modelling along the Western Alps is becoming more common than ex-in the area suggested that these alpine units may have expe- pected. Our results, alongside with the novel evidence for UHP rienced UHP metamorphism, but no direct evidences (i.e., in the Western Alps, will lead to new tectonic models for the coesite occurrence) have been reported to date. The presence subduction and exhumation of UHP terrains, constraining the of coesite is demonstrated by μ-Raman analyses. The Raman evolution of subductionaccretionary systems. spectra show the typical peaks of coesite, slightly shifted Chopin, C. (1984) Coesite and pure pyrope in high-grade blueschists of the western Alps: a first record and some consequences: Contributions to Mineralogy and Petrology, 86, 107–118. https://doi.org/10.1007/BF00381838 22 15TH WORKSHOP Abstract book. 15th Emile Argand Conference on Alpine Geological Studies, 12-14 September 2022, Ljubljana, Slovenia. The prograde history of three Mn-rich garnets from the UHP Lago di Cignana Unit (Italy) Mattia Gilio1, Hugo W. van Schrojenstein Lantman1,2, Alice Girani1,3, Ross J. Angel4, Marco Scambelluri5 and Matteo Alvaro1 1University of Pavia, Department of Earth and Environmental Sciences, Pavia, Italy (mattia.gilio@gmail.com) 2University of Oslo, Njord Centre, Department of Geosciences, Oslo, Norway 3ETH Zürich, Institute for Geochemistry and Petrology, Zürich, Switzerland 4IGG-CNR, Padova, Italy 5University of Genoa, Department of Earth, Environmental, and Life Sciences, Genoa, Italy Extensive rock recrystallization and element redistribution marble from the Lago di Cignana Unit (Italy). The rock consists during retrogression often hampers our understanding of the of mainly quartz and calcite with garnet porphyroblasts. The early stages of metamorphism. Garnet is the mineral that best three garnets show a very large core-to-rim compositional zon-preserves information about its growth during the prograde ing with Mn-rich cores, Fe-rich mantles, and rims with a slight history of the rock as compositional zoning. In most metamor- increase in Mg. Mineral inclusions in garnet cores and mantles phic rocks, garnet zoning varies between almandine, grossular, are mainly quartz, with minor titanite, calcite, and apatite. and pyrope endmembers with minor spessartine content. Coesite, aragonite, zircon, and rutile are instead present with-This variability and the diffuse presence of mineral inclusions in garnet rims. The three investigated garnets vary in shape, in garnet enables the coupling of thermodynamic tools (e.g., zonation, inclusions type and size while having a comparable pseudosections) with classical element exchange and elastic core-to-rim composition. In two garnets, quartz inclusions are geothermobarometry to gather information on their pressures tiny (20-30 μm) and spread evenly within the garnets. The and temperatures of equilibration. Such studies give their best third garnet has larger quartz inclusions (50-100 μm) in the results when applied to metapelites due to their relatively large core and smaller in the mantle, decreasing progressively in mineral variability over the typical PT range of metamorphic size from the inner to the outer mantle (50-10 μm). Elastic rocks. However, monomineralic lithotypes, such as impure geobarometry on these quartz inclusions in garnet allowed the quartzite or marble, consist of minerals stable over a wide PT tracking of the pressures at which garnet cores and mantles range and therefore lack mineralogic change. Furthermore, formed. We can show that these garnets formed during multiple currently available solution models are not calibrated for use distinct growth stages along the prograde path from 1.2 GPa and on unconventional bulk rock compositions and therefore do 430 °C to 1.8 GPa and 500 °C and finally at UHP conditions, not guarantee reliable geothermobarometric results. as testified by the coesitebearing garnet rims. This difference in pressure and temperature of garnet growth might be due to In this contribution, we use elastic geobarometry to track pro- local (cm-to-mm-sized) changes in chemical composition at the grade garnet growth from low- to ultrahigh-pressure conditions scale of the thin section and/or to reaction overstepping. in three Mn-rich garnets (up to 50 % sps) from an impure 23 15TH WORKSHOP Abstract book. 15th Emile Argand Conference on Alpine Geological Studies, 12-14 September 2022, Ljubljana, Slovenia. Episodes of open fissure formation in the Alps Edwin Gnos1, Josef Mullis2, Emmanuelle Ricchi3, Christian Bergemann4, Emilie Janots5, and Alfons Berger6 1Museum of Natural History of Geneva, Department of Mineralogy and Petrography, Geneva, Switzerland (edwin.gnos@ville-ge.ch) 2Department of Earth Sciences, University of Basel, Bernoullistrasse 32, 4056 Basel, Switzerland 3Department of Earth Sciences, University of Geneva, Rue de Maraîchers 13, 1205 Geneva 4Institute of Geosciences, Heidelberg University, Im Neuenheimer Feld 236, 69120 Heidelberg, Germany 5ISTerre, University of Grenoble Alpes, 38041 Grenoble, France 6Insitute of Geological Sciences, University of Bern, Baltzerstrasse 8+10, 3012 Bern, Switzerland Fluid assisted Alpine fissure-vein and cleft formation starts type of fluid constrains the morphology of the very frequently at prograde, peak or retrograde metamorphic conditions of crystallizing quartz crystals. Open fissures also form in asso-450–550 °C and 0.3–0.6 GPa and below. Early-formed fissures ciation with more localized strike-slip faults and are oriented become overprinted by subsequent deformation, locally leading perpendicular to the faults. The combination of fissure orien-to a reorientation. Deformation that follows fissure formation tation, fissure quartz fluid inclusion and fissure monazite-(Ce) initiates a cycle of dissolution, dissolution/reprecipitation (hereafter monazite) Th–Pb ages shows that fissure formation or new growth of fissure minerals enclosing fluid inclusions. occurred episodically (1) during the Cretaceous (eo-Alpine) Although fissures in upper greenschist and amphibolite facies deformation cycle in association with exhumation of the Aus-rocks predominantly form under retrograde metamorphic con- troalpine Koralpe-Saualpe region (~ 90 Ma) and subsequent ditions, this work confirms that the carbon dioxide fluid zone extensional movements in association with the formation of correlates with regions of highest grade Alpine metamorphism, the Gosau basins (~ 90–70 Ma), (2) during rapid exhumation suggesting carbon dioxide production by prograde devolatiliza- of high-pressure overprinted Briançonnais and Piemontais tion reactions and rock-buffering of the fissure-filling fluid. For units (36–30 Ma), (3) during unroofing of the Tauern and Lep-this reason, fluid composition zones systematically change in ontine metamorphic domes, during emplacement and thrusting metamorphosed and exhumed nappe stacks from diagenetic to of the external Massifs (25–12 Ma; except Argentera) and amphibolite facies metamorphic rocks from saline fluids dom- due to local dextral strike-slip faulting in association with the inated by higher hydrocarbons, methane, water and carbon opening of the Ligurian sea, and (4) during the development dioxide. Open fissures are in most cases oriented roughly per- of a young, widespread network of ductile to brittle strike-slip pendicular to the foliation and lineation of the host rock. The faults (12–5 Ma). 24 15TH WORKSHOP Abstract book. 15th Emile Argand Conference on Alpine Geological Studies, 12-14 September 2022, Ljubljana, Slovenia. Magnetic susceptibility and chemostratigraphy of the Jurassic/Cretaceous boundary interval – new data from the Slovenian Basin Jacek Grabowski1, Jolanta Iwańczuk1, Daniela Rehakova2, Boštjan Rožič3, Petra Žvab Rožič3, Andrzej Chmielewski1, Lucjia Slapnik3 and David Gerčar3 1THE POLISH GEOLOGICAL INSTITUTE - NATIONAL RESEARCH INSTITUTE, Warsaw, Poland (jacek.grabowski@pgi.gov.pl; jolanta.iwanczuk@pgi.gov.pl) 2Comenius University, Faculty of Natural Sciences, Department of Geology and Paleontology, Bratislava, Slovakia 3University of Ljubljana, Faculty of Natural Sciences and Engineering, Department of Geology, Ljubljana, Slovenia The pelagic succession from the Slovenian Basin (Petrovo Brdo Lithogenic input increases again at ca 30 m of the section. As in section) covers the lower Tithonian to upper Berriasian interval numerous Tethyan domains (e.g. Western Carpathians, Northern (ca. 40 m). At 5 m of the section a sharp transition is observed Calcareous Alps, Western Balkan) the increase of marly sedimen-between clay rich radiolarian cherts of Tolmin Fm. and calpio- tation starts in the lower part of the Calpionellopsis Zone (mag-nellid limestones of Biancone Limestone Fm. Calpionellid asso- netozone M16n), this level is tentatively interpreted as being ciations are not numerous and poorly preserved, therefore only close to the lower/upper Berriasian boundary. Relative variations rough biostratigraphic dating is possible. Crassicollaria Zone of K and Ti content (K/Ti, Ti/Al ratios) indicate enrichment of (upper Tithonian) was documented between 8 and 13 m of the K and depletion in Ti in the upper Tithonian/lower Berriasian section, while the beginning of the Calpionella alpina Subzone interval which accounts for decreased chemical weathering in (present day J/K boundary) is situated at ca. 20 m. Transition the provenance areas. Additionally, the interval is enriched in between Tolmin and Maiolica Fm. falls in the UAZ 12 radiolar- redox sensitive trace metals (Cu, Zn, Cd) and reveals decreased ian Zone which is close to the lower/upper Tithonian bound- δ 13C values, which accounts for bottom water stratification. ary. The section supplied high-resolution magnetic susceptibil- The overall palaeoenvironmental trends might be interpreted ity (MS), as well as chemostratigraphic data ( δ 13C, main and in favor of aridification trend throughout the late Tithonian trace elements), acquired with portable XRF device, gamma and early Berriasian and more humid episodes in the early ray spectrometer and verified with ICPMS laboratory measure- Tithonian and late Berriasian. The trends seems to correlate ments. Lithogenic elements (Al, K, Rb, Ti, Zr etc.) and MS show throughout the Western Tethys domain and might be related prominent decrease between Tolmin and Maiolica Fm., reaching with large-scale palaeoenvironmental perturbations. minimum values in the upper Tithonian and lower Berriasian. 25 15TH WORKSHOP Abstract book. 15th Emile Argand Conference on Alpine Geological Studies, 12-14 September 2022, Ljubljana, Slovenia. Project DIVE (Drilling the Ivrea-Verbano zonE): A joint petrological, geochemical, and geophysical exploration of the lower continental crust Andrew Greenwood1,2, György Hetényi1, Luca Ziberna3, Mattia Pistone4, Alberto Zanetti5, Othmar Müntener1 and Project DIVE Team6 1University of Lausanne, Switzerland (gyorgy.hetenyi@unil.ch) 2Montanuniversität Leoben, Austria (andrew.greenwood@unileoben.ac.at) 3University of Trieste, Italy 4University of Georgia, USA 5CNR, Italy & University of Pavia, Italy 6www.dive2ivrea.org Despite the structural complexity of the Alps at numerous tions, and additional surveys around each site. Taken together, scales, geological and geophysical investigations have respec- these should cover a large range of spatial scales covering at tively mapped and imaged tremendous amounts of information least 6 orders of magnitude (mm to km), investigate structures near the surface and at depth. However, there is an inherent and their variations in bulk properties within the lower crust, gap between the two sets of approaches, leaving the middle and the transition to mantle rocks in an unprecedented way. and lower crust poorly constrained. This has been one of the The interdisciplinary approach not only allows to correlate main motivations to initiate the ICDP project DIVE (Drilling numerous geophysical and petrological properties, but with the Ivrea-Verbano zonE), in which three geological sites of the modelling it will also allow to investigate the causative rela-Ivrea-Verbano Zone will be explored through scientific drilling. tionships. The detailed aims, preparatory steps, as well as In this zone, near-complete sections of the continental crust are the current status of project DIVE, will be presented at the exposed at the surface, and with careful geological preparation conference. By that time, drilling of the first hole is expected and geophysical site surveys we have targeted three areas with to start near Ornavasso, followed by a second hole in Megolo a great potential of further discoveries during DIVE. Almost all (both in Val d’Ossola). For the third site near Balmuccia, which physical and chemical properties will be characterized on the is planned for later, site survey results will be presented. recovered rock core samples, in borehole logging investiga- 26 15TH WORKSHOP Abstract book. 15th Emile Argand Conference on Alpine Geological Studies, 12-14 September 2022, Ljubljana, Slovenia. Remote sensing of active tectonics in NE Italy, eastern Southern Alps Christoph Grützner1, Mattis Grenier2, Jakob Stubenrauch1, Markus Hermann1, Klaus Reicherter3 and Kamil Ustaszewski1 1Institute for Geological Sciences, Friedrich Schiller University Jena, Jena, Germany (christoph.gruetzner@uni-jena.de) 2Department of Earth Sciences, University of Cambridge, Cambridge, UK 3Neotectonics and Natural Hazards Group, RWTH Aachen University, Aachen, Germany Due to the collision of the European and Adriatic plates, about value, terrain ruggedness index, and stream knickpoints. The 3 mm/yr of N-S convergence are accommodated in the Eastern results were checked with geological data, mapped faults, and and Southern Alps. This shortening is mainly taken up by c. seismicity. We also conducted extensive field work to verify E-W trending reverse faults along the South Alpine Front and the results on the ground. Our results show that the applica-on NW-SE-trending dextral strike-slip faults in western Slove- tion of large-scale tectonic geomorphology in this particular nia. Strong historical earthquakes and instrumental seismicity, Alpine region is complicated by numerous factors. Small-scale however, show that some deformation also occurs in the inte- variations in lithologies with variable erodibility strongly rior of the Southern Alps. Little is known about which faults influence the analysis. The same holds true for variations in are active here. In this study we present results from a region- dip direction and dip angles of bedding planes; occasionally, al-scale remote sensing analysis focusing on the Bellunese and vertical strata erroneously suggest linearly trending faults. In Friulian sectors of the Southern Alps in northeastern Italy. Our addition, we found that glacial features and alluvial deposits aim was to identify areas with relatively increased tectonic have locally overprinted the traces of known faults. Despite activity based on landscape features. We made use of high-res- of these challenges, we found hints for active deformation in olution digital elevation models from aerial laser scanning the landscape, in particular in the epicentral area of the 1976 campaigns. We downsampled the data to 5 m resolution and Friuli earthquakes. We highlight potential pitfalls of the applied calculated the most widely used geomorphic indices that might methods and discuss ways to overcome some of the problems indicate active tectonics: normalised steepness index, the Chi we encountered. 27 15TH WORKSHOP Abstract book. 15th Emile Argand Conference on Alpine Geological Studies, 12-14 September 2022, Ljubljana, Slovenia. Alpine-Carpathian-Pannonian Geodynamics: the McKenzie and Royden models and the limitations of their applicability Istvan Gyorfi1, Laura Petrescu2, and Felix Borleanu2 1Eotvos Lorand University, Sciences, General Geology, Hungary (istvan_gyorfi@yahoo.ca) 2National Insititute of Earth’s Physics, Magurele, Romania Since the 80s’ the geodynamic evolution of the Alpine-Car- style and timing of extensional deformation is indeed out of pathian-Pannonian (ACP) region has been clearly dominated the reach of model predictions. Shortly afterwards, Royden has by two geodynamic models: McKenzie (1978) and Royden proposed (1988, 1993) that the extension of the Pannonian Ba- (1993). The model of McKenzie was the first numerical model sin System would be coupled with the compressional tectonics to explain the continental extension in terms of lithospheric of the Carpathians. Royden et al. have implied that the driving stretching and following thermal subsidence. The model has force behind the two concurrent processes (e.g. basinal exten-envisaged, that these two processes are recorded by the inter- sion and orogenic growth) would be the subduction roll-back, vening sedimentary processes: the initial syn-rift phase charac- which they thought to be represented by the Vrancea Seismic terized by extensional growth sequences and the subsequent Zone (VSZ) high-velocity subducted slab. This model was sim-thermal phase best described in terms of tectonic quiescence ple and elegant, to such extent, that has been widely adopted with no, or little deformation of the sedimentary cover. The by the majority of the geoscientific community. While it is clear, McKenzie model has been tested first in the North-Sea and that the VSZ is a well documented geodynamic entity (e.g brought serious breakthrough in the understanding of its geo- refraction tomography, focal mechanism solution), remains un-dynamic evolution, and became a strong predictive tool for the clear how far the implied subduction roll-back can be applied oil and gas exploration community. Further on, the model has to the geodynamic evolution of the whole Intra-Carpathian been applied to the Pannonian Basin by Sclater et al. (1980). Region (ICR). There is a number of growing evidences coming The results were ambiguous, and Bally and Snelson (1980) from distinct regions of the ICR, such as the Transylvanian have highlighted that the syn-rift phase is not responding prop- Basin, Apuseni Mountains and ultimately the Pannonian Basin erly to the model prediction, as the amount of the extension suggesting that the subduction roll-back model has certain of the crust was not implying the high heat-flow observed. limitations and cannot be retained as the sole viable solution to In spite of these early concerns, the McKenzie model has explain the Miocene-Pannonian geodynamics of the ACP area. been widely accepted for the Pannonian Basin for the coming Moreover, possible alternative interpretation(s) of the VSZ is decades. Evidences from reflection seismic data coupled with calling for a revision of the mechanisms of basin and orogenic recent industry well-data, however were to confirm that the evolution of the whole region. Bally A. & Snelson S. (1980). Realms of subsidence, Geology McKenzie D. (1978). Some remarks on the development of sedimentary basins. Earth and Planetary Science Letters, 40 (1978) 25-32. Royden L.H. & Horvath F. (eds) (1988). The Pannonian Basin: a Case Study in Basin Evolution. American Association of Petroleum Geologists, Memoir 45. Royden L. H. (1993). Evolution of retreating subduction boundaries formed during continental collision, Tectonics, 12, 629-638. Sclater J.G, Royden L.H., Horvath F., Burchfiel B. C., Semken S. & Stegena L. (1980). The formation of Intra-Carpathian Basins, as determined from subsidence data. Earth Planet. Sci. Lett. , 51, 139-152. 28 15TH WORKSHOP Abstract book. 15th Emile Argand Conference on Alpine Geological Studies, 12-14 September 2022, Ljubljana, Slovenia. How AlpArray is guiding us to a new model of Alpine orogenesis Mark R. Handy1 and the members of 4D-MB and the AlpArray Working Group* 1Freie Universität Berlin, Geologische Wissenschaften, Earth Sciences, Berlin, Germany (mark.handy@fu-berlin.de) *A full list of authors appears at the end of the abstract AlpArray has challenged notions of lithospheric subduction We propose a new model for Alpine orogenesis that invokes along the Alps and its effects on the asthenosphere and oro- changing wedge stability and migrating subduction singularities genic lithosphere. Teleseismic Vp tomography reveals a slab of above the delaminating and detaching Alpine slab in the east to European lithosphere that is largely detached at and below 150 explain eastwest differences in Oligo-Miocene structure, magma-km in the Western and Eastern Alps. Only in the Central Alps tism, erosion and sedimentation in peripheral Alpine basins. A is the slab still attached, possibly reaching down to the MTZ, decrease in Adria-Europe convergence rate to < 1 cm/yr after where it may be connected to subducted remains of Alpine collision at ~35 Ma led to slab steepening and northward mo-Tethys. Downgoing European lithosphere appears thicker and tion of the singularity, combined with increased shortening and more heterogeneous than the Adriatic upper plate. Arcuate taper of the Central Alpine wedge. There, rapid exhumation SKS directions beneath the Alps suggest that asthenosphere and denudation during this stage were initially focused in the not only flowed passively around the sinking slab, but may retro-wedge just north of the Periadriatic Fault. In the Eastern have induced the anomalous northward dip of the detached Alps, slab pull during northward delamination drove subsid-slab segment beneath the Eastern Alps. The structure of the ence and marine sedimentation in the eastern Molasse basin orogenic lithosphere differs profoundly along strike of the Alps, from 29-19 Ma, while the western Molasse basin filled with as revealed by local earthquake tomography, ambient-noise terrigeneous sediments. The dramatic switch at 23-21 Ma from studies, as well as S-to-P receiver-functions and gravity studies: northward advance and stagnation of the northern front in the In the Central Alps west of the Giudicarie Fault where the slab Eastern Alps to southward advance of the southern front in the is still attached, the exhumed retro-wedge of the orogen over- eastern Southern Alps, as well as rapid exhumation of Penninic rides a wedge of Adriatic lower crust. East of this fault where units in the Tauern Window are attributed to slab detachment the slab has detached, exhumation is focused in the orogenic beneath the Eastern Alps combined with a northward and up-core (Tauern Window) north of and above a bulge of thickened ward shift of the subduction singularity to the tip of the lower lower crust of presumed Adriatic origin. The Moho is not offset crust bulge. This is inferred to have reduced the wedge taper by the Giudicarie Fault and shallows eastward, from 50-60 km in the Eastern Alps. Rapid west-to-east filling of the eastern beneath the western Tauern Window to 20-30 km beneath the Molasse basin between 19-16 Ma is interpreted to reflect east-Pannonian Basin. This necessitates massive decoupling at and ward propagation of the slab tear and the onset of Carpathian above the Moho to accommodate coeval Miocene N-S shorten- rollback subduction. ing, orogen-parallel thinning and eastward extrusion of Eastern Alpine orogenic lithosphere. Members of 4D-MB and the AlpArray Working Group: The complete member list of the AlpArray Working Group can be found at http://www. alparray.ethz.ch. A list of active members of the 4D-MB is available at http://www.spp-mountainbuilding.de/research/projects/index.html. 29 15TH WORKSHOP Abstract book. 15th Emile Argand Conference on Alpine Geological Studies, 12-14 September 2022, Ljubljana, Slovenia. A buried fold and thrust belt: the structural geometry of the central part of the Tisza Unit, East Hungary Gábor Héja, Katalin Lőrincz, László Bereczki, Gábor Markos, Gyula Maros, and Márton Palotai Supervisory Authority of Regulatory Affairs, Budapest, Columbus u. 17-23, Hungary (gabor.heja@sztfh.hu) The basement of the south-eastern part of the Miocene Pan- In this study we use modern 3D seismic data sets and well nonian back-arc basin is represented by the Tisza Unit. The data to investigate the central part of the Tisza Unit. Based on deep structure of the Tisza unit is poorly studied, despite its that, the Tisza Unit is a Late Cretaceous fold and thrust belt, significant geothermal and CH potential. This work is a first which can be characterized by major thick-skinned nappes, and step in our structural mapping project, which investigates the second-ordered thin-skinned structures. Such second-ordered structures within the basement of the Pannonian Basin. structures are the active and passive roof-duplexes below the Villány nappe (Derecske), and out-of-the-syncline thrusts in The Tisza unit is composed of Proterozoic to Early Paleozoic the front of the Codru nappe (Vésztő). The basal thrust of the poly-metamorphic basement rocks, and Late Paleozoic to Me- Villány nappe cuts across pre-existing normal faults and asso-sozoic sedimentary cover. The Tisza Unit is built up by three ciated half-grabens, demonstrating the presence of the early main nappes, the Mecsek, the Villány-Bihar and the Codru sub- Alpine rift-related structures. Major nappes are unconformably units. The Tisza Unit is exposed in inselbergs (Mecsek, Villány, overlain by Santonian to Maastrichtian beds, nevertheless, Apuseni Mts.), however, most of it is covered by several km the presence of growth synclines in this succession indicates thick Miocene succession. The pore space containing energy ongoing shortening after major nappe emplacement during the source materials is located in the Miocene Pannonian Basin latest Cretaceous. The Cretaceous fold and thrust belt of the cover sediments, and in the fractured basement rocks near its Tisza Unit is strongly overprinted by Miocene extensional and surface and in their deeper part, especially in the Cretaceous transtensional structures, which are related to the rifting of the sedimentary formation. Our research targets the better under- Pannonian back-arc basin. standing of the Alpine shortening tectonics and structure of the Tisza Unit, with special attention to the structures of these tectonically buried sedimentary basement patches. 30 15TH WORKSHOP Abstract book. 15th Emile Argand Conference on Alpine Geological Studies, 12-14 September 2022, Ljubljana, Slovenia. New knowledge about U-Cu mineralization in the Kozie Chrbty Mts. and its relationship to the late (Neotectonic) structures (Hronic Unit, Western Carpathians, Slovakia) Eva Hoppanová, Štefan Ferenc, Viera Šimonová, and Richard Kopáčik Matej Bel University , Faculty of Natural Sciences, Department of Geography and Geology, Slovakia (ehoppanova@umb.sk) Stratiform U-Cu mineralization (0.02-1.13 % U) in the east- southern blocks faults, and faults with northeast-to-southwest ern part of the Kozie Chrbty Mts. Is bound to the Permian direction causing 10 m declines of southwestern blocks. The volcano-sedimentary complex of the Ipoltica Group, Hronic deposit conditions on the eastern part of the Dúbrava Mts. are Unit (Western Carpathians). The wide surroundings of the limited by the combination of the neotectonic fault systems: deposits are formed by other, Triassic sediments of Hronic Unit Vikartovce, Gánovce and Muráň-Divín. (limestones, dolomites, quartzites, shales) also by Paleogene sedimentary complexes of the Podtatranská Group (sandstones, At the Kravany deposit, local tectonic caused the formation of conglomerates, claystones). The ore deposits (Vikartovce, so-called „zone ore mineralization“, when U-Cu mineralization Kravany, Švábovce, Spišský Štiavnik) are situated in the arcosic occurs in the tectonic zone (reprocessed carbonized plant resi-sandstones of the Upper Permian part of the Kravany Beds with dues, uraninite, pyrite, chalcopyrite and carbonates). carbonized fragments of higher plants. The deposits were ex- ploited during the survey (60s – 70s of the 20th century). Stratiform, infiltration U-Cu-Pb mineralization in the eastern part of the Kozie Chrbty Mts. is bound to the Upper Permian Relatively late tectonic events affected the volume and the clastic sediments (Kravany Beds, member of Malužiná Forma-quality (and also minig-technical conditions) of considered tion, Hronic Unit). Their lithological composition is represented ore deposits. This tectonics resulted in iregular distribution of by green to dark gray fine to medium-grain arcosic sandstones, mineral ore in this region. In the western part of the Dúbrava arcoses, gray-black sandstones and siltstones with a significant Mts. (Vikartovce, Kravany deposits), the distribution of the content of carbonized plant debris. Uranium mineralization ore is relatively regular, limited to 1 – 2 ore bearing horizons. together with Cu and Pb mineralization are concentrated In this case the structure of the deposits is limited mainly by mainly in the cracks and pores of corbonized organic matter. Vikartovce Fault with subvertical sence of movement. Concern- Stratiform U-Cu-Pb mineralization is represented by minerals: ing the tectonic condition, Kravany and Vikartovce deposits uraninite, coffinite, U-Ti oxides accompanied by arsenopyrite, are situated to the north (in the bedrock block) and in close chalcopyrite, pyrite, marcasite, tetrahedrite, tennantite, galena, proximity (200 – 300 m) of Vikartovce Fault of east-to-west sphalerite, quartz, calcite and dolomite. The age of stratiform direction. On the contrary, the Švábovce and Spišský Štiavnik mineralization was set at 263 – 274 Ma, based on U-Pb dating. deposits are located on a neotectonic structure that limits Secondary minerals described in the supergene zone of U ore Dúbrava Mts. from the north (W-E direction). The Kravany and deposits are uranophane, autunite, torbernite, metatorbernite, Vikartovce deposits are disrupted by disjunctive tectonics in azurite, malachite, arsenopyrite, goethite, limonite, covellite, two directions: faults east-to-west causing 5 – 10 m declines of chrysocolla, gypsum and zálesíite. Acknowledgements: This work was supported by the Slovak Research and Development Agency under the contract APVV-19-0065, VEGA 1/0563/22, KEGA 033UMB-4/2021. 31 15TH WORKSHOP Abstract book. 15th Emile Argand Conference on Alpine Geological Studies, 12-14 September 2022, Ljubljana, Slovenia. Palaeoenvironmental and drainage network reconstitution of the Oligocene Western Alpine Foreland Basin Bastien Huet1, Nicolas Bellahsen1, Nicolas Loget1, Eric Lasseur2, and Justine Briais2 1Sorbonne Université, Institut des Sciences de la Terre de Paris, Paris, France (bastien.huet@sorbonne-universite.fr) 2BRGM, Orléans, France The Western Alpine Foreland Basin (“French Molasse Ba- composed of massive meandering deposits, which evolve to sin”) is located along the western Alps and is composed of braided river and alluvial fan in a regressive continental se-Oligo-Miocene formations resulting from the erosion of the quence following the flysch formation. Transition from marine alpine range. Although the Miocene molasse basin have been distal turbidites is often missing except in Dévoluy syncline widely described since the last decades, Oligocene basins lack where tidal and shoreface deposits precede fluvial molasse. documentation in terms of palaeoenvironmental evolution and Exotic material from the internal alps is very common and source to sink approach. Most of these basins formed under indicates high landforms nearby. In the Rhone Valley, a mas-both the Alpine influence and the European Cenozoic Rift Sys- sive fluvial system has been identified on seismic and well log tem influence and developed in lacustrine environment with data in the Bas-Dauphiné and we documented a 900 m field local sedimentation next to active normal faults. Several fluvial section with two meandering formations with exotic minerals formations with exotic materials have been briefly described in the Mormoiron basin. Paleocurrents and channels direction and could correspond to a transport from the internal parts indicate a major divide located east of Diois-Baronnies range of the Alps, where collision started at the Eocene/Oligocene with Dévoluy fluvial systems flowing to the north and other boundary. Here, we propose a new tectono-sedimentary study Red Molasse sites located south of the divide converging to of these fluvial deposits based on extensive fieldwork (facies St-Geniez system. On a regional scale, it may be possible that analysis, sequence stratigraphy, palynological analysis) and early salt tectonic which has been widely described caused this reinterpretation of available subsurface data (seismic profile, particular drainage network. South of the divide, converging well data). The goal is to provide a new palaeoenvironmental fluvial formations may have flowed in an Est-West valley be-reconstitution of the Oligocene molasse basin(s) with regional tween Diois-Baronnies range and Ventoux-Lure Montain where correlations and to determine the evolution of early alpine tectonic and Eocene landforms link to the Pyreneo-Provençal drainage network. We focus on the entire Western Alpine orogen have been documented. These deposits where probably Foreland Basin from the Rhone Valley (Bas-Dauphiné, Valréas, connected with Mormoiron and Bas-Dauphiné fluvial forma-Mormoiron) to the Digne Thrust where Oligocene molasse is tions and formed a major drainage system located in the Rhone called « Red Molasse » (Dévoluy, Faucon-du-Caire, St-Geniez, Valley. Esclangon, Barrême). First results show that Red Molasse is 32 15TH WORKSHOP Abstract book. 15th Emile Argand Conference on Alpine Geological Studies, 12-14 September 2022, Ljubljana, Slovenia. Recording of cyclicity in the sediments of the Bajocian and Lower Bathonian on the basis of magnetic susceptibility (Carpathians, Poland) Jolanta Iwańczuk1, Mathieu Martinez2 and Kinga Bobek1 1THE POLISH GEOLOGICAL INSTITUTE - NATIONAL RESEARCH INSTITUTE, Climate and Environmental Changes Program, Poland (jolanta.iwanczuk@pgi.gov.pl) 2Univ Rennes, CNRS, Géosciences Rennes – UMR 6118, 35000 Rennes, France Investigated section is located on the eastern slope of the Ždi- on the basis of the MS, K, Th, U and δ 13C curves. The oldest IIA arska Vidla, Tatra Mts. (Slovakia), along the old tourist path. interval is characterized by a weak positive linear correlation The section belongs to the Križna nappe and to the Havran between MS to Th, Th/U and CGR, which suggests an associ-and the Bujačí unit. Pelagic and hemipelagic sedimentation ation of MS with the supply of terrigenous elements to basin. of the spotted limestones and marls prevailed on the margin The p-values associated with received Pearson R are much of the Zliechov (Križna) during the Early and Middle Juras- above the assumed significance level (0.05), indicating that re-sic. The spotted limestones of the Tatra Mts. depending on ceived results are statistically insignificant. In the IIB and III in-the authors, are included in the Janovky Formation or in the terval, MS correlates inversely to Th, CGR, Th/U, what it might Sołtysia Marlstone Formation. The investigated Ždiarska Vidla show that increase MS is related to oxygen deficiency. Within section is 200-m thick. This unit is dated to the Bajocian based the level IIB, values of Pearson r-value for correlation between on lithological similarity to the Kopy Sołtysie area, where rare MS and Th, CGR, U and K varies between -0.2 and -0.43 with ammonite fauna was described. The lithology is composed of p-values in the range from 0.03 to 0.3 meaning, that only part spiculite limestones and marly spiculite limestones (with marly of the results is statistically significant. The III interval is char-spiculite wackestone–packstone, and marly bioclastic filament acterized by a moderate negative linear correlation between wackestone microfacies). Field magnetic susceptibility (MS) MS and Th, K and CGR, where Pearson R reaches values from and gamma–ray spectrometric measurements (indicating -0.42 to -0.56 with p-values much below the assumed level of content of potassium, K (%); uranium, U (ppm,); thorium, Th 0.05, meaning that received results are statistically significant. (ppm)) have been carried out. The Ždiarska Vidla section has Spectral analyses done on the MS signal in Intervals II and III also been sampled for carbon isotopes with resolution of ca. reveal cycles of 18 m, 4-5 m and 1.3-1.8 m, respectively relat-0.5-1 m. The bulk carbonate obtained carbon isotope curve is ed to the 405-kyr, 100-kyr and 40-kyr cycles. The duration of characterized by positive shift. It is assigned to the Lower Ba- Intervals II and III are thus assessed at 4.4 to 4.5 Myr, with a jocian. The section is subdivided into three parts (IIA, IIB, III) mean sedimentation rate of 4.4 cm/kyr. 33 15TH WORKSHOP Abstract book. 15th Emile Argand Conference on Alpine Geological Studies, 12-14 September 2022, Ljubljana, Slovenia. On the way to building the Norian conodont biozonation of the Circum-Pannonian Region Viktor Karádi Eötvös Loránd University, Institute of Geography and Earth Sciences, Department of Palaeontology, Budapest, Hungary (karadi.viktor@ttk.elte.hu) Conodont biozonation of the Norian (Upper Triassic) of the and Ancyrogondolella ex gr. triangularis. In the upper half of Western Tethys realm is in development from the 1970’s, how- the section, bedding is often disturbed, intervals of fractured ever, a satisfactory scheme has not yet been established. The blocks are common. Conodonts with morphological characters problem originates in the over-simplified taxonomy of Norian transitional to those of typical Middle Norian species first conodonts, since biostratigraphic investigations have never occur at the lower level of this interval, though Lacian forms coupled with thorough and detailed systematic studies. Even remain dominant. This part represents the Lower-Middle Nothe zonal schemes proposed after the millennium were based rian transition, which is often characterized by sedimentary mainly on the species described in the second half of the 20th breccias and/or fissure fills (e.g., Dovško section – Karádi et al., century. Consequently, conodont zones of the existing schemes 2021; Kälberstein quarry section – Gawlick and Böhm, 2000). cover longer time intervals, although a finer subdivision would Species indicating inevitably Middle Norian age (Alaunian-1) be possible. An ongoing research attempts to refine the Norian were found 1.5 m below the top of the section where Lacian conodont biozonation of the Circum-Pannonian Region based species are absent. This fauna is composed of Ancyrogondolella on abundant conodont faunas of various localities. equalis, Ancyrogondolella ex gr. transformis and Mockina ex gr. matthewi. The old trench at Mátyás Hill of the Buda Hills (Transdanu- bian Range, Hungary) exposes a ca. 20 m thick sequence of Due to the large morphological variety and the very low hemipelagic cherty dolostones of Lower to Middle Norian age. number of figured specimens, the taxonomic revision of these Dense sampling of the section yielded well-preserved conodont Norian assemblages is yet to be done. Anyhow, the establish-elements in high numbers. The lower half of the succession ment of a high-resolution Norian conodont biozonation of the can be dated as Lower Norian (Lacian-3) based on the pres- Circum-Pannonian Region seems feasible, which will allow a ence of Norigondolella navicula, Norigondolella hallstattensis better correlation potential within the Western Tethys realm. Acknowledgements: The research was supported by the National Research, Development and Innovation Office NKFIH PD-131536 grant. Gawlick, H.-J., & Böhm, F. (2000). Sequence and isotope stratigraphy of Late Triassic distal periplatform limestones from the Northern Calcareous Alps (Kälberstein Quarry, Berchtesgaden Hallstatt Zone). International Journal of Earth Sciences, 89, 108–129. Karádi, V., Kolar-Jurkovšek, T., Gale, L., & Jurkovšek, B. (2021). New Advances in Biostratigraphy of the Lower/Middle Norian Transition: Conodonts of the Dovško Section, Slovenia. Journal of Earth Science, 32, 677–699. 34 15TH WORKSHOP Abstract book. 15th Emile Argand Conference on Alpine Geological Studies, 12-14 September 2022, Ljubljana, Slovenia. Crustal structure in the eastern Alps from ambient-noise Tomography Emanuel Kästle1 and the AlpArray Working Group* 1Freie Universität Berlin, Institut für geologische Wissenschaften, Berlin, Germany (emanuel.kaestle@fu-berlin.de) *A full list of authors appears at the end of the abstract Since the onset of continental collision in the eastern Alps, uncertainties. The shallow structure is well correlated with the several large-scale reorganizations have affected the crustal major faults in the area. Additional information from the an-structure, such as Adriatic indentation, eastward extrusion or isotropy at mid to lower crustal levels is interpreted in terms of the Tauern window exhumation. This work aims to improve the strain direction. Eastward orientated fast axis are observed the understanding of the tectonic history of the region, by pro- at a large depth range in the central part of the mapped region. viding a new shear-velocity model of the eastern Alpine crust. This may indicate that the eastward extrusion affects all crustal It makes use of data from the AlpArray and the dense SwathD levels down to Moho depths. The mapped features are com-networks from which phase velocities are measured. These pared to previous works from local earthquake tomography are inverted in a two-step approach based on a Markov-Chain and receiver functions to provide a joint interpretation of the Monte Carlo sampler to obtain the model structure and its crustal structure. AlpArray Working Group: http://www.alparray.ethz.ch 35 15TH WORKSHOP Abstract book. 15th Emile Argand Conference on Alpine Geological Studies, 12-14 September 2022, Ljubljana, Slovenia. Seismic activity along the Periadriatic and Sava Faults in the past two millennia – an archaeoseismological assessment Miklos Kazmer1 and Krzysztof Gaidzik2 1Eötvös University, Budapest, Hungary (mkazmer@gmail.com) 2Institute of Earth Sciences, University of Silesia in Katowice, Sosnowiec, Poland Most faults of the Periadriatic Fault System have been active Roman Celeia (Celje) at the Savinja / Sava faults, and Roman during Oligocene and Miocene times. Its western part seems to Siscia (Sisak) nearby the Croatian Sava fault. Damaged upright be inactive ever since, while the Lavanttal and Sava faults in walls of Medieval buildings and deformed floors of Roman set-the east show limited seismic activity. We conducted a system- tlements testify to local intensity up to IX. Ongoing studies of atic archaeoseismological survey along the Periadriatic-Sava archaeological stratigraphy and construction history allow dat-fault system, assessing buildings and archaeological sites for ing of one or more seismic events at each site, ranging from the earthquake damage. Eight sites, four Roman and four Medie- 1st century AD to the 17th century. We would be cautious about val, display evidence for destructive earthquakes during the pointing out epicentres at this moment. However, it is remark-past 2000 years. These are San Candido (Medieval) and Lienz able that sites, 70 km apart in average, along a a 380 km long (Medieval) on the Pustertal fault, Teurnia (Roman) and Mill- segment of an ‘inactive’ fault zone carry evidence for so many statt (Medieval) on the Mölltal fault, Arnoldstein (Medieval) high-intensity destructive events. and Magdalensberg (Roman) just north of the Karavanke fault, 36 15TH WORKSHOP Abstract book. 15th Emile Argand Conference on Alpine Geological Studies, 12-14 September 2022, Ljubljana, Slovenia. Facies analysis of Ladinian and Carnian beds in the area of Rute Plateau (External Dinarides, Central Slovenia) Anja Kocjančič1, Boštjan Rožič2, Luka Gale2,4, Primož Vodnik3, Tea Kolar-Jurkovšek4 and Bogomir Celarc4 1Ivan Rakovec Institute of Palaeontology, ZRC SAZU, Novi trg 2, 1000 Ljubljana, Slovenia (anja.kocjancic@zrc-sazu.si) 2Department of Geology, NTF, UL, Aškerčeva cesta 12, 1000 Ljubljana, Slovenia 3ELEA iC, Dunajska c. 21, 1000 Ljubljana, Slovenia 4Geological Survey of Slovenia, Dimičeva ulica 14, 1000 Ljubljana, Slovenia The Rute Plateau is a region located 25 km south of Ljubljana. carbonates. Each of these Ladinian facies is characteristic of a Structurally, it belongs to the External Dinarides, which form particular sedimentary environment and is indicated from the an extensive fold and thrust belt. The study area is located in most distal sedimentary environment (F1) to the most proxi-the eastern part of the Hrušica Nappe in a very complex tecton- mal carbonate platform environment (F4). Facies F1 consists ic area between two major NW-SE fault zones. of greenish to light ochre bentonitic clays, tuffitic sandstones, pelitic tuffs, and subordinate felsic extrusive rocks. Facies F2 The peculiarity of the Rute Plateau consists in a varied succes- consists of laminated black micritic limestones (mudstones to sion of sedimentary and volcanoclastic rocks of Ladinian and wackestones) with horizons of bioclastic packstones rich in fila-Carnian age, while the whole area is divided into different ments, limestones rich in organic residue and interbedded with tectonic blocks with local differences in stratigraphic evolution. dark chert laminas and marlstones. In facies F3 we find up to The reason for these deformations and the variability of the 30 cm thick beds of calcarenites, limestone breccias often with paleotopography lies in the Middle Triassic extensional phase, large olistoliths, graded and laminated calciturbidites - mostly which completely disintegrated the uniform Slovenian carbon- packstone, grainstone and rudstone beds with rare chert lam-ate platform at the end of the Anisian (for details see Rožič inas and nodules. Finally, facies F4 consists largely of massive, et al., this volume). Subsequently, the Ladinian strata of the light grey calcimicrobial and dasycladacean limestones with External Dinarides reveal that deep marine sediments in this horizons or lenses of white bioclasts and intraclasts derived area were deposited in small basins or tectonic depressions, from coral reefs. The last two facies are commonly dolomitized. while carbonate deposition continued on higher or relatively less subsided tectonic blocks (isolated platforms). During the At the end of the early Carnian, the entire region was subject-Ladinian, tectonic movements were also accompanied by vol- ed to the regional emersion phase when deposition of clastic canic activity. sediments began. It is characterized by facies F5 - red clastic sediments consisting mainly of sandstone with quartz grains Six sedimentological sections were logged in the studied area, and carbonate lithoclasts and conglomerates. Within all these and the Ladinian strata were divided into four different facies: facies, we were able to determine 28 different microfacies, F1 - deep marine (volcano)clastic rocks, F2 - hemipelagic lime- which, based on their composition, further elucidate sedimen-stones, F3 - resedimented limestones and F4 - shallow marine tation in different paleoenvironments. 37 15TH WORKSHOP Abstract book. 15th Emile Argand Conference on Alpine Geological Studies, 12-14 September 2022, Ljubljana, Slovenia. Origin of submarine swell (Czorsztyn Ridge of the Pieniny Klippen Belt, Polish/Ukrainian Carpathians) and it’s geotectonic consequences by biostratigraphy/volcano- sedimentary record Michał Krobicki AGH University of Science and Technology; Geology, Geophysics and Environmental Protection; General Geology and Geotourism; Mickiewicza 30, 30-059 Kraków, Poland (krobicki@agh.edu.pl) The most important geotectonic element within Polish/Slovaki- Tectonic rejuvenation of Middle Jurassic structures took an/Ukrainian Western Carpathians basins has been the Czorsz- place during the earliest Cretaceous (Berriasian) times and tyn Ridge (Swell), which originated during Early Bajocian have been connected with active volcanogenic events which time. Then, palaeogeographicaly during Middle Jurassic–Late occur now within several tectonostratigraphic units of the Cretaceous span it has been the main object which separated Ukrainian Carpathians, including PKB. In the Veliky Kamenets two large Carpathians basins – the Magura Basin on NW side active quarry (PKB) a continuous section occurs with a Lower and the Pieniny Basin on SE side – and therefore the detail dat- Jurassic (since Hettangian?) to the lowermost Cretaceous ing of its origin is crucial for recognition of its geodynamic sig- (Berriasian) sedimentary succession. The biostratigraphy of nificance. This first uplift is correlated with stratigraphical hia- the Toarcian-Berriasian part of this section is very precisely tus between sedimentation of dark/black shales of oxygen-poor based on ammonites, dinoflagellates and calpionellids. Basaltic environments (latest Pliensbachian–earliest Bajocian) and rocks occur in the uppermost part and overlie creamy-white white/light grey crinoidal limestones of well oxygenated re- Calpionella-bearing limestones. They are directly covered by gimes (late Early Bajocian), which documented drastic change biodetritic limestones and synsedimentary breccias. The lat-of sedimentation/palaeoenvironments which took place in ter are the so-called Walentowa Breccia Member of the Łysa meantime as effect of uplift. This stratigraphical gap was per- Limestone Formation, according to the Polish and Slovakian fectly dated biostratigraphicaly by ammonites collected from parts of the PKB, which are dated by calpionellids as middle the basal part of crinoidal limestones in several outcrops of the and/or upper Berriasian and upper Berriasian, respectively. Polish part of the Pieniny Klippen Belt (PKB). The evidences Importantly, in this breccia some clasts of basaltic rocks occur of condensation event at the beginning of crinoidal limestones (sometimes developed as pillow lavas and/or peperites) which sedimentation are marked by: phosphatic concretions concen- implies they are middle and/or upper Berriasian in age as well. tration, pyrite concretions, large clasts of green micritic lime- New investigations are concentrating on radiometric dating of stones, fossils (ammonites, belemnites, brachiopods). On the these basaltic rocks, which geochemically have previously been other hand, high variable thickness of these limestones (from determined to be caused by intra-plate volcanism. Integrated ca. 10 m up to 100 m) suggests origin of synsedimentary tec- litho-, bio-, chemo- and magnetostratigraphic studies carried tonic blocks and troughs during syn-rift episode. This Bajocian out in this section can be here supplemented by absolute age tectonic activity within Pieniny Klippen Basin corresponds very determination of a submarine volcanic event. Additionally, well with others Middle Jurassic Western Tethyan geodynamic this is a unique chance to calibrate the absolute age of the J/K reorganizations. Estimation of duration of aforementioned boundary. hiatus – based on a cyclostratigraphic analysis of the carbonate content from the Subalpine Basin in France, which indicates that the Early Bajocian only lasted c. 4.082 Ma – time necessary for origin/uplift of the Czorsztyn Ridge is about 2 Ma. 38 15TH WORKSHOP Abstract book. 15th Emile Argand Conference on Alpine Geological Studies, 12-14 September 2022, Ljubljana, Slovenia. Variation in style of Adriatic lower crust indentation west and east of the Giudicarie Fault Eline Le Breton1, Mark R. Handy1, Peter McPhee1, Azam Jozi-Najafabadi2 and Christian Haberland2 1Freie Universität Berlin, Institute for Geological Sciences, Geological Sciences, Berlin, Germany (eline.lebreton@fu-berlin.de) 2GFZ German Research Centre for Geosciences, Potsdam, Germany Neogene tectonics of the Alps is marked by the indentation of These sections reveal differences in the style of indentation tec-the Adriatic Plate into the Alpine Orogen and onset of escape tonics, specifically in the behavior of the Adriatic lower crust, tectonics in the Eastern Alps. This resulted in the formation of between the Central and Eastern Alps. West of the GF, the a system of strike-slip faults, mainly the Periadriatic Fault (PF), lower crust of the Adriatic plate detached from its mantle lith-separating the Eastern and Southern Alps, and the sinistral osphere and wedged within the Alpine orogenic crust, whereas Giudicarie Fault (GF), which offsets the PF. The GF is kinemat- to the east of the GF, the Adriatic lower crust forms a bulge just ically related to Neogene shortening in the Southern Alps but to the south of the PF. The Adriatic upper crust responded by questions remain on its geometry at depth, in particular its shortening and formation of a fold-and-thrust belt, while the relation to the crust/mantle boundary (Moho). Europe-derived orogenic crust underwent upright, post-nappe folding and exhumation in the Tauern Window. We discuss In this study, we compare geological cross-sections and pre-ex- the possible causes for such along-strike variations in terms of isting geophysical datasets (controlled-source seismology, changes in crustal rheology and structural inheritance within local earthquake tomography) with a new high-resolution 3-D the Adriatic Plate, contrasting metamorphic histories within local earthquake tomographic model from the AlpArray and the Alpine orogenic crust west and east of the GF, and potential SWATH-D experiment along two N-S profiles west and east Neogene slab break-off beneath the Eastern Alps. of the GF, as well as a NW-SE oriented section across the GF. 39 15TH WORKSHOP Abstract book. 15th Emile Argand Conference on Alpine Geological Studies, 12-14 September 2022, Ljubljana, Slovenia. Exhumation of metamorphic core complexes of the internal Dinarides was triggered by the opening of the Pannonian Basin Georg Löwe1, Dejan Prelević2,3, Blanka Sperner4, Susanne Schneider7, Jörg A. Pfänder4, Philipp Balling1, Sami Nabhan5, Albrecht von Quadt Wykradt-Hüchtenbruck6 and Kamil Ustaszewski1 1Institut für Geowissenschaften, Friedrich-Schiller-Universität Jena, Jena, Germany (georg.loewe@uni-jena.de) 2Rudarsko-Gološki fakultet, Univerzitet u Beogradu, Beograd, Serbia 3Institut für Geowissenschaften, Johannes-Gutenberg-Universität Mainz, Mainz, Germany 4Institut für Geologie, TU Bergakademie Freiberg, Freiberg, Germany 5Department of Biology, Nordcee, University of Southern Denmark, Odense, Denmark 6Institut für Geochemie und Petrologie, ETH Zürich, Zürich, Switzerland 7Federal Office of the Safety of Nuclear Waste Management, Berlin, Germany The Sava suture zone of the internal Dinarides contains during E-W extension at approximately 20 Ma, Cer MCC was Maastrichtian trench-fill sediments, termed “Sava flysch” that exhumed as part of the underlying Adriatic basement during record the closure of the northern branch of the Neotethys. N-S extension between 17-16 Ma. For the Cer MCC, a concor-Subsequent collision between Adria-derived thrust sheets and dia age of 17.6±0.1 Ma (2σ) obtained by U-Pb LA-ICP-MS on blocks of European affinity in Latest Cretaceous to Paleogene zircons from an S-type granite in combination with an Ar-Ar times culminated in the formation of the Dinarides fold-and- inverse isochron age of 16.6±0.2 Ma (2σ) obtained on white thrust belt. The suture zone hosts numerous Oligocene plutons mica from the same sample, indicate a cooling rate of approxi-of I-type granitic composition. Many of these intrusions are mately 400 °C/Ma. located in the center of metamorphic core complexes (MCCs) that were exhumed in early Miocene times. This phase of Our results contribute to the idea of rapid exhumation of post-collisional extension was concomitant with the opening mid-crustal material in the form of MCCs in response to the of the northerly adjacent Pannonian Basin and associated with opening of the Pannonian Basin. This is further corroborated granitic S-type magmatism. Both the processes responsible for by results of Raman spectroscopy on carbonaceous material, as extensional deformation and magmatic activity in the internal the temperature profile across the shear zone implies extremely Dinarides are still a matter of debate. condensed isotherms of 250 °C/km. Additionally, U-Pb analyses show that zircons of the I-type intrusion contain inherited cores Our Study contributes spatio-temporal constraints to better with age maxima at 270 Ma and 516 Ma and newly formed understand the tectono-magmatic processes of this area. We rims with an age maximum at 31.7 Ma, indicating the timing present field-kinematic, geochronological, and thermobaro- of intrusion. The S-type granite of Cer in parts reworks the metric data from two MCCs at the transition between the I-type intrusion, as inherited cores include ages of 31-32 Ma, internal Dinarides and the Pannonian Basin. Both MCCs are while the rims show an age of 17-18 Ma, suggesting a syn-ex-characterized by plutonic rocks in the center, surrounded by up tensional emplacement. Our data further shows that zircons of to amphibolite-grade mylonites of exhuming shear zones. Het- the I-type intrusion contain a significant amount of inherited erogeneous extensional reactivation of formerly contractional cores with an age spectrum that resembles the detrital age structures that gave rise to these core complexes as low-angle spectrum from sediments of the Sava zone. This challenges the detachments in the early Miocene is indicated by a variation in idea that these I-type melts were solely generated from igneous deformation ages of 3 Ma, obtained by Ar-Ar in-situ dating of protoliths, and rather suggests a formation from melting of Pa-white mica from deformed rocks of the respective shear zones. leozoic to Mesozoic successions constituting tectonically buried While Motajica MCC was exhumed from within the Sava zone nappes of the internal Dinarides. 40 15TH WORKSHOP Abstract book. 15th Emile Argand Conference on Alpine Geological Studies, 12-14 September 2022, Ljubljana, Slovenia. Challenges in the interpretation of the structural and metamorphic record in the Adula and Cima Lunga units (Central Alps) Matteo Maino1, Filippo Schenker2, Leonardo Casini3, Stefania Corvò1, Michele Perozzo1, Antonio Langone4 and Silvio Seno1,2 1Departiment of Earth and Environmental Sciences, University of Pavia, Pavia, Italy (matteo.maino@unipv.it) 2Institute of Earth Sciences, SUPSI, Mendrisio, Switzerland 3Department of Chemistry, Physics, Mathematics and Natural Sciences, University of Sassari, Sassari, Italy 4IGG,CNR, Pavia, Italy The Adula and Cima Lunga units show the best preserved on the estimation of the pressure and temperature conditions record of the deformation and metamorphic history of the represent the major tool for tectonic reconstruction as proxies Central Alps. Alpine studies lasting more than a hundred years of the burial and exhumation history of the rocks during sub-documented a complex tectono-metamorphic evolution, in- duction-exhumation phases. cluding the presence of relicts of ultrahigh pressure and high temperature metamorphism. Throughout this long history of Alternative explanations highlight the role of deformation in researches, a few key questions stand out, still challenging the promoting the coexistence of multiple local equilibria, which geological community. Major questions regard how to reconcile cease to correlate with lithostatic conditions and thus burial the structural pattern with the metamorphic path, as well as depths. In this view, the non-hydrostatic stress and the local the timing relationships. The occurrence of ultrahigh-pressure temperature deviations are accounted as important compo-and/or high-temperature rocks embedded within significantly nents potentially modifying the metamorphic system. lower grade metamorphic rocks rises a major challenge for In this contribution, we show new structural, petrological and developing a consistent geodynamic model for exhumation thermochronometric data from the Adula and Cima Lunga of such deep-seated rocks. Subduction zones are, in fact, effi- units. The wide dataset comprises new field mapping covering cient players driving material from the surface down into the the entire areas (several hundred square kilometres) and struc-Earth’s mantle. However, the mechanisms to exhume part of tural-petrochronological analyses at the meso- to micro-scale. this material (and particularly the denser oceanic rocks) back Our results show the highly variable pressure-tempera-to the shallow crust are still highly debated. Scientists gener- ture-time-deformation paths experienced by the compositional-ally invoke either mechanical decoupling within a tectonic ly heterogeneous rocks of the Cima Lunga and Adula nappes. mélange or variable metamorphic re-equilibration during the We present evidence of contrasting metamorphic records retrograde path. These interpretations are based on the com- among the rocks of these nappes, providing arguments to dis-mon assumption that the mineral assemblages form under cuss pros and cons of the tectonic models proposed to explain lithostatic pressure and near-equilibrium regional geothermal these contrasting metamorphic records. gradients. Hence, the resulting metamorphic histories based 41 15TH WORKSHOP Abstract book. 15th Emile Argand Conference on Alpine Geological Studies, 12-14 September 2022, Ljubljana, Slovenia. A journey towards the forbidden zone: a new, cold, UHP unit in the Dora-Maira Massif (Western Alps) Paola Manzotti1, Federica Schiavi2, Francesco Nosenzo1, Pavel Pitra3 and Michel Ballèvre3 1Stockholm University, Department of Geological Sciences, Sweden (paola.manzotti@geo.su.se) 2Université Clermont Auvergne, CNRS, IRD, OPGC, Laboratoire Magmas et Volcans, 63000 Clermont-Ferrand, France 3Univ Rennes, CNRS, Géosciences Rennes – UMR 6118, F–35000 Rennes, France The distribution of ultrahigh-pressure metamorphism ( UHP) increase in P and T (25–27 kbar 470–500 °C) (stage 1), up to at the scale of a mountain belt is of prime importance for the coesite stability field (27–28 kbar 520–530 °C) (stage 2), as deciphering its past subduction history. In the Western Alps, well as sub-isothermal decompression of about 10 kbar (down to coesite has been recognized in the southern Dora-Maira mas- 15 kbar 500–515 °C) (stage 3). The main regional, composite, sif, in the lens-shaped Brossasco-Isasca Unit, but has not been foliation, marked by chloritoid and rutile, began to develop found up to now in the other parts of the massif. We report during this stage, and was then overprinted by chloriteilmenite the discovery of a new UHP unit in the northern Dora-Maira (stage 4). The Chasteiran Unit is discontinuously exposed in Massif (Western Alps), named Chasteiran Unit (Manzotti et the immediate hangingwall of the Pinerolo Unit, and it is lo-al., 2022). It is only a few tens of metres thick and consists of cated far away from, and without physical links to the classic garnet-chloritoid micaschists. Garnet inclusions (chloritoid, UHP Brossasco-Isasca Unit. Moreover, it records a different, rutile) and its growth zoning allow to precisely model the P–T much colder, P–T evolution, showing that different slices were evolution. Coesite crystals, which are pristine or partially trans- detached from the downgoing subduction slab. The Chasteiran formed to palisade quartz occur as inclusions in the garnet Unit is the fourth and the coldest Alpine UHP unit known so far outer cores. According to thermodynamic modelling, garnet in the entire Alpine belt. Its P–T conditions are comparable to displays a continuous record of growth during the prograde the ones of the Tian Shan coesite-chloritoid-bearing rocks. Manzotti, P., Schiavi, F., Nosenzo, F., Pitra, P., Ballèvre, M. (2022). A journey towards the forbidden zone: a new, cold, UHP unit in the Dora-Maira Massif (Western Alps). Contributions to Mineralogy and Petrology, 117, article 59. https://doi.org/10.1007/s00410-022-01923-8 42 15TH WORKSHOP Abstract book. 15th Emile Argand Conference on Alpine Geological Studies, 12-14 September 2022, Ljubljana, Slovenia. Tectonic implications of paleomagnetic results from the Northern Adriatic area: an overview Emö Márton1, Vlasta Ćosović2, Katica Drobne3, Alan Moro2, Damir Bućković2 and Gábor Imre1 1SARA, Geophysical Department, Paleomagnetic Laboratory, Budapest, Hungary (paleo@sztfh.hu) 2Sveuciliste u Zagrebu, Prirodoslovno-matematicki fakultet, Geoloski odsjek, Zagreb, Croatia 3Ivan Rakovec Institute of Palaeontology, ZRC SAZU, Novi trg 2, 1000 Ljubljana The systematic paleomagnetic investigations concentrating on The paleomagnetic results, which permit to conclude to poten-the northern part of stable Adria and the External Dinarides tial large-scale relative movement between areas, suggest that provided tectonically applicable results for nearly 200 localities stable Adria and the whole chain of the Adriatic islands moved from Italy, Slovenia and Croatia. The ages of the studied local- in a co-ordinated manner, i.e. the islands represent the imbri-ities were tightly controlled by a bed by bed checking of the cated margin of stable Adria, at least from the Aptian onward. fossil content. The age of the acquisition of the magnetization During the Late Cretaceous, the area was close (38 °N) to the was constrained by between-locality fold/tilt test, which often northernmost limit (40 °N) of the intensive carbonate produc-proved the pre-deformation “primary” age of the magnetiza- tion (carbonate factory). Stable Adria with its imbricated mar-tion. It is important to emphasize that most of the sampled gin exhibits about 30° larger CCW rotation than the High Karst sediments were shallow water carbonates with weak natural belonging to the Dinaric platform, thus giving further support remanent magnetizations (about 30 % of the sampled localities to considering the chain of the Adriatic island as belonging failed to yield paleomagnetic signal). However, those providing to Adria. The practically parallel “primary” paleomagnetic results are extremely valuable, for inclination flattening is prac- declinations characterizing the Northern Adriatic area are at tically absent in platform carbonates, therefore the estimation variance with the oroclinal origin of the arcuated shape of the of the paleolatitudes are reliable. chain of the Adriatic islands and of the thrust front between them and stable Adria. We attribute this shape to the domi- The majority of the tectonic models published for the area are nance of the Late Cretaceous E-W compression in the northern in agreement about the existence of two Mesozoic carbonate segment, the Late Eocene-Oligocene NE-SW compression in the platforms, an Adriatic and a Dinaric, which came into contact central segment, and the N-S oriented Neotectonic compres-during the Late Eocene-Oligocene thrusting of the latter over sion in the Central Adriatic area. the former. They are in the External Dinarides, but the exact boundary between them is a matter of discussion. The tec- tonostratigraphic complexity of the External Dinarides is the main reason for the large number of models published for the Northern Adriatic area. Acknowledgements: This work was financially supported by the National Development and Innovation Office of Hungary project K 128625. 43 15TH WORKSHOP Abstract book. 15th Emile Argand Conference on Alpine Geological Studies, 12-14 September 2022, Ljubljana, Slovenia. Pressure-temperature-time evolution of Austroalpine meta- morphic rocks from the southeastern Pohorje Mountains Hans-Joachim Massonne and Botao Li School of Earth Sciences, China University of Geosciences at Wuhan, China (h-j.massonne@mineralogie.uni-stuttgart.de) We have studied eclogite, garnet clinopyroxenite, and gar- pressures up to 2.4 GPa in the Eocene. For example, two gener-net-bearing micaschist and gneiss from the southeastern flank ations of potassic white mica (phengite) formed in micaschist. of the Pohorje Mountains (Mts.) in order to better understand The Eo-Alpine one was relatively coarse grained, whereas the the pressuretemperature (P-T)-time evolution of these rocks. Eocene generation replaced this coarse-grained phengite by Geochronology was performed by in-situ analyses of monazite newly grown small flakes. No indications for ultrahigh-pressure in different textural positions with an electron microprobe and metamorphism were found. a laser-ablation inductively coupled plasma mass-spectrometer. P-T trajectories were obtained by thermodynamic modelling We interpret our findings, including previous results on rocks considering strongly the chemical zoning of garnet and mica of our study area in the Pohorje Mts., in a geodynamic context and the mineral inclusions in these phases. In addition, we as follows: A first collision of continental (micro)plates oc-calculated the influence on intracrystalline cation diffusion on curred in the Late Cretaceous after a branch of the Neotethys garnet zoning also to gain time constraints. Ocean was closed. The subduction of the corresponding ocean- ic plate including sediments on top led to eclogite (+ HP gar- Two high-pressure (HP) events were proved for metamorphic net clinopyroxenite) and HP micaschist which were exhumed rocks of the Pohorje Mts. These events occurred at tempera- during the continent-continent collision in an exhumation tures between 570-650 °C for micaschist and 670-740 °C for channel. About 45 Ma after this Eo-Alpine collisional event, eclogite + garnet clinopyroxenite in Late Cretaceous and another part of the Neotethys Ocean was closed followed by a Eocene times. In addition, we found that a micaschist sample second collision of continental (micro)plates. This process led taken close to the Pohorje pluton was partially overprinted in to clearly overthickened crust and deep burial of rocks residing the Miocene (18.9±0.2 Ma) by this intrusion at depths of 30- in the Eo-Alpine exhumation channel. Exhumation of the stud-32 km. Thus, the subsequent uplift of the Pohorje pluton and ied metamorphic rock units, probably mainly caused by surface its surrounding occurred at a mean rate of 1.6-1.7 mm/a. The erosion, followed this Eocene collisional event. A particular studied metamorphic rocks were also significantly exhumed event in the Miocene is characterized by intrusions of large probably soon after the Eo-Alpine event that had led to peak volumes of acidic magma. These intrusions formed the Pohorje pressures up to about 2.3 GPa. This exhumation was accom- pluton, which produced discernable contact metamorphism, panied by cooling. Another burial process followed during for instance in micaschist, close to its margin. which Eo-Alpine rocks were significantly overprinted at peak 44 15TH WORKSHOP Abstract book. 15th Emile Argand Conference on Alpine Geological Studies, 12-14 September 2022, Ljubljana, Slovenia. Anagolay: the shape of the Philippines and the Luzon Syntaxis John Milsom1 and Jenny Anne Barretto2 1Gladestry Associates, Preseigne, UK (gladassoc@btinternet.com) 2GNS Science, 1 Fairway Drive, Avalon 5010, PO Box 30-368, Lower Hutt, New Zealand The India-Asia collision can have only a limited role as an the anomalous features of the Philippines can be attributed to actualistic model for the closure of Western Tethys and the this cause. A sharp bend in topographic trends involving most subsequent Alpine orogenies because the impacting margins of the southern part of the island of Luzon is here interpreted appear to have been sub-parallel and rather regular and the as a consequence of the impact on the east-facing subduction intervening ocean seems to have contained few volcanic zone of the Anagolay volcanic massif formed by hot-spot volca-edifices or continental fragments. A better guide to possible nism associated with the spreading ridge in the West Philippine pre-collision processes is provided by the incipient Australia – Basin. This bend can be considered a small-scale analogue of Southeast Asia collision, which has already proved its worth the syntaxes that define the limits of the India-Asia collision as a key area for the study of small extensional zones within and demonstrates the way in which the presence of even a overall compressional environments. Insights into the possible relatively small region of thickened crust can influence the roles of ridge-related features during oceanic closure are now morphology of an entire collision zone. Similar processes must being obtained from studies in the northern part of the Phil- have operated in other Alpino-type orogenic belts but may be ippines Archipelago, which was largely formed by post-Middle hard to recognise because the generative units are no longer Cretaceous volcanic activity associated with subduction of oce- observable and their effects may be partly concealed by later anic crust from both east and west. Double-sided subduction tectonic over-printing. inevitably produces geomorphological complexity, but not all 45 15TH WORKSHOP Abstract book. 15th Emile Argand Conference on Alpine Geological Studies, 12-14 September 2022, Ljubljana, Slovenia. Quartz and zircon in garnet elastic geobarometry of HP rocks from the Sesia Zone Giulia Mingardi1, Mattia Gilio1, Francesco Giuntoli2, Kira A. Musiyachenko3 and Matteo Alvaro1 1University of Pavia, Department of Earth and Environmental Sciences, Pavia, Italy (giulia.mingardi02@universitadipavia.it) 2Department of Biological, Geological, and Environmental Sciences, Università degli Studi di Bologna, Bologna, Italy 3Department of Earth, Ocean and Atmospheric Sciences, University of British Columbia, Vancouver, Canada The Sesia zone is a rifted portion of the Adriatic Margin that EC. Entrapment P obtained for the quartz inclusions in garnet subducted to high-pressure conditions during the Alpine Orog- in the IC range from 1.5-2 GPa at 600-650 °C, in agreement eny. It consists of two main complexes: the Internal Complex with the P-T estimates determined through thermodynamic (IC) and the External Complex (EC). The IC is made up of modelling. Coupled quartz and zircon in garnet geobarometry polymetamorphic micaschists, eclogites, and orthogneisses in the garnet-orthogneiss from the EC also display P-T condi-equilibrated at eclogite facies conditions; the EC consists of tions of 1.8 GPa and 650 °C. These estimates disagree with the alpine monometamorphic orthogneiss with minor paragneiss greenschist facies mineral assemblage of the rock (Ttn + Grt + and quartzites metamorphosed at epidote blueschist facies Phg + Chl) and with the results of thermodynamic modelling conditions and intensely retrogressed at greenschist facies con- for the garnet-bearing assemblage (0.6-0.8 GPa and 500 °C). ditions. The question is therefore to understand if we can trace The misfit in P-T estimates between elastic geobarometry and the Alpine metamorphic history through methods that do not thermodynamic modelling might be due to an elastic reset of rely only on chemical equilibration. the quartz and zircon host-inclusion pairs at HP conditions. The use of coupled elastic geobarometry and thermodynamic To tackle this objective, we used elastic geobarometry to derive modelling can help to unravel complex tectonometamorphic pressure and temperature (P-T) conditions reached by three histories. micaschists from the IC and one garnet-orthogneiss from the 46 15TH WORKSHOP Abstract book. 15th Emile Argand Conference on Alpine Geological Studies, 12-14 September 2022, Ljubljana, Slovenia. How active is recent tectonics in the central Balkans: Evidence from the Serbian Carpatho-Balkanides Ana Mladenović University of Belgrade - Faculty of Mining and Geology, Belgrade, Serbia (ana.mladenovic@rgf.bg.ac.rs) Since the Late Cretaceous, after closure of the Neotethys fault), that accommodated up to 100 km of cumulative dis-ocean, tectonic processes in the central Balkan Peninsula were placement. According to earthquake focal mechanisms, faults mainly controlled by the mutual interaction of the Adriatic and belonging to these fault systems are still active. the Eurasian plates, and tectonic units in-between. Most of the tectonic structures that have been active during Cenozoic times In this contribution we present new data about the youngest were inherited from previous tectonic stages under different and recently active faults in the area of the Carpatho-Balka-tectonic regimes. nides in eastern Serbia, based on the studies of fault kinemat- ics, seismicity and earthquake focal mechanisms, as well as Tectonic activity within the Carpatho-Balkan orogen in eastern tectonic geomorphological studies in karst caves. Results show Serbia since Miocene is conditioned by the existence of the rig- that the research area is primarily characterized by strike-slip id Moesian promontory east of the research area, which limited tectonics, which most likely results from far-field stress gener-thrusting of the Carpatho-Balkan units. Rather than that, fur- ated by the Adria-push mechanism. However, the stress field ther compression and complex rotations around the Moesian is highly heterogeneous, with local areas of transtension and promontory have been accommodated by the formation of transpression that have also been important in controlling the the large strike-slip fault systems (e.g. Cerna-Jiu fault, Timok recent fault kinematics in this part of the Carpatho-Balkanides. 47 15TH WORKSHOP Abstract book. 15th Emile Argand Conference on Alpine Geological Studies, 12-14 September 2022, Ljubljana, Slovenia. Partial drowning or backstepping of the Early Norian Dachstein Carbonate Platform in the Dinarides (Poros, Montenegro) Milica Mrdak1,2, Hans-Jürgen Gawlick2, Nevenka Đerić1, Martin Đaković3, and Milan Sudar4 1University of Belgrade, Faculty of Mining and Geology, Belgrade, Serbia (mrdak.milica@yahoo.com) 2Montanuniversität Leoben, Department Applied Geosciences and Geophysics, Leoben, Austria 3Geological Survey of Montenegro, Podgorica, Montenegro 4Serbian Academy of Sciences and Arts, Belgrade, Serbia In the Dinarides the reef rim to the open marine deep-water to Sevatian (with E. bidentata) is characterized by a thick series depositional realm (outer shelf) of the Late Triassic Dachstein of slump deposits with carbonate turbidite intercalations. Up-Carbonate Platform is not known. On the road from Gradac section follow polymictic breccias (debris flows) and carbonate to Šula near to the village Poros a more than 120 m thick far turbiditic microbreccias with older open-marine hemipelagic travelled and overturned Late Triassic succession of reefal components, as proven by conodonts. The overlying dm-bed-to bedded siliceous limestones was studied (biostratigraphy, ded grey-reddish siliceous limestones with red chert nodules microfacies). The section is slightly tectonic overprinted, with are Rhaetian in age dated by the appearance of M. hernsteini. slump deposits in the central and upper part. Upsection 5-10 cm-bedded grey siliceous and slightly marly limestones (in a thickness of less than 20 m) follow, overlain The section starts with a roughly 20 m thick reefal to fore-reef- by roughly 10 m thick dm-bedded red-grey siliceous limestones al limestone succession with deep-water matrix in the upper with red marl to claystone intercalations, in the lower part with part (Lacian 2 in age with following conodonts: Epigondolel- slump deposits, again overlain by 5-10 cm-bedded grey sili-la. rigoi, E. abneptis). Near the base the reefal limestones is ceous and slightly marly limestones. An exact age of this part think-bedded to massive (rudstones), higher up in the section of the series could not be determined, only conodont multiele-various bedded. We attribute these fore-reefal limestones as ments could be isolated from this part of the succession. The part of the Late Triassic Dachstein Limestone, interestingly with age is most likely Rhaetian 2-3, but earliest Jurassic for highest a deepening upward sequence from the middle Lower Norian parts of the sequence cannot be excluded. onwards. Around the Lacian 2-3 boundary the depositional characteristics changed relatively abrupt from reefal- rudstones The higher Lacian to Late Norian part of the succession cor-to bedded siliceous limestones intercalated by few and turbid- responds to the reef-near facies belt in open shelf position, ite layers containing shallow-water debris. The next, 30 m thick known in the type-area in the Northern Calcareous Alps as part of the succession consists of dm-bedded limestones with Gosausee Limestone facies. However, the section Poros shows chert nodules and layers, grey limestones and reddish lime- during the Norian a general deepening trend during the time stones (radiolarian-filament wackestones), in parts with slump span Lacian 3 to the end of the Rhaetian opposite of the well-intercalations or medium-grained microbreccias. Conodont known platform margin in the Northern or Southern Alps. In dating show that the age of this part of the section is Lacian 3 the Dinarides a backstepping of the reef belt in the late Early to Alaunian 1-2 in the upper part (dated by E. spatulata to E. Norian result in a drowning unconformity of the Early Norian slovakensis) probably reaching the Alaunian 3. The Alaunian 3 part of the long-living Dachstein Carbonate Platform. 48 15TH WORKSHOP Abstract book. 15th Emile Argand Conference on Alpine Geological Studies, 12-14 September 2022, Ljubljana, Slovenia. New data on the Late Pleistocene evolution of the Klagenfurt Basin, Austria Mark Mücklisch1, Christoph Grützner1, Erick Prince1, Sumiko Tsukamoto2 and Kamil Ustaszewski1 1Friedrich-Schiller University Jena, Institute for Geological Sciences, Jena, Germany (mark.muecklisch@uni-jena.de) 2Leibniz Institute for Applied Geophysics, Hanover, Germany The Klagenfurt Basin in the southern Austrian region of models to scan the area for postglacial deformation but found Carinthia was glaciated during the Last Glacial Maximum no conclusive evidence for tectonic activity since the Würm (LGM). Next to numerous lakes, the present-day landscape glaciation. We then analysed several outcrops of Late Pleisto-predominantly exhibits landforms such as moraines and large cene sediments throughout the Klagenfurt Basin to check for river terraces systems. These landforms can be seen as markers soft-sediment deformation features that could be linked to for post-LGM tectonics: If they are deformed, the basin has strong seismic shaking. These outcrops were documented as 3D taken up a share of the ~N-S shortening prevailing due to the virtual models. Deformed silty-sandy layers were encountered ongoing collision of Adria and Europe. If the landforms are in several places, and one outcrop showed spectacularly folded undeformed, this deformation is accommodated elsewhere, fluvial gravels. However, we do not need to invoke tectonics as most likely further south along the Periadriatic and Sava Fault the causative mechanism. Instead, we interpret these structures system or by a NW-SE-trending strike-slip fault system at the as evidence for a late glacial advance. Luminescence dating is junction between Southern Alps and Dinarides in Slovenia. Our underway to put constraints on the timing of this event. Our study is motivated by the recent discovery of earthquake-trig- study implies that although there are records for recent strong gered mass movements in Carinthian lakes and new data on earthquakes around the Klagenfurt Basin, the rates of deforma-Late Pleistocene-Holocene speleothem damage in the Karawan- tion are so low that they can not be detected in the post-LGM ken mountains, illustrating that the area is seismically active. landscape. We used newly available high-resolution digital elevation 49 15TH WORKSHOP Abstract book. 15th Emile Argand Conference on Alpine Geological Studies, 12-14 September 2022, Ljubljana, Slovenia. Nappe stacking and syn-nappe folding in the northern Dora-Maira Massif (Western Alps) Francesco Nosenzo1, Michel Ballèvre2, and Paola Manzotti1 1Stokholm University, Department of Geological Sciences, Sweden (francesco.nosenzo@geo.su.se) 2Université de Rennes, Géosciences Rennes, Rennes, France The internal structure of the Dora-Maira Massif is of key 324 Ma (U-Pb LA-ICP-MS on monazite inclusions in garnet) is importance for understanding exhumation mechanisms of well preserved in undeformed volumes (Nosenzo et al., 2022). continental-derived HP-UHP rocks in the Western Alps. Nu- A new, colder (garnet + Fe-rich chloritoid +coesite), UHP unit merous petrologicalgeochemical studies have been done on (the Chasteiran Unit) has been discovered (Manzotti et al., the world-famous UHP Brossasco-Isasca Unit in the southern 2022 and this meeting). This Unit, located in the immediate Dora-Maira Massif, and recent syntheses have provided an hangingwall of the Pinerolo Unit, occupies the same structural updated view of its metamorphic (Groppo et al., 2019) and position than the UHP Brossasco-Isasca Unit, but records tem-structural (Michard et al., 2022) history. By contrast, the north- peratures 200 °C lower. ern Dora-Maira Massif has been much less explored. We are presently undertaking a multidisciplinary project aimed at bet- Geological mapping, structural data, and petrological investi-ter constraining its geometry and history. We studied in detail gations provide new constraints on the geometry and kinemat-an area comprised between the Germanasca and the Chisone ics of this part of the Dora-Maira Massif. The main foliation D1 rivers. The first results are as follows: developed at different peak PT conditions in the different units. The nappe stack comprises, from bottom to top, the Pinerolo During their stacking, a new foliation D2 developed associated (Carboniferous metasediments intruded by dioritic and granitic with kilometer-scale, E-W trending folds. Final doming of the plutons), Chasteiran (UHP), Muret (polycyclic unit, made of Dora-Maira nappe stack (D3) is associated to the westward a Variscan basement overprinted during Alpine HP metmor- displacement of the Adria mantle indentor. Detailed geological phism) and Serre (Permian rhyolitic to granitic rocks, and the maps and cross-sections will be provided for illustrating the associated epiclastic rocks; slices of Mesozoic cover) Units. The main steps of the history. pre-Alpine history of the Muret Unit (6-7 kbar, 650 °C) dated at Groppo, C., Ferrando, S., Gilio, M., Botta, S., Nosenzo, F., Balestro, G., Festa, A., & Rolfo, F. (2019). What’s in the sandwich? New P–T constraints for the (U)HP nappe stack of southern Dora-Maira Massif (Western Alps). European Journal of Mineralogy, 31, 665–683. Michard, A., Schmid, S.M., Lahfid, A., Ballèvre M., Manzotti, P., Chopin, C., Iaccarino, S., Dana, D. (2022). The Maira-Sampeyre and Val Grana Allochthons (south Western Alps): a review and new data on the tectonometamorphic evolution of the Briançonnais distal margin. Swiss Journal of Geosciences, 115, in press. Manzotti, P., Schiavi, F., Nosenzo, F., Pitra, P., Ballèvre, M. (2022). A journey towards the forbidden zone: a new, cold, UHP unit in the Dora-Maira Massif (Western Alps). Contributions to Mineralogy and Petrology, 117, article 59. https://doi.org/10.1007/s00410-022-01923-8 Nosenzo, F., Manzotti, P., Poujol, M., Ballèvre, M., & Langlade, J. (2022). A window into an older orogenic cycle: P-T conditions and timing of the pre-Alpine history of the Dora-Maira Massif (Western Alps). Journal of Metamorphic Geology, 40, 789-821. 50 15TH WORKSHOP Abstract book. 15th Emile Argand Conference on Alpine Geological Studies, 12-14 September 2022, Ljubljana, Slovenia. Exhumation response to climate and tectonic forcing in the southern Patagonian Andes (Torres del Paine and Fitz Roy plutonic complexes) Veleda Astarte Paiva Muller1, Christian Sue2, Pierre Valla2, Pietro Sternai1, Thibaud Simon-Labric3, Cécile Gautheron2, Joseph Martinod2, Matias Ghiglione4, Lukas Baumgartner5, Fréderic Hérman5, Peter Reiners6, Djordie Grujic7, David Shuster8, Jean Braun9, Laurent Husson2 and Matthias Bernet2 1Università degli Studi di Milano-Bicocca, Earth and Environmental Sciences, Milan, Italy (v.paivamuller@campus.unimib.it) 2Institute des Sciences de la Terre (ISTerre), Université Grenoble Alpes - Savoie Mont Blanc, CNRS, IRD, IFSTTAR, Grenoble - Chambéry, France 3Centre de Géologie Oisans Alpes, Musée des Minéraux, 38520 Bourg-d’Oisans, France 4Instituto de Estudios Andinos “Don Pablo Groeber”, Universidad de Buenos Aires, CONICET, Buenos Aires, Argentina 5Institut des Sciences de la Terre (ISTE), Université de Lausanne, CH-1015 Lausanne, Switzerland 6Geosciences University of Arizona, Tucson, USA 7Department of Earth and Environmental Sciences, Dalhousie University, Halifax, Canada 8Earth and Planetary Science, University of California – Berkeley, USA 9Helmholtz-Zentrum Potsdam, University of Potsdam, Potsdam, Germany Alpine landscapes form in mountain belts that likely experi- inversion numerical modeling, to identify the geodynamic pro-enced tectonic uplift during plate’s convergence, and efficient cesses forcing on the exhumation of the mountain belt. These erosion dominated by glacial carving and circle retreat. In complexes are separated by 200 km along the strike of the belt, southern Patagonia N-S oriented late Miocene plutonic com- and share a pulse of rapid exhumation at ca. 6 Ma, likely show-plexes are exposed in deep incised valleys with summits topo- ing that glaciation was regionally starting at this moment. After graphically above the glacial equilibrium line altitude. Two of a period of quiescence, in Torres del Paine the exhumation rate the most emblematic ones are the Fitz Roy (Chaltén, latitude is accelerated from ~2 Ma to the present, interpreted as a sig-49 °S) and the Torres del Paine (latitude 51 °S) plutonic com- nal of the Pleistocene climatic transition creating incise valleys. plexes, ~2 km higher than the mostly flat bottom valley that Only in the Fitz Roy a pulse of rapid exhumation is present at is partially covered by the Southern Patagonian Icefield. This ca. 10 Ma, approximately coincident with the time range in continental region is located above an asthenospheric window which the ridge was subducting beneath the continent at that that opens and migrates from the latitude 54 °S towards the latitude. This allows us to separate the climatic from the tec-latitude 46 °S since ~16 Ma, and experienced dynamic uplift tonic/mantle forcing to the exhumation in southern Patagonia, during episodes of spreading ridge collision with the conti- and represents the first in-situ observation of the passage of the nental margin. Here we present a new dataset of combined asthenospheric window in the lowtemperature thermochrono-low-temperature thermochronometers from the Chaltén and metric record of the region. Torres del Paine plutonic complexes, and their thermal history 51 15TH WORKSHOP Abstract book. 15th Emile Argand Conference on Alpine Geological Studies, 12-14 September 2022, Ljubljana, Slovenia. Discovery of sheath folds in the Adula nappe and implications for the tectonic evolution (Central Alps) Michele Perozzo1, Matteo Maino1, Filippo Schenker2, and Silvio Seno1,2 1Department of Earth and Environmental Sciences, University of Pavia, Pavia, Italy (michele.perozzo01@universitadipavia.it) 2University of Applied Sciences and Arts of Southern Switzerland (SUPSI), Institute of Earth Sciences, Mendrisio, Switzerland Orogenic deformation patterns show intricate overprinting a recognition of sheath folds from the central part of the Adula and structural relations, variations of style and orientation of nappe, the largest high-pressure nappe of the Central Alps. folds and sense of shear, which are traditionally interpreted as We performed detailed geological mapping (scale 1:10000) due to polyphase deformation, i.e. distinct deformation phases and structural characterization of the spectacular outcrops of separated by periods of tectonic quiescence. The Adula nappe the Piz de Cressim glacial cirque. Here a large antiform is de-in the Central Alps displays exceptional exposures of complex scribed as the main structure classically associated with the D3 internal structures involving heterogeneous rocks (meta-pelitic backfolding phase. We show that the meso/leucocratic hetero-and meta-granitic gneisses, micaschists, amphibolites, eclog- geneous rocks (orthogneisses, micaschists, migmatitic gneisses, ites, minor quartzites and limestones). The Adula structures amphibolitic lenses) form highly non-cylindrical folds. Sheath are distinguished through the style and the orientation of folds, folds are highlighted by several cm to km scale omega and ellip-schistosity and the observation of refolded folds. Structural tical eye-structures in cross sections perpendicular to the shear features show a great variability within the unit, making the direction (yz plane). Local variations of style and orientation of structures along the nappe difficult to correlate. However, the folds and sense of shear are easily explained by the three-dimen-Adula deformation patterns are classically interpreted as gener- sional structure of the sheath folds. All lithological units show ated by multiple, distinct deformation phases (five deformation one penetrative foliation and a related stretching lineation with phases; D1-5), despite only one schistosity and lineation may variations in orientation. We suggest that the Cressim antiform be clearly recognized in the field. Kinematic indicators indicate formed during a progressive, highly non-cylindrical folding dominant top-to-N sense of shear, although local top-to-S shear under top-to-N deformation accomplished within rheological is interpreted as developed during the D3 backfolding phase heterogeneous rocks. (e.g. Löw, 1987; Nagel, 2008). In this contribution, we show Löw S. (1987). Die tektono-metamorphe Entwicklung der Nördlichen Adula-Decke (Zentralalpen, Schweiz). Materiaux pour la Carte Geologique de la Suisse, N.S. , 161, 84. Nagel T. (2008). Tertiary subduction, collision and exhumation recorded in the Adula nappe, central Alps. In: Siegesmund S, Fu¨genschuh B,- Froitzheim N (Eds) Tectonic aspects of the Alpine–Dinaride–Carpathian system (special publications 298, 365–392). Geological Society of London. 52 15TH WORKSHOP Abstract book. 15th Emile Argand Conference on Alpine Geological Studies, 12-14 September 2022, Ljubljana, Slovenia. Lower to Middle Jurassic clastic formations of the Western Carpathian Klippen Belt: testimony to the rifting-breakup- drifting Processes Dušan Plašienka, Marína Molčan Matejová, and Tomáš Potočný Comenius University, Faculty of Natural Sciences, Dept. Geology and Palaeontology, Slovakia (dusan.plasienka@uniba.sk) The Lower to early Middle Jurassic terrigenous clastic depos- black shales representing the Toarcian oceanic anoxic event. its witness the early breakup processes of Pangaea. Rifting Deposition of oxygen-depleted black shales continued into and subsequent ocean-floor spreading of the Central Atlantic the Aalenian and early Bajocian as the Szlachtowa Fm., which branch that propagated eastward into the Alpine–Carpathian is characteristic of the Šariš Unit. In addition to micaceous realm split several continental blocks (Adria, Tisia, Dacia, Moe- black shales with common imprints of pelagic bivalves of Bos-sia), and smaller intervening fragments (such as Cervinia and itra buchi, it comprises also beds of black turbiditic siliciclastic Oravic), off the southern European plate margin. Alongside the sandstones rich in white mica flakes and few allochthonous ocean-facing margins of Europe and drifting blocks, the initial coal seams. Black shales with pelocarbonate nodules out of rifting phases are recorded by terrigenous terrestrial fluvi- the reach of turbiditic currents are identical with the concom-al-limnic, deltaic to open marine clastic formations. Although itant Skrzypny Fm. recognized also in the successions of the showing some regional variations in composition and age, they Subpieniny Nappe. Beds of calciturbiditic crinoidal limestones share many common developmental characteristics. occurring in the upper part of the formation indicate input of shallow-marine bioclastic material derived from the adjacent In the Carpathian Pieniny Klippen Belt (PKB), the Lower – Czorsztyn Ridge uplifted during the middle–late Bajocian. Sub-early Middle Jurassic clastics are partly preserved in the Šariš sequent latest Bajocian hiatus and drowning of the Czorsztyn (Grajcarek) Unit that was derived from the outer (northern) Ridge, along with a sudden decline of clastic input in the Šariš margin of the continental ribbon surrounded by the Pennine Basin, are interpreted as the breakup phase of a nearby oceanic oceanic branches. Palaeogeographically, this continental zone. splinter is known as the Czorsztyn Ridge and its detached Ju- rassic–Eocene sedimentary nappes are designated as the Oravic The post-breakup pelagic succession represents the drifting tectonic units (Šariš, Subpieniny and Pieniny). stage and consists of the late Middle–Upper Jurassic dark, calcite-poor siliceous shales, red ribbon radiolarites, red marl- The Šariš sedimentary succession related to the incipient rifting stones and cherty limestones, followed by the Lower Creta-stage begins with massive quartzitic sandstones of probably ceous spotted micritic limestones with cherts, mid-Cretaceous Hettangian age deposited in continental to shallow-marine en- Fleckenmergel and dark silicitic shales and Upper Cretaceous virons. The mature rifting stage is represented by quartz-calcar- red calcite-free claystones. Finally, the synorogenic phase is reeous, partly turbiditic sandstones rich in imprints of Sinemu- corded by the Maastrichtian–Paleocene calcareous flysch with rian ammonites intercalated by thin layers of grey shales. olistostrome bodies and limestone megaolistoliths derived from Overlying spotted marlstones of the Fleckenmergel facies of the overriding Subpieniny Nappe. the Pliensbachian–Toarcian Allgäu Fm. are locally passing into 53 15TH WORKSHOP Abstract book. 15th Emile Argand Conference on Alpine Geological Studies, 12-14 September 2022, Ljubljana, Slovenia. The thermotectonic evolution in front of the Dolomites Indenter Hannah Pomella1, Thomas Klotz1, Anna-Katharina Sieberer1, Martin Reiser2, Peter Tropper3 and Ralf Schuster2 1University of Innsbruck, Institute of Geology, Innsbruck, Austria (hannah.pomella@uibk.ac.at) 2Geologische Bundesanstalt, Neulinggasse 38, Wien, Austria 3University of Innsbruck, Institute of Mineralogy and Petrography, Innsbruck, Austria The Adriatic Indenter is subdivided into a western and an Fission track data from the western Tauern Window and the eastern domain termed Canavese-Insubric Indenter and Dolo- Austroalpine units adjacent to the north-western corner of the mites Indenter, respectively, and offset for ~75 km from late DI, indicate cooling below 180-200 °C (Zircon Fission track Oligocene onwards by the NNE-SSW-trending sinistral-trans- data) in the Early Miocene and below the 100-120 °C (Apatite pressive Giudicarie fault system (GFS). The N(NW)-directed Fission track data) in the Late Miocene (Klotz et al., 2019). movement of the Dolomites Indenter (DI) modifies the early (U-Th)/He on Apatite data, derived from a horizontal section Cenozoic nappe structure of the Alpine orogen as the accom- of the Brenner Base Tunnel and reaching from the DI into the modated shortening changes substantially, depending on the Austroalpine nappe stack, indicate continuous differential oblique shape of the indenter and its counter-clockwise rota- uplifting of the northern block along the, in this area, approxi-tion. The Austroalpine basement units northwest of the GFS mately E-W striking Periadriatic fault system until the Pliocene experienced open folding of the Cretaceous nappe stack and (Klotz et al., 2019). preserved Cretaceous metamorphic ages. In contrast, the pre- viously deep-seated Neoalpine metamorphic Subpenninic and Earthquake focal solutions and satellite-based geodetic stud-Penninic units of the Tauern Window in front of the DI’s tip ies show, that indentation is ongoing today. The significant are exhumed and the Austroalpine units adjacent to the DI are present-day seismotectonic activity concentrates in the Friuli brought into a subvertical or even overturned position. area in the southeast, whereas there is currently no significant seismicity along the western and northern boundaries of the The combination of several thermochronological methods DI or in the northerly adjacent Austroalpine basement and the and structural field work allows for constraining time on this Tauern Window. Increased seismic activity can only be detected tectonic evolution: The Austroalpine units directly adjacent to north of the Tauern Window, along, and north of the Inn Valley the DI belong to the uppermost nappe system of the Eoalpine (Reiter et al., 2018). Based on field evidence and the thermo-orogeny (Drauzug-Gurktal Nappe System) and experienced chronological record, the recent seismic distribution indicates an anchizonal to lowermost greenschist-facies metamorphic an important change in style and localisation of deformation overprint during the Alpine orogeny resulting in an only par- compared to what is documented from the past. tial reset of Variscan Rb/Sr Biotite ages (Pomella et al., 2022). Klotz, T., Pomella, H., Reiser, M., Fügenschuh, B., Zattin, M. (2019). Differential uplift on the boundary between the Eastern and the Southern European Alps: Thermochronologic constraints from the Brenner Base Tunnel. Terra Nova .31, 281-294. Pomella, H., Costantini, D., Aichholzer, P., Reiser, M., Schuster, R., Tropper, P. (2022). Petrological and geochronological investigations on the individual nappes of the Meran-Mauls nappe stack (Austroalpine unit/South Tyrol, Italy). Austrian Journal of Earth Sciences, 115, 15-40. Reiter, F., Freudenthaler, C., Hausmann, H., Ortner, H., Lenhardt, W., Brandner, R. (2018). Active seismotectonic deformation in front of the Dolomites indenter, Eastern Alps. Tectonics, 37, 4625-4654. 54 15TH WORKSHOP Abstract book. 15th Emile Argand Conference on Alpine Geological Studies, 12-14 September 2022, Ljubljana, Slovenia. Calcite microstructures recording polyphase deformation history of the Meliata Unit Tomáš Potočný and Dušan Plašienka Comenius University Bratislava, Faculty of Natural Sciences, Department of Geology and Paleontology, Slovakia (potocny9@uniba.sk) The geological structure of the Western Carpathians is very large calcite grains and microstructure pointing to the Grain complicated and is result of several deformation phases. The Boundary Migration deformation mechanism, which suggests Meliata Unit (Meliaticum) as a significant part of the Western the higher temperature during dynamic recrystallization. Carpathians proves existence of substantial tectonic move- The higher temperature is also proven by character of twin ments. The Meliata Unit incorporates the Permian to Jurassic lamellas. The GI microstructures are related to the subduction blueschists-facies Bôrka Nappe and the Jurassic low-grade processes after closure of the Meliata Ocean and exhumation of mélange complexes with huge Triassic olistostrome bodies – the high-pressure complexes. The second group (GII) is char-the Meliata Unit s.s. Based on microstructural characteristics, acterised by a significant grain size reduction and strong shape the calcite is one of the most suitable minerals for study of preferred orientation and thus with development of calcitic deformation history. Calcitic metacarbonates are common el- mylonite zones. They are related to forming of the Meliatic ements of subduction-accretionary complexes and thus also a accretionary wedge. The third group (GIII) shows completely considerable element in rock composition of the Meliata Unit. recrystallized microstructure of relatively uniform calcite Samples were taken from various Meliatic complexes either grain size with sharp edges of grains. They were recrystallized within the Bôrka Nappe, or as olistoliths embedded in the in an annealing regime due to higher temperature gradient Jurassic mélange. Variations in deformation microstructures generated by a shallow granitic intrusion associated with the are clearly visible in sampled metacarbonates, what was main exhumation of the underlying Veporic metamorphic dome. The aspect to separate them into groups reflecting different P/T last deformation phase is marked by the bulging deformation conditions. The distinguished groups more-or-less correspond mechanism, thus to a partial replacement of primary grains by to their regional occurrences and grade of metamorphosis of newly formed fine-grained calcites and represent final stages of surrounding rocks. The first group (GI) contains relatively nappe emplacement. Acknowledgements: Financial support from the Slovak Research and Development Agency (project APVV-17-0170) and from the Grant Agency for Science, Slovakia (project VEGA 1/0435/21) is gratefully appreciated. 55 15TH WORKSHOP Abstract book. 15th Emile Argand Conference on Alpine Geological Studies, 12-14 September 2022, Ljubljana, Slovenia. Finding Quaternary Seismogenic Activity Along the Eastern Periadriatic Fault System: Dating of Fault Gouges via Electron Spin Resonance Erick Prince1, Sumiko Tsukamoto2, Christoph Grützner1, Marko Vrabec3, and Kamil Ustaszewski1 1Friedrich-Schiller University Jena, Institute of Geological Sciences, Structural Geology & Tectonics, Jena, Germany (erick.prince@uni-jena.de) 2Leibniz-Institut für Angewandte Geophysik - LIAG Hannover, Germany 3University of Ljubljana, Faculty of Natural Sciences and Engineering, Department of Geology, Ljubljana, Slovenia The Periadriatic Fault System (PAF) is among the most import- activity at near-surface conditions due to its dating range ant post-collisional structures of the Alps; it accommodated (~104 - ~106 years) and low closing temperature (< 100 °C). between 150-300 km of right-lateral strike-slip motion between During our field campaigns, we acquired structural data and col-the European and Adriatic plates from about 35 until 15 Ma. lected 19 fault gouge samples from 15 localities along the PAF, The scarcity of instrumental and historical seismicity on the the Labot/Lavanttal Fault, and the Šoštanj Fault. We measured easternmost segment of the PAF is intriguing, especially when the ESR signals from the Ti and Al centers following the ad-compared to nearby structures in the adjacent Southern Alps. ditive and regenerative protocols on 60 mg aliquots of quartz, Through this project, we aim to show which segments of the and compared the measurements between different grain size PAF accommodated seismotectonic deformation during the fractions. Here, we present our preliminary results from select-Quaternary by applying Electron spin resonance (ESR) dating ed localities, suggesting Quaternary earthquake activity along to fault gouges produced by this fault system. The method is the studied part of the PAF. especially useful for dating shear heating during earthquake 56 15TH WORKSHOP Abstract book. 15th Emile Argand Conference on Alpine Geological Studies, 12-14 September 2022, Ljubljana, Slovenia. Formation of esseneite and kushiroite in calc-silicate skarnoid xenoliths from Southern Slovakia Luca Reato1, Monika Huraiová1, Patrik Konečný2 and Vratislav Hurai3 1Comenius University in Bratislava, Faculty of Natural Sciences, Department of Mineralogy, Petrology and Economic Geology, Slovakia (reato1@uniba.sk) 2State Geological Institute of Dionýz Štúr, Department of Special Laboratories, State Geological Institute of Dionýz Štúr, Mlynská Dolina 1, 817 04 Bratislava, Slovakia 3Institute of Earth Sciences, Slovak Academy of Sciences, Dúbravská Cesta 9, 840 05 Bratislava, Slovakia Skarnoid calc-silicate xenoliths composed of anorthite, clino- ary calculated for a CO saturated environment using Perple_X 2 pyroxene and Mg-Al spinel were discovered in an alkali basalt (Connolly, 1990). Tschermakite touching interstitial plagioclase quarry located in the Belinsky vrch lava flow, near Fiľakovo was suitable for the application of the barometer of (Molina (Southern Slovakia). Randomly oriented tschermakite pseu- et al., 2021), which yielded 781±13 °C and 2.05±0.03 GPa domorphs are replaced by olivine, spinel, and plagioclase. consistent with the olivineilmenite-calcite-aragonite thermo-The relict amphibole within the pseudomorphs is character- barometry. The estimated PT conditions fall well inside the ized by high VIAl (1.95 to 2.1 apfu), and very low occupancy garnet stability field, although no garnet has been observed in of the A-site (< 0.1 apfu), which are a diagnostic feature of the mineral assemblage. However, the presence of esseneite highpressure metamorphic rocks. Pyroxene compositions plot and kushiroite with melilite inclusions suggest high CO partial 2 along continuous mixing line extending from nearly pure di- pressure, low SiO activity and strongly oxidizing conditions, 2 opside-augite towards a Ca(Fe3+Al)AlSiO endmember with an in which the high Al, Fe pyroxenes are formed at the expense 6 equal proportion of VIAl3+ and Fe3+. Forsterite (Fo72–83) and of the garnet (Ohashi and Hariya, 1975). The protolith is still Fe3+-rich ilmenite crystallized from the melt, leaving behind the ambiguous, and two options have been considered. The relict residual calcic carbonate with minor MgO (1–3 wt%). Euhedral tschermakite in spinel-plagioclase-forsterite pseudomorphs aragonite and apatite embedded in the fine-grained calcite or suggests a metamorphosed calc-silicate marble originating aragonite groundmass indicate slow crystallization of residual from a sedimentary protolith. High Cr contents in spinel and carbonatite around the calcite-aragonite stability boundary. pyroxene, abundant Cu-sulfides, and high CaO contents, Olivine-ilmenite thermometry (Andersen and Lindsley, 1981) 0.3–1.0 wt% CaO, in forsterite, suggest a magmatic protolith, yielded temperatures between 770 and 860 °C. Pressures of similar to layered gabbro-anorthosite complexes modified by 1.8–2.1 GPa were estimated by intersection of the olivine-il- interaction with calcic carbonatite melt. menite thermometer with the calcite-aragonite stability bound- Andersen, D., & Lindsley, D. (1981). A valid Margules formulation for an asymmetric ternary solution: revision of the olivine-ilmenite thermometer, with applications. Geochimica et Cosmochimica Acta, 45(6), 847–853. Connolly, J. (1990). Multivariable phase diagrams; an algorithm based on generalized thermodynamics. American Journal of Science, 290(6), 666–718. Molina, J., Cambeses, A., Moreno, J., Morales, I., Montero, P., & Bea, F. (2021). A reassessment of the amphibole-plagioclase NaSi-CaAl exchange thermometer with applications to igneous and highgrade metamorphic rocks. American Mineralogist, 106(5), 782–800. Ohashi, H., & Hariya, Y. (1975). Phase relation of CaFeAlSiO6 pyroxene at high pressures and temperatures. The Journal of the Japanese Association of Mineralogists, Petrologists and Economic Geologists, 70(3), 93–95. 57 15TH WORKSHOP Abstract book. 15th Emile Argand Conference on Alpine Geological Studies, 12-14 September 2022, Ljubljana, Slovenia. Age and structure of the Stubai Alps (Ötztal-Nappe, Tyrol/Austria) Martin Reiser1, Christoph Iglseder1, Ralf Schuster1, David Schneider2 and Daniela Gallhofer3 1Department of Hard-Rock Geology, Geological Survey of Austria, Vienna, Austria (martin.reiser@geologie.ac.at) 2Department of Earth and Environmental Sciences, University of Ottawa, Ottawa, Canada 3Institute of Earth Sciences, University of Graz, Graz, Austria The Ötztal-Nappe in the central Eastern Alps represents a clas- associated with a pervasive axial plane foliation. Shearbands sical area of polyphase deformation and metamorphism. The dissecting the foliation indicate a top-NE directed shear sense, pre-Mesozoic basement (Ötztal-Stubai Complex; OSC) com- which probably correlates with post-Variscan exhumation. prises metasediments (paragneiss and mica schist), metaigne- Locally, the shearbands show a SE-directed overprint, which ous rocks and metabasites that experienced a polymetamorphic is attributed to Late Cretaceous extension in the course of the overprint during Ordovician, Variscan (Devonian to Carbonif- Eo-Alpine event. erous) and Eo-Alpine (Early/Late Cretaceous) events. In the Stubai Alps, basement rocks are unconformably overlain by a (Eo-)Alpine metamorphism of the Ötztal-Nappe, represented monometamorphic Permo-Triassic cover sequence (i.e. “Bren- by a southward increasing gradient from greenschist-facies ner-Mesozoic”), which truncates pre-Mesozoic structures and conditions in the northwest to epidote-amphibolite-facies allows discriminating pre-Alpine and (Eo-)Alpine structures. conditions in the southeast, led to a differential structural over- print. Ar-Ar white mica ages from the Stubai Alps yielding Mid- Ordovician metagranites (analysed using LA-ICP-MS U-Pb dle to Upper Pennsylvanian ages (post-Variscan cooling) and dating of zircon), deformed together with their metasedimen- “mixed” Variscan-to-Alpine ages reflect the metamorphic gradi-tary host rock, highlight the large-scale structure of the OSC. ent. Late Cretaceous ages from Rb-Sr analyses on biotite and During the Variscan event, metabasitic rocks of the central OSC (UTh)/He) zircon thermochronology provide time constraints underwent eclogite-facies metamorphism followed by an am- on large detachment faults that created several tectonic klip-phibolite-facies overprint. Two pre-Alpine fold generations can pen of Mesozoic rocks in the study area. These detachments be distinguished: i) NE-dipping fold axes of isoclinal folds over- formed in a general SE-directed extensional regime, which is printed by ii) subhorizontal NW-SE trending fold axes that are widely reported from Upper Austroalpine units. 58 15TH WORKSHOP Abstract book. 15th Emile Argand Conference on Alpine Geological Studies, 12-14 September 2022, Ljubljana, Slovenia. Architecture and sedimentary evolution of the Ladinian Kobilji curek Basin of the External Dinarids (Rute Plateau, central Slovenia) Boštjan Rožič1, Anja Kocjančič2, Luka Gale1,4, Tomislav Popit1, Petra Žvab Rožič1, Primož Vodnik3, Nina Zupančič1,2, Rok Brajkovič4 and Tea Kolar-Jurkovšek4 1Department of Geology, NTF, UL, Aškerčeva c. 12, 1000 Ljubljana, Slovenia (bostjan.rozic@ntf.uni-lj.si) 2Ivan Rakovec Paleontological Institute, ZRC SAZU, Novi trg 2, 1000 Ljubljana, Slovenia 3ELEA iC, Dunajska c. 21, 1000 Ljubljana, Slovenia 4Geological Survey of Slovenia, Dimičeva ul. 14, 1000 Ljubljana, Slovenia The largest Mesozoic paleogeographic perturbation of the istic sequences, separated by roughly N-S and E-W trending present-day Alpine-Dinaric transition zone occurred in the paleofaults. In the NW tectonic block (B1), the most basinal Ladinian. The entire area was subjected to intense tectonic ex- succession is outcropping with two intervals of platform car-tension related to the rifting of the Neotethys Ocean. The most bonates, while the sequence in the SE block (B4) is entirely intense subsidence occurred in the central part of this segment characterized by platform carbonates. In the transition blocks of the continental margin, and the area remained deep-marine (B2 and B3), platform carbonates predominate with minor ba- (called the Slovenian Basin) until the end of the Mesozoic. To sinal intervals. The entire Ladinian succession shows five major the south, extension also resulted in differentiation, but the subsidence pulses followed by partial or twice also complete predominant paleoenvironments were either continental (often platform progradation. The first subsidence is documented emerged areas) or shallow-marine. Locally, however, small- exclusively in B2 and B3 (F1 and F2), followed by platform scale, short-lasting, deep-marine environment also developed. progradation (F4). During the second subsidence, the major Herein we present the study of the Kobilji curek Basin in the paleofault between B1 and B2 is activated. This pulse is evi-Rute Plateau (central Slovenia, 25 km south of Ljubljana), dent in B1 as a fairly thick basinal succession (F1) containing where the Ladinian platform to basin transition has recently carbonate resediments (F3) in the upper part, indicating dis-been studied in detail. tant platform progradation. This pulse is also seen in B2 as thin deep marine limestones (F2 and F3), again followed by plat- The study includes sedimentological analysis, biostratigraphy, form carbonates (F4). The third pulse is seen in B1 as coarse mineralogical analysis, and detailed mapping. In the studied resediments (F3) followed by general platform progradation area, following Ladinian facies were outlined: F1 - deep ma- (F4), and in B2 as thin deep marine carbonates (F2 and F3) rine (volcano)clastic rocks (bentonitic clays, tuffitic sandstone, followed by platform carbonates (F4). This platform prograda-tuffs), F2 - hemipelagic limestone (micritic and filament lime- tion seals the paleofault between B1 and B2. The fourth pulse stone), F3 - resedimented limestone (breccia and calcarenite), is uniform in blocks B1 and B2 and consists of a continuous and F4 - shallow marine carbonates (bioclastic limestone and basinal interval (F1 and F2) followed by a final rapid platform dolomite) (for details see Kocjančič et al., this volume). The progradation (F4). The fifth subsidence is uniform in B1, B2, base is Anisian dolomite and the top Carnian clastites. In con- and B3 and begins with hemipelagic limestone (F2) followed trast, the highly variable Ladinian facies merge both laterally by (volcano)clastic rocks (F1) with some felsic extrusive rocks. and vertically. Detailed geological mapping revealed that the In B4, this pulse either did not occur or the rocks were eroded area can be divided into four tectonic blocks with character- during regional emersion in the early Carnian. 59 15TH WORKSHOP Abstract book. 15th Emile Argand Conference on Alpine Geological Studies, 12-14 September 2022, Ljubljana, Slovenia. From Permian to rift-inception: new insight from the Western Southern Alps (Varese Area) Emanuele Scaramuzzo1, Franz A. Livio1, and Maria Giuditta Fellin2 1University of Insubria, Department of Science and High Technology, via Valleggio 11, 22100 Como, Italy (escaramuzzo@uninsubria.it) 2ETH Zürich, Department of Earth Sciences, Clausiusstrasse 25, 8092 Zürich, Switzerland The Permian-Triassic tectonic evolution of Western Adria has sector of Northern Italy (Varese Area), where the outcropping been variously interpreted either as the first rifting phase Permo-Carboniferous sequence and the overlying Triassic to that led to the opening of the Alpine Tethys or as the result Early Jurassic units allow to investigate the crosscut relation-of continental-scale strike-slip movements. Additionally, a com- ships between structures that were active during pre-rift and mon view on the age of inception of the rifting of the Alpine syn-rift tectonic phases. By means of a 3D geological model of Tethys, its duration and its relationship with the antecedent the Varese Area, built on a brand-new geological map, firstly Variscan tectonic phases, is still lacking. The European Western we restored Alpine tectonics and then performed a progressive Southern Alps expose the basement and cover rocks of Western geological restoration of faults, aided by new preliminary Adria and therefore represent a key area for understanding thermochronological data. We unveiled a polyphasic strike-slip and testing the post-Variscan to prerifting evolution of this Permian tectonic phase that switch to an unexpectedly early plate. We focus, in particular, on a relatively poorly deformed inception of the rifting. 60 15TH WORKSHOP Abstract book. 15th Emile Argand Conference on Alpine Geological Studies, 12-14 September 2022, Ljubljana, Slovenia. Platform to basin transitions: mapping observations at the Krvavica Mountain, and Čemšeniška Planina, in the Sava Folds Region Benjamin Scherman1,2, Boštjan Rožič3, Ágnes Görög4, Szilvia Kövér1,2 and László Fodor1,2 1Elte Eötvös Lorand University, Institute of Geography and Earth Sciences, Department of Geology, Budapest, Hungary (benjaminscherman@gmail.com) 2MTA-ELTE Geological, Geophysical and Space Science Research Group of the Hungarian Academy of Sciences at Eötvös University, Budapest, Hungary 3Faculty of Natural Sciences and Engineering, Department of Geology, University of Ljubljana, Ljubljana, Slovenia 4Hantken Miksa Foundation, Budapest, Hungary The Krvavica Mountain and Čemšeniška Planina are situated formations are repeated at least twice by a major thrust. On on the northern limb of the Trojane anticline, a part of the the other hand, a platform progradation into the clastics basin Sava Folds region in central Slovenia. This Cenozoic fold belt is can also be supposed; this feature is typical in central Slovenia situated in the transition zone of the Pannonian basin, the Alps (Gale el al., 2020). However, 500 m west of the Krvavica Mt. and the Dinarides. This area was a part of the Adriatic rifted in the eastern side of Čemšeniška Planina and on the Flinskovo margin of the Neotethys during the Middle-Late Triassic. Re- ridge, recent mapping showed a lithologically typical but con-peated rifting phases continued into the Jurassic. This tectonic densed Slovenian Basin-type sequence. Here, the succession conditions created the Slovenian Basin, which subsided until starts with the pelagic Norian Bača dolomite, followed by the the Late Cretaceous. The extensional phasees were followed by Hettangian–Pliensbachian calciturbiditic Krikov Formation. contraction in the Paleogene and Neogene during the Dinaric After a potential gap in Toarcian, the latter is followed by the and Alpine phases (Placer, 1998a; Schmid et al., 2020). The recently described Bajocian-Bathonian Ponikve Breccia as interplay of two-phase thrusting led to specific young-on-older a part of the Tolmin Formation (Rožič et al., 2018). After a tectonic contact between the Dinaridic Carboniferous-Permian possible gap in the early late Jurassic, the Late Jurassic-Early clastics (“softbed” of Placer, 1998b) and Mesozoic formations Cretaceous Biancone Formation represents the youngest ex-of uncertain origin (Placer, 1998b). The study area SW from posed lithostratigraphic unit in studied area. The proximity of Celje, near the Krvavica Mt., provides good outcrops. Accord- fundamentally different lithological sequences can shed new ing to previous studies the Krvavica Mt. is composed of the light on the platform to basin transition at the border of Slove-platform Schlern Formation while the Čemšeniška Planina is nian Basin with the Dinaridic carbonate platform. However, the partly composed of Bača dolomite, a characteristic Slovenian structural geometry is complex, and could be also explained Basin formation. Our observations show that through the by normal faulting to achieve young-on-older contacts. Alter-Krvavica Mt. three formations can be traced from S to N: 1) natively, post-folding, gently dipping thrusts could dismember the Pseudozylian Formation of latest Ladinian to Carnian age, the pre-existing northern limb of the Trojane anticline. The dis-composed of siliciclastic basin sediments (shales, sandstones, placement of the tilted (folded) Mesozoic Slovenian basin suc-siltstones, micritic cherty limestones, breccia, and pyroclastics), cession can also be explained by a post-folding thrust, which 2) the Schlern Fm. composed of Triassic platform carbonates led to the contact of the pelagic formations with the underlying and 3) formation composed of latest Jurassic to Early Creta- folded Carboniferous-Permian rocks of the Dinarides. ceous carbonates and mixed carbonate-siliciclastic rocks. These Acknowledgements: The research was supported by the National Research, Development and Innovation Office of Hungary (134873) and the Slovenian Research Agency (No. P1-0195). Gale, L., Peybernes, C., Mavrič, T., Kolar-Jurkovšek, T., & Jurkovšek, B. (2020). Facies and fossil associations in Ladinian carbonate olistoliths at Dole pri Litiji, Slovenia. Facies, 66(3), 1-25. Placer, L. (1998a). Structural meaning of the Sava folds. Geologija, 41, 191–221. https://doi.org/10.5474/geologija.1998.012 Placer, L. (1998b). Contribution to the macrotectonic subdivision of the border region between Southern Alps and External Dinarides. Geologija, 41(1), 223–255. Rožič, B., Gerčar, D., Oprčkal, P., Švara, A., Turnšek, D., Jurkovšek, T., Udovč, J., Kunst, L., Fabjan, T., Popit, T., Gale, L. (2019). Middle Jurassic limestone megabreccia from the southern margin of the Slovenian Basin. Swiss J Geosciences, 112, 163–180. 61 15TH WORKSHOP Abstract book. 15th Emile Argand Conference on Alpine Geological Studies, 12-14 September 2022, Ljubljana, Slovenia. Geological history of the Troiseck-Floning Nappe (Austroalpine unit, Styria/Austria) Ralf Schuster1, Christoph Iglseder1, Martin Reiser1 and Daniela Gallhofer2 1Geological Survey of Austria, Vienna, Austria (ralf.schuster@geologie.ac.at) 2Institute of Earth Sciences, University of Graz, Graz, Austria This contribution reports LA-ICP-MS zircon ages and Rb-Sr bi- composition is granitic/rhyolitic with an alkali-calcic signature. otite ages from the Troiseck-Floning Nappe, forming the north- In classification diagrams it plots in the field of syn-collision easternmost extension of the Silvretta-Seckau Nappe System granite. Zircon ages of about 270 Ma indicate a Permian crys-in the Eastern Alps. The Troiseck-Floning Nappe comprises a tallization. Similar rocks interpreted as Permian rhyolitic me-basement formed by the Troiseck Complex and a Permo-Trias- tavolcanics appear in the cover sequence. They share a similar sic cover sequence. The basement consists of paragneiss with chemical composition and crystallization age of 270 Ma. Asso-intercalations of micaschist, amphibolite and different types of ciated intermediate metavolcanics developed from calc-alkaline orthogneiss, which was affected by a Variscan (Late Devonian) basaltic andesite. amphibolite facies metamorphic overprint. The cover sequence includes Permian clastic metasediments and metavolcanics, as According to Rb-Sr biotite ages cooling of the Troiseck-Floning well as Triassic quartzite, rauhwacke, calcitic marble and dolo- Nappe below c. 300 °C occurred at about 85 Ma in the west mite. During the Eoalpine (Cretaceous) tectonothermal event and 75 Ma in the east. the nappe experienced deformation at lower greenschist facies conditions. In summary, the Troiseck Complex developed from Cambrian to Ordovizian clastic metasediments and granitic and basaltic Detrital zircon grains from paragneiss are in the range of 530- magmatic rocks emplaced in the same time range. During the 590 Ma, indicating an Ediacarian to earliest Cambrian source Late Devonian, it was affected by the Variscan collisional event, and a Cambrian to Ordovizian deposition age of the protolith. causing deformation at amphibolite facies conditions and intru-Late Cambrian to Ordovician crystallization ages from leu- sion of calc-alkaline granites. In early Mississippian time peg-cogranitic intrusions represent the earliest magmatic event of matite dikes intruded, maybe induced by decompression and the Troiseck Complex. The amphibolite bodies derived from exhumation. The deposition of clastic sediments and (sub)vol-basalt with a calcalkaline to island arc tholeiitic signature. canic rocks (rhyolite and basaltic andesite) constrains a surface position of the Troiseck Complex during the Permian. Based Leucocratic orthogneiss with K-feldspar porphyroclasts and a on regional considerations an extensional environment is calc-alkaline granitic composition plots in the field of volcanic assumed. In Triassic times carbonate platform sediments were arc granite. The youngest zircon grains indicate a Late Devoni- deposited. During the Eo-Alpine collision in the Cretaceous an crystallization. Two pegmatite gneisses with a calc-alkaline the unit was part of the tectonic lower plate and subducted composition are early Mississippian in age. to shallow crustal levels, indicated by a lower greenschist fa- cies metamorphic overprint. The Troiseck-Floning Nappe was Mylonitic orthogneiss with a pronounced stretching lineation formed and exhumed since about 85 Ma. Rb-Sr as well as ap-appears as irregularly shaped layers. It is leucocratic, very fine atite fission track data from the literature indicate tilting with grained and contains scattered feldspar porphyroclasts with more pronounced exhumation and erosion in the eastern part a round shape and a diameter of about 1 mm. Its chemical during Miocene lateral extrusion of the Eastern Alps. 62 15TH WORKSHOP Abstract book. 15th Emile Argand Conference on Alpine Geological Studies, 12-14 September 2022, Ljubljana, Slovenia. Internal deformation and tectonic evolution of the Dolomites Indenter, eastern Southern Alps: A combined field and analogue modelling study Anna-Katharina Sieberer1, Ernst Willingshofer2, Thomas Klotz1, Hugo Ortner1, and Hannah Pomella1 1University of Innsbruck, Department of Geology, Innsbruck, Austria (anna-katharina.sieberer@uibk.ac.at) 2Utrecht University, Department of Earth Sciences, Utrecht, Netherlands In the evolution of the Alps, the Adriatic plate is tradition- Analyses of surface displacement vectors show that these areas ally considered as rigid indenter and research on collision are associated with changes in shortening directions, resulting and extrusion tectonics mainly focused on the areas north in, curved faults. All models emphasise that the overall style of it. However, the structure of the northernmost part of the of deformation is less dependent on the material of the basal Adriatic microplate in the eastern Southern Alps of Italy and décollement, but is ruled by the inherited platform and basin Slovenia, referred to as Dolomites Indenter (DI), demonstrates configuration, independent of orthogonal or oblique inversion. significant internal deformation of a continental indenter that contains the structural memory of Jurassic extension leading to To compare analogue modelling results with deformation in the formation of the Alpine Tethys. Here we argue that these the DI, structural fieldwork accompanied by thermochronolog-pre-existing NNE-SSW trending normal faults are of paramount ical sampling was carried out. Examined cross-cutting criteria importance for understanding and explaining Paleogene covering the entire DI comprise evidence for four distinguish-to Neogene crustal deformation of the DI. In particular, we able deformation phases during Paleogene (Dinaric) shortening demonstrate through physical analogue modelling that lateral and subsequent Neogene (Alpine) continental indentation: changes of thrust fault orientations are controlled by the in- Top SW, Top (S)SE, Top S and Top E(SE). However, shortening herited fault bound basin and platform configuration (e.g., in directions along several of the studied faults, e.g. the overall the Cadore area, where the Trento platform merges into the SSE-vergent Belluno thrust (Valsugana fault system), change Belluno basin). locally from top SSW to top SSE along strike. Based on our modelling results, we infer that the variability In our brittle and brittle-ductile analogue experiments, short- of shortening directions along these thrust faults may depend ening is orthogonal or oblique to platform and basin configu- on inherited structures and do not necessarily reflect different ration, which is represented by either (i) pre-scribed strength deformation phases. As such the number of deformation phases contrasts between platforms/basins or (ii) graben structures in the Southern Alps may have been overestimated so far. modelled by an initial extensional phase. This approach allows us to test various deformational wavelengths as well as timing and localisation of uplift of the DI’s upper to middle crust. Modelling results indicate that the localisation of deformation is controlled by lateral strength contrasts, as transitions from platforms to basins represent. 63 15TH WORKSHOP Abstract book. 15th Emile Argand Conference on Alpine Geological Studies, 12-14 September 2022, Ljubljana, Slovenia. Differentiation and genesis of the Middle Triassic mafic volcanic and volcaniclastic facies in NW Croatia - case study from Vudelja quarry Duje Smirčić1, Matija Vukovski2, Damir Slovenec2, Duje Kukoč2, Mirko Belak2, Tonći Grgasović2, Branimir Šegvić3 and Luka Badurina3 1University of Zagreb, Faculty of mining, geology and petroleum engineering, Department for mineralogy, petrology and mineral resources, Pierottijeva 6, 10000 Zagreb, Croatia (duje.smircic@rgn.hr) 2Croatian Geological Survey, Department of Geology, Sachsova 2, HR-10000 Zagreb, Croatia. 3Department of Geosciences, Texas Tech University, 1200 Memorial Circle, Lubbock, TX 79409, USA The Middle Triassic period represents a very dynamic time tion of a basaltic effusion in the marine environment is another in a broader Tethyan region. Tectonic movements related to possible process explaining the formation of basalt clasts. Py-disintegration of Pangea and opening of the Neotethys gave roclastic flow facies is composed of plagioclase crystalloclasts, rise to the formation of volcanic and volcaniclastic deposits. In basaltic lithoclasts and scoria fragments, with the flow texture the NW Croatia, these rocks outcrop in approximately 60 km indicated by clast arrangement and glassy matrix with flow long intra-Pannonian Mountain chain (Mts. Kalnik, Ivanščica, features. This facies occurs only locally and its geographical Strahinjščica, Kuna Gora, Desinić Gora and Ravna Gora), rep- extent is limited thus indicating a small volume of the flow, resenting the junction between the Southern Alps and Internal characteristic for basaltic pyroclastic flows of scoria and ash Dinarides. Among these mountains, Mt. Ivanščica represents type. Resedimented autoclastic facies is dominant at the out-a complex structure built of shallow-marine to pelagic succes- cropping quarry front and is composed of several lithotypes sions originating off the passive continental margin of Adria with various grain sizes and types of matrix. Clast dimensions microplate. These deposits are found in a tectonic contact with vary from block to ash size. Some samples exhibit common ophiolitic mélange containing remnants of Neotethys. Middle sedimentary features such as horizontal lamination. The facies Triassic volcanic and volcaniclastic rocks from this area include was formed by the autofragmention processes of hot basaltic basic/intermediate to acidic effusive and pyroclastic lithologies magma in contact with sea water, and subsequent resedimenta-and are interfingered with marine sediments. tion of newly formed volcaniclastic particles. Due to an intense tectonic disruption, spatial organization of determined facies is The specific area of Vudelja quarry, situated in the central part not clear, though the alienation from the primary source can of the northern Ivanščica slopes, is composed mainly of mafic generally be followed from south to north. lithologies and their volcaniclastic derivates. Volcanic and vol- caniclastic rocks of basaltic composition were studied in detail Studied locality presents a portion of Middle Triassic volcanic to distinguish different facies and their spatial distribution. and volcano-sedimentary formations well known from the Three different facies were recognized: 1)autoclastic effusive Southern Alps, Transdanubian Range and the Dinarides. facies; 2) pyroclastic flow facies, and 3) resedimented autoclas- Intense volcanic activity, related to the rifting between the fu-tic facies. Autolcastic effusive facies is composed of hyaline to ture Adria microplate and southern edge of Laurasia, fed the intersertal basalts, with incorporated clasts of the same litho- material to a complicated pattern of sedimentary environments type. This facies was formed by effusion of basaltic magma. formed along the future Adria passive margin. Extensional tec-Basaltic clasts were likely incorporated by the primary effusive tonics created deep faults within the continental crust which flow during magma ascent, or following effusion while flowing might have served as conduits for submarine basaltic extru-over the fragmented basaltic material. Quenching fragmenta- sions. 64 15TH WORKSHOP Abstract book. 15th Emile Argand Conference on Alpine Geological Studies, 12-14 September 2022, Ljubljana, Slovenia. Tectonic Transfer from the Western Alpine Front to the French Rhône Valley in its 3D-Structural Context Christian Sue1,2, Andrea Walpersdorf1, Dorian Bienveignant1, Lina Al Najjar1, Estelle Hannouz1, Anne Lemoine3 and Stephane Baize4 1University Grenoble Alpes, University Savoie Mont Blanc, CNRS, IRD, IFSTTAR, ISTerre, Grenoble, France (christian.sue@univgrenoble-alpes.fr) 2Univ. Franche Comte, Besancon, France 3Brgm, Orleans, France 4IRSN-BERSSIN, Fontenay-aux-Roses – France The Western Alps current tectonics is characterized by seismi- Seismic strain rates are then compared to the geodetic strain cally active radial extension in the core of the belt, combined field obtained from an updated GNSS solution focused on with transcurrent to transpressive tectonics in its external zone the study area. Seismic strain rates of subareas in the Rhone and foreland associated with a moderate seismicity. We focus Valley and surroundings range between a few nanostrains/ on the tectonic transfer from the W-Alps to their foreland, yr and 10E-2 nanostrains/yr. In terms of amplitude, geodesy namely the French Rhône Valley, a region with high societal seems to provide deformation rates one order of magnitude challenges, including demography, nuclear powerplants, and higher than seismicity. However, our seismic strain tensors chemical industries. We combine seismotectonic and geodetic are globally consistent with the geodetic ones, specifically in (GNSS) approaches to constrain the stress and strain fields the front of the Alps (Belledonne region), where seismic and of the area extended from the alpine External Crystalline geodetic networks are denser. In a last step, we replace these Massifs to the eastern edge of the French Massif Central, strain and stress fields in a new 3D-structural model, which has which encompasses the Rhône Valley. Seismic strain rates been developed on purpose. It integrates the main crustal units for a set of subareas defined on tectonic arguments (seismo- and the main faults of the area, allowing to better constrain tectonic zoning) have been evaluated. They are processed by the relationship between the current deformation and stress combining the total seismic energy obtained with statistical patterns of the Rhône Valley under the Alpine influence, and integrations of Gutenberg-Richter distributions with repre- the inherited fault system carving the entire domain. sentative focal-mechanisms obtained from stress inversions. 65 15TH WORKSHOP Abstract book. 15th Emile Argand Conference on Alpine Geological Studies, 12-14 September 2022, Ljubljana, Slovenia. Petrography of ultrabasic and basic rocks from the Ozren ophiolite complex (Bosnia and Herzegovina) Samir Ustalić1, Marián Putiš1, Ondrej Nemec1, Peter Ružička1, Elvir Babajić2 and Petar Katanić3 1Comenius University, Faculty of Natural Sciences, Department of Mineralogy, Petrology and Economic Geology, Ilkovičova 6, 842 15 Bratislava, Slovakia (ustalic1@uniba.sk) 2University of Tuzla, Faculty of Mining, Geology and Civil Engineering, Department of Mineralogy and Petrology, Urfeta Vejzagića 2, 75 000 Tuzla, Bosnia and Herzegovina 3GIM GEOTEHNIKA d.o.o, Bulevar vojvode Stepe Stepanovića 177, 78 000 Banja Luka, Bosnia and Herzegovina The Ozren ophiolite complex (OOC) in Bosnia and Herzegovi- troctolites in peridotite. These dykes have randomly oriented na is a part of large Dinaride ophiolite belt (Babajić, 2019, and minerals, only locally showing mylonitization signatures. A reference therein). This contribution comprises mineralogi- basaltic dyke cross-cuts gabbro collected from a borehole core. cal-petrographical descriptions of representative rocks of the Dolerites are composed of Cpx, Amp and Pl but we also found OOC, which we sampled during the field investigation: lherzo- an Ol-bearing dolerite dyke cross-cutting peridotite. It has well lites, harzburgites, dunites, gabbros, dolerites, and troctolites. preserved magmatic ophitic texture composed of Ol, Opx, Cpx, The mineral composition was determined by polarized trans- Amp, Pl, Ilm and Ap. Pyroxenes and amphiboles are weakly mitted light microscopy and introductory EPMA. The purpose chloritized and Ol is serpentinized. Dolerites and basalts have of this and the next study is the determination of magmatic and an ophitic texture, defined by fine-grained prismatic Pl, Px and metamorphic evolution, and geochronology of the OOC. Lher- Amp. Secondary Amp2 and Chl follow the grain boundaries of zolites contain Ol (55 vol. %), Opx (25 %) and Cpx (15 %). magmatic minerals. Ophiolitic breccias cover some peridotite Anhedral Opx porphyroclasts have Cpx exsolution lamellae. parts. These breccias contain 1 cm – 10 m size fragments of Similarly, porphyroclastic Cpx contains Opx exsolution lamel- all lithological members of the OOC, including radiolarites. lae. Late magmatic Cpx and Opx aggregates ingrow the Ol Gabbros from ophiolitic breccia have coarse grained Pl and Px. matrix and porphyroclastic Px1 boundaries. Spinel is immersed Exsolution lamellae in Px and their kink-banding are character-in the Ol matrix. Harzburgites are composed of Ol (55 vol. %), istic features from the subsolidus late-magmatic conditions. A Opx with Cpx exsolution lamellae (35 %), and Cpx with Opx rare plagiogranite intrusion in peridotite is composed of Qz, Pl exsolution lamellae (5 %) the latter following Ol-Opx bound- and needle-like Amp aggregates after Bt. Such an association aries. Spinel occurs in the form of anhedral grains. Dunites are of ultrabasic and basic rocks have formed by a contribution rare. A remnant of the inferred gabbroic layer was identified of percolating gabbroic magmas through the peridotites at a from a borehole core and a few km-size gabbro-doleritic blocks higher lithosphere level, crystallizing Pl and Cpx. Amphibolites within peridotites. These gabbros have ophitic texture and were found only at one locality so far, most likely indicating contains primary magmatic porphyric Pl, Cpx and green Amp1. metamorphic sole of an ophiolitic thrust sheet. The preliminary Clinopyroxene and Amp1 are partially replaced by blue-green results suggest at least two magmatic evolutional stages of the Amp2 aggregates and Chl. Plagioclase is weakly altered. More- OOC, in the Spl and Pl stability field, respectively. Metamorphic over, we found cross-cutting gabbroic (microgabbros, called overprinting is indicated by the newly formed Amp generations dolerites, to gabbro-pegmatites) dykes, and dunite-associated and an amphibolitic sole. Acknowledgements: APVV Agency Project No. APVV-19-0065 (M.P.) is acknowledged. Babajić E. (2019) Krivaja-Konjuh ophiolite complex – petrology, geochemistry and geotectonics of mafic sequences. (Monograph), MIT-ALEX, Tuzla (Bosnia and Herzegovina) 66 15TH WORKSHOP Abstract book. 15th Emile Argand Conference on Alpine Geological Studies, 12-14 September 2022, Ljubljana, Slovenia. Jurassic pelagic succession of NW Croatia – a key to better understanding tectonic setting of the Southern Alps – Dinarides transition zone Matija Vukovski, Duje Kukoč, Tonći Grgasovic, Ladislav Fuček, and Damir Slovenec Croatian Geological Survey, Department of Geology, Zagreb, Croatia (mvukovski@hgi-cgs.hr) Ivanščica Mt. is an inselberg in the transitional area where Dachstein limestone, which were so far interpreted as klip-S-verging Southern Alpine structures overprint NNW-verging pes (Šimunić et al., 1976), or olistoliths (Babić and Zupanič, Dinaric structures (van Gelder et al., 2015, and references 1978). Our new data indicate continuous succession on top of therein). It is composed of Triassic to Cretaceous shallow to Dachstein limestones composed of shallow-marine carbonates, deep-marine sedimentary succession of the Adriatic continental represented by intraclasticpeloidal packstones to grainstones, passive margin (Šimunić et al., 1976), overthrust by ophiolitic gradually transitioning to wackestones with pelagic influence. mélange (Babić et al., 2002). Early Cretaceous siliciclastic fly- The onset of pelagic sedimentation took place around the end sch-type deposits continuously overlaying pelagic limestones of the Early Jurassic when thin bedded marls, shales, marly clearly indicates distal position of these successions on the limestones with intercalated fine-grained calciturbidites were continental margin. However, so far complete Jurassic suc- deposited. Higher in the succession Callovian to possibly early cession on Mt. Ivanščica was never found, causing different Tithonian radiolarian cherts are overlaid by calcarenites, late interpretations of its Mesozoic history. Babić (1974) assumed Tithonian to Early Cretaceous pelagic limestones and Early the existence of Jurassic pelagic succession on top of the Late Cretaceous flysch-type deposits. Triassic shallow-water carbonates, describing up to few meters of Early to Middle Jurassic condensed pelagic limestone over- Discovery of the Jurassic pelagic sediments allows for a new lain by Late Jurassic radiolarian cherts and pelagic limestones. interpretation of structural relations on the Ivanščica Mt. In Contrary, Šimunić et al. (1976) assumed shallow-marine condi- our opinion occurrence of Dachstein limestone, previously tions throughout the Early Jurassic followed by emersion until interpreted as klippes or olistoliths represent an imbricate fan. latest Jurassic. Our study revealed for the first time complete Because the Southern Alps thrust front in this area was inter-shallowwater to pelagic Jurassic succession on Mt. Ivanščica. preted according to these mapped klippes and nappe contact, our findings may also have an impact on the redefining of the Southern slopes of Ivanščica Mt. are mostly built of ophiolitic easternmost Southern Alps thrust front. mélange, except for prominent hills built of the Late Triassic Babić, Lj. (1974). Jurassic−Cretaceous sequence of Mt. Ivanščica (North Croatia). Bull. Sci. Cons. Acad. Yugoslav. (A), 19/7−8, 180−181. Babić, Lj. & Zupanič, J. (1978). Mlađi mezozoik Ivanščice. In Babić, Lj. & Jelaska, V. (Eds.). Fieldtrip Guidebook 3. Skupa sedimentologa Jugoslavi-je. , (11–23). Hrvatsko Geološko Društvo. Babić, Lj., Hochuli P. A.. & Zupanič, J. (2002). The Jurassic ophiolitic mélange in the NE Dinarides: dating, internal structure and geotectonic implications. Eclogae Geologicae Helvetiae, 95, 263–75. Šimunić, A., Pikija, M., Šimunič, Al., Šikić, K. & Milanović, M. (1976): Stratigrafsko – tektonski odnosi centralnog i istočnog dijela Ivanščice. In 8. Jugosl.geol.kongres, Bled, 1974. (303-313)., Slovensko geološko društvo. van Gelder, I., Matenco, L., Willingshofer, E., Tomljenović, B., & Andriessen, P., Ducea, M., Beniest, A. & Gruić, A. (2015). The tectonic evolution of a critical segment of the Dinarides-Alps connection: Kinematic and geochronological inferences from the Medvednica Mountains, NE Croatia. Tectonics, 34(9), 1952-1978. https://doi.org/10.1002/2015TC003937 67 15TH WORKSHOP Abstract book. 15th Emile Argand Conference on Alpine Geological Studies, 12-14 September 2022, Ljubljana, Slovenia. The Albian/Cenomanian Boundary Event (OAE1d) reflected in ammonite-rich layers in central Serbia (Topola area) Marija Vuletić1, Hans-Jürgen Gawlick2, Nevenka Đerić1, László Bujtor3, Katarina Bogićević1 and Draženko Nenadić1 1University of Belgrade, Faculty of Mining and Geology, Belgrade, Serbia (marija.vuletic@rgf.bg.ac.rs) 2Montanuniversität Leoben, Department Applied Geosciences and Geophysics, Leoben, Austria 3University of Pécs, Department of Geology and Meteorology, Pécs, Hungary Occurrences of the Albian/Cenomanian Boundary Event bitolinid-bearing carbonate ramp. In the more fine-grained (OAE1d, namely Breistroffer Level), reflected in a series of four and slightly organic-rich silt to fine-sand layers approx. eight distinct positive δ 13C excursions (peak in the latest Albian) are meters above the first ammonite-bearing level following until now not described in Serbia even various associations of ammonite fauna indicate the uppermost Albian to lowermost late Early Cretaceous ammonite faunas are known from several Cenomanian ( Arrhaphoceras briacensis Zone or Stoliczkaia dis-locations in central Serbia. These ammonite-bearing sedimen- par Zone): Phylloceras (Hypophylloceras) velledae, Kossmatella tary rocks are exposed in the narrow belt of the Belgrade-Kos- agassiziana, Puzosia (Puzosia) mayoriana, Beudanticeras sp., maj-Topola-Gledić Mts. above shallow-water orbitolinid fora- Mortoniceras sp., Stoliczkaia (Stoliczkaia) dispar, Mariella sp., minifera-bearing limestones (carbonate ramp deposits). and Scaphites (Scaphites) sp. Near village Kotraža (22 km SE of Topola) a roughly 20 m Whereas in the Western Tethys Realm the latest Albian OEA1d thick sedimentary succession of sand- and siltstones, marls and is mainly characterized by the deposition of organic-rich fine-claystones with intercalated volcanic rocks and two distinct grained sediments, in central Serbia west of the Drina-Ivanjica ammonite bearing horizons is preserved (“Stragari facies” in continental realm more coarse-grained sediments were depos-the Serbian literature). In the lower (roughly 11 m thick) and ited. However, the occurrence of the younger ammonite-rich more coarse-grained part of the succession, beside belemnites, interval in slightly organic-rich sedimentary rocks mirror the gastropods, and plant remains, a rich, but poor to moderately global late Albian OAE1d, whereas the older ammonite-rich preserved ammonite fauna occur in slump deposits together intervall is a precursor event associated with intense volcanic with coarse eruptive volcanic material: Kossmatella agassiziana, activity near to the study area. This intense volcanic activity led Puzosia (Puzosia) mayoriana, Mortoniceras (Subschloenbachia) to the regional drowning of the shallow-water orbitolinid fora-perinflatum, Anisoceras perarmatum, Anisoceras sp., Idiohamites minifera-bearing carbonate ramp and creates relief as indicated elegantulus, Mariella sp., Ostlingoceras cf. puzosianum, and by the slump deposits. It is proposed that in central Serbia Scaphites (Scaphites) sp. The occurrence of Praeschloenbachia regional and global events work in concert to form in the late perinflatum indicates the Upper Albian Mortoniceras perinfla- Albian deeper-water environment ammonite-rich horizons, tum Zone. Upsection a fining-upward trend indicates ongoing which have the potential for a correlation of late Albian events deeping of the depositional realm due to the stepwise sea-level in the Dinarides and adjacent areas. rise from the late Albian onwards and the decease of the or- Acknowledgements: In the frame of the IGCP 710 „Western Tethys meets Eastern Tethys“. 68 15TH WORKSHOP Abstract book. 15th Emile Argand Conference on Alpine Geological Studies, 12-14 September 2022, Ljubljana, Slovenia. Peak pressure estimates of Koralpe-Saualpe-Pohorje Complex based on Raman Spectroscopy Iris Wannhoff, Jan Pleuger, Timm John, Xin Zhong, and Moritz Liesegang Freie Universität Berlin, Institut für Geologische Wissenschaften, Berlin, Germany (i.wannhoff@fu-berlin.de) The Koralpe-Saualpe-Pohorje Complex in the Eastern Alps rep- show an overall residual P increase of the quartz inclusions from resents a lithologically heterogenous (U)HP nappe with eclogite the northern Saualpe towards Pohorje in the South. The quartz lenses embedded in gneissic and metasedimentary rocks. The inclusions inside garnet in eclogite show higher residual P with aim of this project is to determine whether or not tectonic pres- ≤ 0.72 GPa with respect to the ones in the metasedimentary or sure occurred due to differences in viscosity of different litholo- gneissic lithologies with ≤ 0.43 GPa. Elemental maps of garnets gies. In this study we investigate in detail the P and T conditions in eclogite from three locations show rather variable results with during the formation of the Koralpe–Saualpe–Pohorje Complex a significant variation of Ca and Mg content in the core, whereas along a NW-SE transect. In order to determine the P conditions, the Mn content is general very low. The metasedimentary and quartz inclusions in garnet are investigated with Raman spec- gneissic garnets are predominantly much richer in Fe and show troscopy (RSQI barometry). With Zr-in-rutile thermometry, the higher Mn with respect to the eclogites. temperature conditions will be determined. Preliminary results 69 15TH WORKSHOP Abstract book. 15th Emile Argand Conference on Alpine Geological Studies, 12-14 September 2022, Ljubljana, Slovenia. Tectonic and metamorphic record in the Badstub Formation, Carboniferous of Nötsch, Austroalpine Davide Zanoni, Marco Filippi, Manuel Roda, Alessandro Regorda, and Maria Iole Spalla Dipartimento di Scienze della Terra “A. Desio”, Università degli Studi di Milano, Milano, Italy (davide.zanoni@unimi.it) The Badstub Formation is part of the Carboniferous of Nötsch GPa and testify that the Badstub Formation recorded a metasedimentary sequence, of the Upper Austroalpine domain. This morphic imprint characterized by a low temperature/depth formation outcrops in Carinthia (Austria), a few kilometres ratio (≈15 °C km-1). The comparison between a 2D thermo-me-north of the Periadriatic line (Gailtal line), where a sequence chanical numerical model and the metamorphic conditions of various conglomerates and breccias with interbedded inferred with thermodynamic models suggest that the Badstub sandstones, siltstones, and fossiliferous carbonatic schists is ex- Formation underwent a thermal state consistent with that of posed. These rocks preserve pristine sedimentary features and the Alpine subduction. These results provide the first quantita-even an outstanding fossil record, but multi-scale structural tive pressure constraints on Alpine subduction metamorphism analysis revealed a tectonitic foliation localized in fine-grained on the Austroalpine Carboniferous covers nearby the Periadri-rocks, different sets of mineralized faults and veins, and corona atic line. Thus, within the Upper Austroalpine nappe system, textures. Vein fillings and coronas are characterized by equilib- pre-Alpine rocks were involved into the Alpine subduction at rium mineral assemblages that include prehnite, pumpellyite, different structural levels and under metamorphic conditions, chlorite, phengite, winchite, and riebeckite. Chlorite-thermom- which therefore span from eclogitic to prehnite-pumpellyite etry and thermodynamic modelling on mineralized veins and facies. coronas revealed PT conditions of 260-310 °C and 0.25-0.50 70 15TH WORKSHOP Abstract book. 15th Emile Argand Conference on Alpine Geological Studies, 12-14 September 2022, Ljubljana, Slovenia. 71 15TH WORKSHOP Abstract book & Fieldtrip guide. 15th Emile Argand Conference on Alpine Geological Studies, 12-14 September 2022, Ljubljana, Slovenia. Ladinian halfgrabens above Ajdovska deklica in Mt. Prisojnik, Julian Alps (Author: Boštjan Rožič) 72 15TH WORKSHOP Abstract book & Fieldtrip guide. 15th Emile Argand Conference on Alpine Geological Studies, 12-14 September 2022, Ljubljana, Slovenia. Fieldtrip guide 15TH Emile Argand Conference on Alpine Geological Studies 12-14 September 2022, Ljubljana, Slovenia 73 15TH WORKSHOP Fieldtrip guide. 15th Emile Argand Conference on Alpine Geological Studies, 12-14 September 2022, Ljubljana, Slovenia. 74 15TH WORKSHOP Fieldtrip guide. 15th Emile Argand Conference on Alpine Geological Studies, 12-14 September 2022, Ljubljana, Slovenia. Adria margin of the Alpine-Dinaric transition area – sedimentary view and a structural glimpse FIELDTRIP A Boštjan Rožič1, Matevž Novak2, Luka Gale1,2, Andrej Šmuc1, Duje Kukoč3 and Stanka Šebela4 1Department of Geology, NTF, UL, Aškerčeva cesta 12, 1000 Ljubljana, Slovenia (bostjan.rozic@ntf.uni-lj.si) 2Geological Survey of Slovenia, Dimičeva ulica 14, 1000 Ljubljana, Slovenia 3Croatian Geological Survey, Department of Geology, Milana Sachsa 2, 10 000 Zagreb, Croatia 4Karst Research Institute, ZRC SAZU, Titov trg 2, 6230 Postojna, Slovenia Introduction The entire region of western Slovenia is characterized by sedi- mentary rocks and sediments that reveal a long geologic history, stretching from the Devonian to the present, and documenting the late-Variscan and the entire Alpine orogenic cycle. Structur- ally, western Slovenia is marked by the Alpine-Dinaric transition zone. The Dinarides are characterized by the Late Eocene to Oligocene SW verging thrusts, while in the Southern Alps the S-verging thrusts overprint the previous. Neotectonic activity is dominated by NW-SE dextral striking strike-slip faults (Placer, 1998, 2008; Vrabec and Fodor, 2006) (Fig. 1). In general, the oldest rocks occur in the northern part of the Southern Alps in the Karavanke (Karawanken) Mts., while the rocks become progressively younger towards the south. The Vari- scan cycle starts with Devonian passive margin carbonates dom- inated by Middle Devonian reef limestones, which pass upward and downward into the deep marine thin-bedded limestones with intercalations of fine clastics. In the Early Carboniferous, the deposition of flysch (Hochwipfel Fm) begins (Turnšek, 1970; Ramovš, 1993; Ramovš and Buser, 2009). After emergence (discontinuity), the extensive foreland basin was formed, and the Late Carboniferous to Early Permian is characterized by the deposition of a shallow-marine carbonate-siliciclastic sequence (Auernig, Schulterkofel, Dovžanova soteska, Born, Rigelj, Trog- hkofel fms) in the Southern Alps (STOP 1/1) (Novak, 2007; Novak and Skaberne, 2009) and by the deltaic-fluvial clastites in the Dinarides (Mlakar et al., 1993). The Middle Permian be- gins with carbonate breccias (Tarvis/Trbiž Breccia Fm) overlain by thick, mostly reddish/purple fluvial clastites (Val Gardena/ Gröden Fm) (Skaberne, 2003; Skaberne et al., 2009). The thick- ness of this formation varies greatly, indicating intense normal faulting and marking the transition to the Alpine orogenic cycle. Figure 1: Structural subdivision of western Slovenia (after Placer 1999 and Goričan et al., 2018) and generalized stratigraphic columns of the main thrust units. The structural distribution of the major Mesozoic paleogeographic units is as follows: Dinaric Carbonate Platform – AF, KTS, STS, HN, TrN and ToN, Slovenian Basin – SB, Julian Carbonate Platform – KN and SN, Bled Basin – PN. 75 15TH WORKSHOP Fieldtrip guide. 15th Emile Argand Conference on Alpine Geological Studies, 12-14 September 2022, Ljubljana, Slovenia. At the beginning of the Late Permian, the region is character- and Buser, 1991; Ogorelec and Buser, 1996; Turnšek, 1997; ized by a marine transgression, and a long period of predomi- Dozet and Buser, 2009; Ogorelec, 2011; Gale et al., 2013). The nantly carbonate sedimentation begins (STOP 1/2). The Upper thick carbonate succession that characterizes the Julian and Permian of the Southern Alps is dolomitic (Karavanke Fm) and Kamnik – Savinja Alps intermits at the drowning unconformity calcareous in the Dinarides (Žažar Fm), overlain by Lower Tri- near the Carnian/Norian boundary (Celarc et al., 2008, 2014). assic mixed siliciclastic-carbonate marine deposits (Werfen Fm) Deep-marine carbonates are thin in much of the JCP, (Martul-that change to pure carbonates in the Anisian (Buser, 1989, jek Fm) and carbonate reinstallation is rapid, while in the NW 1996; Skaberne and Ogorelec, 2003). This broad shelf area, part the longer lived Trbiž/Travisio basin was formed (Krnica/ known locally as the Slovenian Carbonate Platform, begins Carnizza, Bača Dolomite, Dovška Baba/Frauenkogel, Klek/ to disintegrate already in the Anisian, with the formation of Hahnkogel fms) (Gale et al., 2015). The JCP remained shallow small-scale basins dominated by deeper marine (Ljubelj Fm), marine in the Lower Jurassic when it disintegrated due to the often organic-rich (Strelovec Fm), or condensed carbonates opening of the Alpine Tethys (Buser, 1996; Šmuc, 2005; Rožič (Han Bulog-type) (Buser, 1996; Miklavc et al., 2016; Celarc et et al., 2014). On the western margin of the drowned JCP, the al., 2013; Gale et al., 2022). In the locally uplifted areas of the Bovec Basin was formed. It is characterized by Jurassic basinal Dinarides, erosion leads to stratigraphic gaps and the develop- marls (Skrile Fm), (hemi)pelagic and resedimented limestones ment of fluvial-deltaic (Stopnik conglomerate) or marsh (lower (Travnik, Biancone fms). The central part of the drowned Skonca beds) sediments (Čar and Skaberne, 2003; Čar, 2010). JCP turned into a submarine plateau, named the Julian High, The Ladinian is marked by an extensive paleogeographic characterized mainly by condensed carbonates with numerous reorganisation of the region, related to the opening of the Neo- long-lasting unconformities (Prehodavci, Biancone, “Scaglia” tethys Ocean. As a result of intense normal faulting and volca- fms) (Jurkovšek et al., 1988; Šmuc, 2005; Šmuc and Goričan, nic activity, laterally highly variable rocks were formed. Deep 2005; Šmuc and Rožič, 2010). marine clastic, volcanic, siliciclastic, and carbonate successions were deposited in the subsided areas (Pseudozilian beds) The SB succession begins with Carnian sandstone, breccias, (Buser, 1996; Dozet and Buser, 2009). At the same time, a plat- calcarenite (resedimented limestone), and marls (Amphiclina form carbonate continued to be deposited in the less subsided beds) (Buser, 1996; Gale et al., 2016). Upward, gravity-flow areas (Schlern Fm), while calcareous-volcaniclastic sediments deposits are dominated by carbonates, while (hemi)pelagic (Buchenstein Fm) and volcanics (e.g. Rio Fredo/Mrzla reka interbeds vary from carbonates (STOP 2/3) (Bača Dolomite, Riolite) developed in smaller intraplatform basins (Celarc et Slatnik, Krikov, Biancone, Volče fms), marlstones (Perbla, al., 2013), while the half-grabens were characterised by coarse Lower Flyschoid fms), and radiolarites (Tolmin Fm) (Cousin, carbonate clastics (STOP 1/3) (Ukve/Uggovizza Breccia Fm). 1981; Buser, 1996; Rožič, 2005, 2009; Gale, 2010; Goričan et In the Dinarides, a synsedimentary Idria Hg ore originated (up- al., 2012a,b). Resedimented limestones were shed from both per Skonca beds) (Čar, 1990, 2010, 2013). platforms until the end of the Pliensbachian, whereas after the disintegration and drowning of the JCP, the northern parts of Towards the end of the Ladinian, rifting events ceased and the basin became dominated by pelagites (Rožič, 2009; Rožič platforms prograded over small-scale basins (Šmuc and Čar, et al., 2009, 2017, 2018). The transition to flysch sedimenta-2002; Skaberne et al., 2003; Celarc et al., 2013). Two major tion occurred at the end of the Cretaceous (Upper Flyschoid carbonate platforms were formed, the Dinaric (Adriatic, Friuli) Fm) (Buser, 1996). Carbonate Platform (DCP), now found in the Dinarides, and the Julian Carbonate Platform (JCP) of the Southern Alps. In The DCP documents the emersion phase at the beginning of contrast, the most subsided areas remained deep-marine until the Carnian (Celarc, 2008). The unconformity is overlain by al-the end of the Mesozoic (Cousin, 1981; Buser, 1989, 1996). ternating fluvial clastic and shallow marine limestone sedimen-We divide them into two main paleogeographic units: A) the tation (“Raibl beds”) (Jelen, 1990; Čar, 2010), followed by a Bled Basin (BB) was on the ocean side of the JCP; and B) the long, continuous deposition of carbonates (STOP 3/3) (Triassic Slovenian Basin (SB) was between the DCP and the JCP. Today, Main Dolomite/Dachstein Limestone fms, Jurassic Podbukovje, the SB, BB, and JKP deposits are found in different nappes of Laze, Šentrumar, “Reef Limestone” fms, Cretaceous Brje, Povir, the eastern Southern Alps. BB forms the structurally highest Repen, Sežana, Lipica fms, end-Cretaceous – Paleogene Libur-Pokljuka Nappe, JCP the middle Slatna and Krn nappes, and nia, Trstelj, Alveolinid-Nummulitid Limestone fms) (Buser, the SB the lowermost Tolmin nappe (STOP 2/2) (Placer, 1998; 1996; Dozet and Strohmenger, 2000; Otoničar, 2007; Dozet Goričan et al., 2018). The BB succession is characterized by and Buser, 2009; Buser and Dozet, 2009; Jurkovšek et al., carbonates (STOP 1/4) (Zatrnik, Biancone fms) with the ex- 2013; Jež and Otoničar, 2018). The turn to flysch deposition ception of Middle – Upper Jurassic radiolarites and replaced by occurs first in the northeastern part of the DCP at the end of flysch already in the Valanginian (STOP 2/1) (Studor Fm) (Ku- the Cretaceous (STOP 3/1) and becomes progressively young-koč et al., 2012; Goričan et al., 2018; Gale et al., 2019, 2021). er towards southwest due to a propagating thrust belt (STOP The JCP is characterized by the Upper Triassic platform, 3/2), with the youngest, i.e. Eocene (Lutetian) flysch found on which is reef-rimmed and loferitic in the inner parts (Razor, the Slovenian coast (Pavšič, 1994; Pavšič and Peckmann, 1996; Main Dolomite, Dachstein Limestone fms) with marl-rich Tor/ Buser, 1996; Drobne et al., 2009). Tamar Fm documenting the Carnian Pluvial Event (Turnšek 76 15TH WORKSHOP Fieldtrip guide. 15th Emile Argand Conference on Alpine Geological Studies, 12-14 September 2022, Ljubljana, Slovenia. Post-thrusting subsidence occurred already in the Oligocene in the central and eastern parts of present-day Slovenia, includ- ing the Ljubljana field, characterised by two pulses. Oligocene subsidence begins with sedimentation of coarse fluvial depos- its (Škofja Loka conglomerate), followed by a pronounced transgression (Gornji grad, “Sivica”, Govce fms) accompanied by volcanic activity (Smrekovec Volcanic Complex). After the unconformity, the middle Miocene transgression is document- ed (Laško, Dol fms), followed by lacustrine sediments of the Upper Miocene and Pliocene (Aničić et al., 2002; Jelen et al., 2008; Pavšič and Horvat, 2009; Kralj, 2009; see also Fieldtrip guide for excursion B in this volume). The Quaternary is char- acterised by fluvial and glacial sedimentation (Markič, 2009; Bavec and Pohar, 2009). DAY 1, STOP 1/1 – DOVŽANOVA SOTESKA: Figure 2: The localities of the Dovžanova soteska section (STOP 1/1) and Variscan marine molasse Košutnik potok section (STOP 1/2). The Dovžanova soteska (Dovžan’s gorge), NE of the town of clear cyclic transgressive-regressive depositional pattern can be Tržič, also known as Teufelsschlucht (Devil’s Gorge) in Ger- recognised in the siliciclastic-carbonate sedimentary succession, man-language literature, is a scenic north-south trending valley consistent with the idealised model of the so-called Auernig of the Tržiška Bistrica river, which cuts deep into the southern cyclothem (Kahler, 1955; Krainer, 1992) in the similarly devel-slopes of the Karavanke Mountains and exposes a long section oped stratotype sections of Gzhelian Auernig and Schulterkofel of fossil-rich Late Carboniferous to Middle Permian succession. formations in the Carnic Alps (Austria/Italy). Coarse-grained Generally, beds dip steeply toward the southwest and are fluvial, coastal and/or fan-deltaic conglomerates alternate with therefore gradually older from the village of Čadovlje pri Tržiču finer-grained sandstones and bioturbated siltstones, deposited through the lower entrance of the road tunnel upwards to the under the strong influence of storm events in the lower shore-village of Zg. Dolina (Fig. 2). In this guide book the section is face setting and with limestone horizons mainly related to algal described as complete lithostratigraphic successions, which is mound buildups in the offshore setting below the storm wave necessary to explain the sedimentary history. However, due to base (Novak, 2007). difficult access on these steep slopes, only parts of the succession along the 2 km section of road can be seen (Fig. 3). Both high frequency and high amplitude of sea-level changes, re- corded in the Late Paleozoic sedimentary successions on a global Facies association and (micro)facies characteristics indicate that scale caused considerable shifts of the coastal line due to the flat Gzhelian beds were deposited over the entire Karavanke Mts. topography and the gentle angle of ramp inclination (Massari area on a platform with a gently steeping ramp configuration. A and Venturini, 1990; Samankassou, 1997). In the Early Perm- Figure 3: Dovžanova soteska section along the road from Čadovlje to Zg. Dolina exposes the most complete section of shallow-marine fossil-rich Late Paleozoic beds in the Karavanke Mts. (sketch: M. Novak) 77 15TH WORKSHOP Fieldtrip guide. 15th Emile Argand Conference on Alpine Geological Studies, 12-14 September 2022, Ljubljana, Slovenia. ian, a prominent differentiation of the platform morphology is The youngest Lower Permian succession of the Rigelj Formation recorded in the Karavanke Mts. It is marked by the formation, (Novak and Krainer, 2022) indicates a gradual shift of the fa-drowning, reestablishment, and final subaerial exposure of cies belts from high energy coast through open-marine lagoon a larger reef mound in the Dovžanova soteska area, while in towards the shallow-marine and shelf edge. In the transitional other parts of the Karavanke Mts. predominantly siliciclastic coastal belt, conglomerates, sandstones, and oolitic limestones sedimentation continued. were deposited. Black bedded algal limestones with clay shale intercalations were formed in the inner-shelf environment. Reef The lowermost part of the Permian beds of the Dovžanova limestones and calcareous breccias mark the shelf edge setting. Soteska Formation (Buser and Forke, 1996; Forke, 2002) Black limestones with highly diverse biota and oncoids of the reflects a rapid transgression with a progressive increase of car- upper part of the Rigelj Formation suggest a shift of facies belts bonate content within the clastic sequence. It is followed by the back into the open-marine lagoon. A substantial amount of fine-gradual transition from dark bedded limestones to a light grey grained, well-rounded quartz pebbles in several limestone beds to pale red massive Dovžanova Soteska Limestone body. Since indicates periodical terrigenous influx from a distant hinterland. it is built of fragmented bioclasts in a micritic matrix, bounded The regressive trend continues with the deposition of sandstones only with Tubiphytes, bryozoans, algae, and small sessile fora- and calcitic siltstones in a high-energy shoreface setting. minifers we can refer to it as a reef (or skeletal) mound. The bioclastic packstone to microbreccia, composed of fragmented Based on the facies relationships in the succession of Upper allochthonous reef mound derived debris in the upper part of Paleozoic rocks in the Karavanke Mts., a change in platform Dovžanova Soteska Limestone, represents the reef-flank facies morphology can be suggested. In the Dovžanova soteska area, a deposited in the forereef facies belt and suggests a substantial gently steeping ramp without both the marginal barrier and the topographic relief and the rigidity of the reef mound body shelf break in the basinward direction developed into a rimmed (Stanton and Pray, 2004). shelf with steeper slope as result of lateral and vertical accretion in response to numerous relative sea-level changes. During pe- The following horizon, composed of deeper-water calcareous riods of sea-level stillstands or slow rises the reef mound on the siltstones, marlstones, and thin-bedded marly limestones speaks platform margin rapidly prograded, while as a response to peri-for the short-term drowning of the reef complex prior to the ods of rapid sea-level rises the initial drowning and back-step-deposition of red bedded crinoidal limestones with a rich and ping event gave way to vertical accretion and steeper slope angle diverse shallow-water biotic association. Red stained silty crusts (Reading, 1996). A similar platform evolution has been suggest-capping almost every limestone bed represent omission surfaces ed in many sedimentary basins in different geologic periods. of the hardground type. The uppermost part of the Dovžanova Soteska Formation is marked by the reestablishment of reef A more detailed description of the succession with historical growth, this time with strong marine cementation, suggesting background, facies descriptions, and biostratigraphic data is steep slope inclination. The described development of the given in Novak et al. (2019). Dovžanova Soteska Formation with drowning event, restored reefal sedimentation, and intermediate tongue of deeper-wa- ter and upper-slope facies correlates with the description of a DAY 1, STOP 1/2 – KOŠUTNIKOV POTOK: back-stepping reef with a landward shift of carbonate produc- Slovenian Carbonate Platform tion during an episode of relative sea-level rise (Reading, 1996). In the Košutnikov potok (Košutnik Creek) section near Med-Basal quartz conglomerates of the Born Formation cut into vodje (Fig. 2), a continuous stratigraphic succession from the uppermost beds of red limestone with erosional unconformity. Middle Permian (Val Gardena/Gröden Fm), across the P/T A clear erosional surface and features like calcareous pisoids boundary, to Anisian beds is exposed. The Middle Permian and infillings of vadose silt in the topmost limestones of the Val Gardena Formation of mostly fluvial origin is overlain by Dovžanova Soteska Formation suggest that the reef sedimen- an Upper Permian carbonate sequence 270 m thick that was tation was terminated as result of subaerial exposure (Forke, named the Karavanke Formation (Buser et al., 1988). The bas-2002). During the following transgression, the sedimentary al unit of this sequence is represented by an evaporitic facies depocentre migrated towards the open-marine inner platform. up to 70 m thick composed of cellular dolomite (rauhwacke) The alternation of black bedded bioclastic grain- to pack- with layers of cellular dolomitic breccia containing clasts of stones, biocalcarenites, oolites, sandy limestones and quartz Val Gardena clastics. It alternates with thin black bituminous sandstones with shallow-water benthos in the Born Formation shales and grey vuggy dolomites. In the lower part of the basal indicates deposition in an open lagoonal setting repeatedly unit, only in the Košutnik Creek, a 1.5 m thick sequence of well affected by the sedimentary influx from platform-margin oolitic bedded black bituminous biomicritic limestone was found. Ac-and sand shoals. Some of the mixed carbonate-siliciclastic cording to Buser (1974, 1980) it contains tiny sulphur geodes, rocks (e.g. paraconglomerates) display characteristics typical of Bellerophon gastropods and numerous microfossils ( Gymnocodi-the debris flow deposits (Novak, 2007). One of the rocky pyr- um bellerophontis, Permocalculus fragilis, Mizzia velebitana, and amids is built of massive light grey micritic limestone forming Glomospira sp.) that prove the Late Permian age of the Kara-an isolated patch-reef with colonies of rugose corals. vanke Formation. The evaporitic sequence is overlain by a thick 78 15TH WORKSHOP Fieldtrip guide. 15th Emile Argand Conference on Alpine Geological Studies, 12-14 September 2022, Ljubljana, Slovenia. succession (up to 200 m) of fossiliferous biomicritic dolomites, deposited in an open lagoon and shallow shelf environment (Dolenec et al., 1981). The Late Permian age of these beds is indicated by calcareous algal assemblages ( Mizzia cornuta, Per- mocalculus sp., Connexia sp.), as well as by very common small foraminifers which belong to Glomospira sp., Agathammina sp., and Hemigordius sp. (Ramovš, 1986). The biostratigraphic and lithostratigraphic boundary between the Upper Permian Karavanke Formation and the Lower Trias- sic Werfen Formation is transitional, and no exact line can be drawn between them (Dolenec et al., 1998). The P/T boundary is placed arbitrarily at the end of the sedimentation of the well bedded grey dolomicrite. It is followed by a red coloured, more or less terrigenous sequence predominantly composed of well bedded and laminated siltstones, mudstones, and sandstones, alternating with micritic dolomites that contain no charac- teristic fossils. The sequence was deposited in a very shallow evaporitic restricted shelf, into which abundant terrigenous Fig. 5: δ 13C and δ 18O data of the Košutnikov potok section (from Dolenec material was transported (Dolenec et al., 1981), and is about et al., 2005). 5 m thick. These beds are overlain by mostly dark grey and brown micritic and sparitic limestones intercalated with ooid ian regression and further eustatic oscillations of the Tethys limestone, marlstones and shales. Ooid limestone contains fre- sea-level and by tectonics (Dolenec et al., 1998). At Brsnina, quent small gastropods and corresponds to the limestone of the about 1.6 km to the east of the Košutnik section, the P/T Tesero Member of Werfen Formation. (Buser, 1974; Buser et boundary is exposed in an undisturbed section and represented al., 1988). In Košutnik Creek, the P/T contact is tectonic (Fig. by a sharp, not erosional, contact that consists of a clay layer 4). About 70 to 80 m below the P/T boundary a porphyrite (PTB clay layer) with a maximum thickness of 1 cm. It shows dyke of Middle Triassic (Ladinian) age cuts the Upper Permian a characteristic magnetic susceptibility pulse and considerable beds. enrichment in most minor and trace elements (Dolenec, 2005). The dolomite beds of the Karavanke Formation are enriched The Permian/Triassic boundary in the Southern Karavanke with the light carbon isotope by 4 ‰, and at the boundary the Mts. was the object of a stable isotope composition study in the Th/U ratio also increases. The data indicates an oxic event at Košutnikov potok and at Brsnina sections (Dolenec et al., 1998, the P/T transition, which coincides with the terminal phase of 1999). In both sections, the transition from Upper Permian the Late Permian marine regression (Dolenec, 2005). to Lower Triassic is characterized by a major abrupt shift in carbonate carbon δ 13C and δ 18O from heavier to lighter values (Fig. 5). The data suggests that the carbon isotope variability DAY 1, STOP 1/3 – BLED: Ladinian rifting event at the P/T boundary reflects global changes in the carbon cycle and/or climate changes, probably controlled by the Late Perm- Indirect evidence of a late Anisian – early Ladinian extensional event related to the Neotethys rifting is found on the Ojstrica hill on the western edge of Lake Bled (Fig. 6). This extensional event resulted in widespread fragmentation of the entire region, creating the large Slovenian Basin and numerous short-lived basins next to it. The Ojstrica hill is made up of coarse breccias deposited in a small-scale (half)graben (Fig. 7). The base of the studied sequence consists of the shallow-marine Anisian dolomite. This dolomite-dominated formation may laterally pass into limestone (an example of which is the Bled Caste mound), characterized by calcimicrobial grains and crusts (Flügel et al., 1994; Ogorelec, 2011). The Anisian dolomite is overlain by 6 m of Ladinian volcanic rocks (riolite and pelitic tuff), showing that the extensional event was accompanied by volcanic activity. The uppermost part of the Ojstrica hill consists of differently coloured Ukve/ Fig. 4: Košutnikov potok section exposes the P/T fault contact between Uggovizza Breccia 45 m thick, in which bedding is visible in the the Karavanke and the Werfen formations (photo: M. Novak). lowest 10 m. Breccia is composed of centimetre-sized clasts and 79 15TH WORKSHOP Fieldtrip guide. 15th Emile Argand Conference on Alpine Geological Studies, 12-14 September 2022, Ljubljana, Slovenia. usually has a reddish coloured matrix. The uppermost part of the formation is more coarse-grained. The clasts can reach up to several metres in size and the matrix is usually grey. The clasts are almost invariably carbonates, mostly limestones. The com- position and age of the rocks vary widely but can be assigned to underlying formations (Permian Neoschwagerina Limestone, Lower Triassic Werfen, and Anisian dolomite/limestone fms). Since all these formations outcrop in the immediate vicinity of the Ojstrica Hill, the clasts are of rather local origin. Despite the limited outcrops of the Ukve/Uggovizza breccia on the Ojstrica hill, we assume that the sedimentary basin was a rather small (half) graben, which was quickly filled up with coarse-grained local carbonate material. Above, the carbonate platform reinstalled quickly, and shallow marine limestones of the Schlern Formation were deposited in the Late Ladinian and Figure 6: Locations of the Ojstrica hill (STOP 1/3) ana Pokljuška soteska Early Carnian. In the Bled area these were diagenetically altered (STOP 1/4). Figure 7: Detailed geologic map and stratigraphic column of the Ojstrica hill: the Ukve/Uggovizza breccia, deposited in a small (half) graben, reaches a thickness of 45 m and is in stratigraphic contact with the underlying sequence and in fault contact with the overlying sequence; however, according to regional data, probably passes upward into carbonates of the Schlern Formation, which is due to late Ladinian platform progradation. 80 15TH WORKSHOP Fieldtrip guide. 15th Emile Argand Conference on Alpine Geological Studies, 12-14 September 2022, Ljubljana, Slovenia. to coarsely crystalline saharoid dolomite. Halfgrabes with a sim- ilar sedimentary record are well known from other localities in the Julian and Kamnik-Savinja Alps (Celarc et al., 2013). DAY 1, STOP 1/4 – POKLJUŠKA SOTESKA: Upper Triassic Bled Basin The uppermost Ladinian – Lower Cretaceous formations that make up the Pokljuka Nappe between Lakes Bled and Bohinj comprise slope and basin floor sediments. For a long time, these sediments were considered to have been deposited in a shal- lower side-branch (embayment) of the Slovenian Basin (Buser, 1989, 1996). However, the Pokljuka Nappe is now considered to derive from the distal part of the continental shelf, for which the name Bled Basin has been proposed (Cousin, 1981; Kukoč et al., 2012; Goričan et al., 2018). The succession of the Bled Basin starts with an interchange of Ladinian (perhaps already upper Anisian?) micritic limestone, tuff, and volcanics (Buser, 1980), equivalent to the Buchenstein Formation in the South- ern Alps (Fig. 8). The same or similar formation occurs also in other parts of the Julian and Kamnik-Savinja Alps, perhaps also in the Dinarides area (e.g. Kolar-Jurkovšek et al., 1983), suggesting palaeotopography with numerous smaller basins separated by platforms. While prograding platforms sealed off most of the smaller basins (e.g. Skaberne et al., 2003), basinal sedimentation continued in the Bled Basin with the deposition of the Zatrnik (or Pokljuka) Formation. A typical lithology of this formation is bedded limestone with chert (Diener, 1884; Härtel, 1920; Budkovič, 1978; Cousin, 1981; Buser, 1986), but some considerable differences can be noted between different parts of the formation. The lowermost, upper Ladinian part is dominated by thin- to medium-bedded bioclastic wackestone and radio- larian-peloid packstone. Distal calciturbidites with peloids, mi- critic intraclasts, fragments of sponges, and microproblematica dominate in the Carnian part of the succession. Thicker beds of micritic limestone with chert nodules, sporadically interchanging with calciturbidites, become dominant at the transition into the Norian (Gale et al., 2019). In the upper part of the formation, dated as Lower Jurassic, pinkish calciturbidites rich in echino- derms and thin-shelled bivalves are the typical lithology of the Zatrnik Formation (Gale et al., 2022). Slumping is common in all parts of the formation, but is probably more intense in its up- permost part (Kukoč et al., 2012; Gale et al., 2019, 2021). The Zatrnik Formation is followed by Pliensbachian calcarenites and breccias of the Ribnica Breccia unit (the rest of the succession is described in STOP 2/1). Although the aspect of the Zatrnik Formation varies, the largest part of it consists of medium-bedded micritic limestone with chert nodules. Stop 1/4 is in a natural amphitheatre of the Pokl- juka Gorge (Fig. 6), a dry gorge formed at the beginning of the Holocene by the waters running from a retreating glacier. Norian age of the limestone was proven here on the basis of conodont elements. Figure 8: Generalized succession of the Bled basin with the Pokljuška soteska section positioned in the lower part of the Zatnik Formation (Gale et al., 2012; modified from Goričan et al., 2018). 81 15TH WORKSHOP Fieldtrip guide. 15th Emile Argand Conference on Alpine Geological Studies, 12-14 September 2022, Ljubljana, Slovenia. DAY 2, STOP 2/1 – STUDOR: present but rare. Intraclasts of pelagic calpionellid wackestone Oldest Alpine Flysch with sponge spicules and rare planktonic foraminifers are also present. Single bioclasts are common and include fragments Along the road from Srednja vas to Uskovnica in the Bohinj of algae, sponges, bryozoans, echinoderms, and thick-shelled area the topmost part of the Bled Basin succession is exposed bivalves. Well-developed concentric and radial ooids and (Fig. 9). It consists of the Biancone Limestone, Bohinj Brec- oncoids are present as isolated grains. Rare chert grains and cia, and Studor formations, the latter representing the oldest lithic grains of igneous origin, including basalt, also occur in Alpine flysch deposits in western Slovenia. Tithonian to Lower the breccia. Cretaceous Biancone Limestone overlies Bajocian to Tithonian radiolarian cherts. It is represented by a succession of pelag- Calcarenite is predominantly composed of shallow-water ic limestone approximately a 100 m thick, of which only the skeletal fragments and lithoclasts similar to those found in the uppermost part is exposed at this locality. It is characterized breccia. Lithic grains of igneous origin, grains of chert, and by thin- to medium-bedded light grey to white limestone with opaque grains are present but less abundant than the carbon-discontinuous beds of dark-grey chert and irregularly shaped ate components. chert nodules. Intercalations of marl are also present. The predominant microfacies are radiolarian-rich wackestone and The microfacies analysis reveals that the main source area of packstone. Parallel lamination is present in some layers. In the resedimented limestone was a penecontemporaneous car-places, normally graded calcarenites occur as several interca- bonate platform. This platform (named the Bohinj Carbonate lations centimeters thick in micrite beds and contain intraclasts Platform by Kukoč et al., 2012) may have developed on top of of wackestone with radiolarians and chert clasts up to 5 mm a nappe stack, which formed during the early emplacement of in the basal part. Radiolarians extracted from the Biancone the internal Dinaric units onto the continental margin. Grains limestone indicate a latest Tithonian to earliest Berriasian age of basalt indicate ophiolitic origin. (Kukoč et al., 2012). Reddish siliceous limestone similar to the Biancone limestone, Carbonate gravity flow deposits consist of 3 m of carbonate from which it differs with its higher proportion of marl and breccia and 4 m of calcarenite and are called the Bohinj Forma- red colour, is found above the Bohinj Formation at this locality. tion (Kukoč et al., 2012). Slump folds are present in the brec- Latest Tithonian to early Valanginian age of this limestone is cia. The calcarenite is massive and shows no internal folding or inferred based on radiolarians (Kukoč et al., 2012). bedding. The breccia consists primarily of matrix-supported an- gular to subangular shallow-water carbonate clasts up to 2 cm Mixed carbonate-siliciclastic deposits called the Studor For-in diameter. The matrix is radiolarian-rich lime mudstone with mation (Kukoč, 2014; Goričan et al., 2018) are exposed in sponge spicules and scarce calpionellids. Most of the limestone the Vrčica Gorge (Fig. 10). Owing to its lithological charac-clasts are bioclastic grainstones and bioclastic-peloidal pack- teristics the Studor Formation represents a unique and easily stones. Clasts of algal wackestone and oncoid packstone are distinguishable lithostratigraphic unit in the wider area and is considered the oldest body of Alpine flysch-type deposits in Slovenia. The formation starts with beds of light gray radiolarian wacke- stone/packstone 5–10 cm thick intercalated with thin-bedded sandstone, which is less frequent in the lower part of the for- mation. Calcarenite beds are rare. Micrite beds contain chert in places. In the upper part of the formation proportion of marl is higher and micrite and calcarenite beds become subordinate to sandstone. The sandstone beds in this part are up to 1 m thick. Horizontal and cross lamination is observed. The uppermost part of the formation is composed of two olistostrome layers composed of centimeter- to meter-sized blocks of different lithologies in a dark gray sandy matrix. Laminated micritic limestone with radiolarians (Biancone facies) prevails among these olistolithes. Carbonate breccia with limestone and chert clasts is also present, as well as smaller, decimeter-sized clasts of dark green and red chert. Carbonate lithic grains represent approximately 40 % of all lithic grains in sandstone. For the most part, those are small micrite grains, however larger grains of peloidal and bioclastic Figure 9: Locations of Studor (STOP 2/1) and Podbrdo (STOP 2/2). grainstone and packstone also occur. Isolated bioclasts and 82 15TH WORKSHOP Fieldtrip guide. 15th Emile Argand Conference on Alpine Geological Studies, 12-14 September 2022, Ljubljana, Slovenia. echinoderm fragments are rare. Non-carbonate components predominantly include fragments of mafic rocks. Grains of ba- salts predominate, with grains of serpentinite, chert, amphibo- lite, phyllites, quartzite, granitoid rocks, and quartz sandstone are also present. Quartz grains represent approximately 10–20 % of grains and are mostly monocrystalline; however, polycrys- talline quartz of metamorphic origin also occurs. Heavy miner- als make up less than 10 % of all grains. Matrix of sandstone is micritic with an admixture of a clay component. The composition of the sandstone indicates a composite source of material. Shallow-water carbonate clasts, especially iso- lated bioclasts, indicate the proximity of an active carbonate platform, while siliciclastic admixtures indicate the erosion of ophiolites and underlying metamorphic soles. Radiolarians from the lower part of the Studor Formation are assigned to a relatively broad range from the latest Tithonian– earliest Berriasian to the latest Valanginian–earliest Hauteriv- ian due to poor preservation (Kukoč, 2014). The Valanginian – Hauterivian age of the Studor Formation was previously determined using nannoplankton (Buser et al., 1979), but the exact position of the dated sample within the described section is not known. DAY 2, STOP 2/2 – BOHINJSKA BISTRICA – PODBRDO RAILWAY TUNNEL: Thrust structure of the Southern Alps The eastern part of the Southern Alps is composed of four major nappes. The lowest is the Tolmin Nappe, which is in the upwards direction followed by the Krn (Julian), Slatna, and Pokljuka nappes. The Tolmin Nappe consists of Slovenian Ba- sin successions. It is generally divided into three lower-order nappes, the lowest Podmelec, the middle Rut, and the highest Kobla nappes. The major part of the Southern Alps is composed of the next two nappes, both composed of the Julian Carbonate Platform successions. The Krn Nappe consists of rather contin- uous late Paleozoic to Early Jurassic shallow-marine carbonate, and a subordinate clastic succession, with two deeper marine intervals: rifting-related Ladinian and eustatic at the Carnian/ Norian boundary. Within the Krn Nappe sporadic, locally occurring, post-drowning mid-Jurassic and Cretaceous deeper marine sediments (Ammonitico Rosso, Biancone, Scaglia fa- cies) occur. Next is the Slatna Nappe, which forms the highest peaks of the Julian Alps, including Mt Triglav, and is composed solely of the Middle – Upper Triassic (Ladinian – Carnian) massive carbonates. The topmost Pokljuka Nappe is composed of the Bled Basin succession that originated out of the outer, i.e. oceanward side of the Julian Carbonate Platform. It is com- posed of Ladinian to Early Cretaceous deep marine sediments (STOP 1/4), including the oldest Alpine flysch in this part of the Southern Alps (STOP 2/1) (for further reading see Placer, 1998, 2008; Goričan et al., 2018). Figure 10: Sedimentological section of the Studor Formation with posi- tions of radiolarian datations marked (Kukoč, 2014) 83 15TH WORKSHOP Fieldtrip guide. 15th Emile Argand Conference on Alpine Geological Studies, 12-14 September 2022, Ljubljana, Slovenia. Figure 11: Thrust structure of the eastern part of the Bohinj Range as seen from the village of Podbrdo. The highest peaks belong to the Krn (Julian) Nappe composed of Julian Carbonate Platform rocks, whereas on the southern slopes several thrust lower-order units of the Tolmin Nappe are composed of the Slovenian Basin succession. The nappe structure of the eastern Southern Alps is most clear- (as in the major part of the basin), and above Bača Dolomite, ly visible on the southern slopes of the Bohinj Range (Fig. 9). the calcareous Slatnik Formation is preserved. It is composed The top of the range is composed of the Krn Nappe, whereas of micritic limestone that in the upper section contains more the lower parts belong to the Tolmin Nappe (Figs. 11, 12). abundant calciturbidites and calcidebrites. It records the latest Triassic progradation of the Julian Carbonate Platform towards According to Buser (1987), all three lower-order nappes of the the Slovenian Basin (Rožič et al., 2009, 2013; Gale, 2010). The Tolmin Nappe in the slopes between Podbrdo Village and Mt. Hettangian – Pliensbachian Krikov Formation is composed pre- Črna prst are visible. In general, the succession is similar to the dominantly of resedimented limestones composed of ooids in Tolminske Ravne section (STOP 2/3), so herein only the ma- the major part, and crinoids/lithoclasts in the upper part. This jor differences between them will be outlined. The Podmelec change documents the initial drowning of the Julian Carbonate Nappe forms the village of Podbrdo surroundings and consists, Platform (described bellow), which was a source area for these in this area, of the Maastrichtian Upper Flyschoid Formation resediments. The rest of the succession (Toarcian Perbla Fm, (see also STOP 3/1). Above the thrust-plane, the Rut Nappe Aalenian – Lower Tithonian Tolmin Fm, Upper Tithonian – Ber-starts with Upper Cenomanian – Turonian “globotruncana riasian Biancone Limestone Fm and Aprian – Turonian Lower limestone” (described in Cousin (1981) as the upper portion Flyschoid Fm) is dominated by pelagic deposits, whereas of the Lower Flyschoid Formation and in Buser (1986) as a carbonate resediments (known in other parts of the basin) are separate formation), passes through Coniacian – Campanian largely absent in this nappe (Rožič, 2006, 2009; Goričan et al., Volče limestone and again into the Upper Flyschoid Formation. 2012a). This is also attributed to the paleogeographic position Between the Rut and Kobla Nappes a small-scale Mačji potok of the Kobla Nappe succession, which was located adjacent thrust sheet is intercalated. This part was previously described to the Julian Carbonate Platform, and which received large as the Carnian Kobla Formation, but detailed study revealed quantities of shedded carbonate until carbonate drowning, and that it is a thrust-sheet composed of Jurassic beds very similar starved from resediments afterwards (Rožič and Šmuc, 2009; to those from the Tolminske Ravne section (Svetličič, 2011). Rožič et al., 2014). Morphologically, the Kobla Nappe is beautifully expressed. It starts with Carnian “Amphiclina beds” that are, in this nappe, The uppermost part of the Bohinj Range is composed of the composed almost exclusively of micritic limestone with chert, Krn Nappe, which is in this area composed almost exclusively with sporadic resedimented limestones and some marl films of the Norian – Rhaetian Dachstein Limestone that is developed between the beds. Upwards, the succession is similar to Tol- in the loferitic facies. However, data from the 115 year-old Bo-minske Ravne section with some prominent variations: A) hinjska Bistrica – Podbrdo railaway tunnel reveal that the con-the Upper Norian – Rhaetian succession is not dolomitized tact between the Slovenian Basin and Julian Carbonate Plat-84 15TH WORKSHOP Fieldtrip guide. 15th Emile Argand Conference on Alpine Geological Studies, 12-14 September 2022, Ljubljana, Slovenia. Figure 12: Two cross-sections through the eastern part of the Bohinj Range (modified from Kossmat (1907). Stratigraphy is corrected according to Buser (1987) and particularly in the central parts according to Rožič, (2006, 2009) and Rožič et al. (2009, 2013, 2014)): The upper cross-section is directly above the Bohinjska Bistrica – Podbrdo railway tunnel and shows the steeply dipping contact between the Krn and Tolmin nappes, whereas the lower cross-section is across the Mt. Črna Prst, where the contact between the nappes is a thrust fault. form successions in the eastern part of the Bohinj Range (Kobla DAY 2, STOP 2/3 – TOLMINSKE RAVNE: area) is not a thrust, but a steeply inclined, N-deeping fault Slovenian Basin succession (Kossmat, 1907). In the northern slopes of the Bohinj Range Boštjan Rožič (between Mt. Kobla and Bohinjska Bistrica) the succession of the Julian Carbonate Platform begins with Norian – Rhaetian The Slovenian Basin is probably the most prominent and lon-Dachstein Limestone in loferitic as well as reefal development gest lasting deep-marine paleogeographic unit in present-day (Buser, 1987; Turnšek and Buser, 1991; Turnšek, 1997). Early Slovenia. Its foundation was formed during a Ladinian exten-Jurassic is characterized by ooidal limestone overlain by bio- sional event related to the Neotethys opening, and its margins clastic/crinoidal limestone, the latter documenting the initial were defined after late Ladinian progradation of surrounding (Pliensbachian) deepening of the platform (Rožič and Šmuc, platforms. This lasted until the end of the Cretaceous, when it 2009; Rožič et al., 2014). Above, with the stratigraphic gap, turned into a typical foreland basin with the sedimentation of end-Jurassic – earliest Cretaceous Biancone Limestone is over- the flysch. Today, it is found in the Tolmin Nappe and can be lain. As described below, this progressive deepening of the plat- traced in the foothills of the Alps, from the town of Tolmin in form is well manifested also in the adjacent Slovenian Basin the west to the Celje on the East, where these basinal succes-succession. In the area around Bohinjska Bistrica, i.e. at the toe sions become covered with Paratethys sediments (Buser, 1989, of the northern slopes of the Bohinj Range, Oligocene clastics 1996; Goričan et al., 2012b; Rožič, 2016; Rožič et al., 2018). are deposited with the stratigraphic gap above the lowest part of the Dachstein Limestone Formation. These Oligocene beds The section along the road between the villages of Perbla and are also the westernmost outcrops of the Paratethys sediments Tolminske Ravne probably represents the most classical Slo-in this part of the Alpine region (Kossmat, 1907; Buser, 1987). venian Basin succession (Fig. 13), as three formation type-lo-Such geological characteristics reveal that the internal struc- calities are found in this area (Cousin, 1981; Rožič, 2009). ture of the eastern Southern Alps is surely further complicated Along the road that climbs the northern limb of the large and additional studies are needed for more comprehensive anticline latest Norian – Albian strata is exposed (Fig .14). stratigraphic/structural interpretations. The Norian – Rheatian is marked by carbonate sediments that were dolomitized to the Bača Dolomite Formation; i.e. bedded dolomite with chert nodules (1 in Fig. 14). Due to dolomitiza- 85 15TH WORKSHOP Fieldtrip guide. 15th Emile Argand Conference on Alpine Geological Studies, 12-14 September 2022, Ljubljana, Slovenia. and Upper Jurassic is characterized by pelagic siliceous lime- stones (4A in Fig. 14) and later, radiolarian cherts (4B in Fig. 14) (Cousin, 1981; Buser, 1989) known as the Tolmin Forma- tion (Rožič, 2009; Goričan et al., 2012a). Only in the southern and central parts of the basin resedimented limestones occur sporadically and wedge out towards the north. In the Tolmin- ske Ravne area, these occur as rare calcarenitic beds in the middle (Bajocian – Callovian) and uppermost (Lower Titho- nian) part of the formation. The source area of these beds was the south-lying Dinaric Carbonate Platform. In recent years, it was shown that the lower interval passes southwards into limestone breccia several-tens-of meters thick, which indicates the major middle Middle Jurassic collapse and the southward retreat of the Dinaric Carbonate Platform margin (Rožič et al., 2018; submitted). This event coincides with major tectonic perturbation in the Alpine Realm, reflecting the oceanisation (or at least lithospheric breakup) (Ribes et al., 2020) of the Alpine Tethys and the initiation of the intra-oceanic subduction in the Neotethys (Gawlick et al., 2017; Schmid et al., 2020). The Jurassic ends with the upper Tithonian to Berriasian Bian- cone Limestone Formation (5 in Fig. 14) (Cousin, 1981). The change from radiolarian cherts to Biancone Limestone is sharp and characteristic for the entire region (Goričan, 1994; Šmuc, 2005; Clari and Masetti, 2002; Martire et al., 2006). Early Cretaceous (Valanginian – Barremian) is marked by a Figure 13: Location of the Tolminske Ravne (STOP 2/3). prominent stratigraphic gap and the sedimentation reoccurs in the Aptian with locally thick limestone breccia (Cousin, 1981; tion, detailed sedimentological analysis is not possible, but the Buser, 1989). The breccia forms a base of the Aptian – Turonian formation surely sedimented in a deep-marine environment Lower Flyschoid Formation generally characterised by a rather (Gale, 2010). The overlying Hettangian – Pliensbachian Krikov monotonous alternation of pelagic marls and resedimented Formation begins with an interval of basal limestone breccia limestones, mainly calciturbidites (Cousin, 1981; Buser, 1986, several tens of meters thick (2A in Fig. 14), which records 1989). In the Tolminske Ravne area this formation, however, the earliest Jurassic rifting pulse connected to the opening of exhibits great vertical as well as some lateral changes. Solely in the Alpine Tethys (Rožič et al., 2017). Upwards, it passes into the southern limb of the anticline it begins with channelized, the alternating calciturbidites and hemipelagic limestone with marl-supported olistolithic breccia several tens of meters thick chert nodules (2B in Fig. 14). Within the basin, calciturbidites (6A in Fig. 14). Towards the northern limb, this bed wedges start to prevail towards the north, which indicates the Julian out. Upwards, the formation starts with limestone breccia (6B Carbonate Platform as a main source of the resediments during in Fig. 14), which passes into a marl-dominated interval (6C in this period (Rožič, 2006, 2009). In the lower part, resediments Fig. 14), again into the calciturbidite-dominated interval (6D in are characterised by ooids, whereas in the upper part crinoids Fig. 14), further to a marly interval with manganese (6E in Fig. and lithoclasts become predominant. This change in compo- 14) (probably recording Bonarelli OAE level) and then again a sition reflects the gradual drowning of the Julian Carbonate calciturbiditic interval (6F in Fig. 14) (the last two intervals do Platform, which is related to the late Early Jurassic rifting not outcrop along the road). An abundance of carbonate grav-phase of the Alpine Tethys (Rožič and Šmuc, 2009; Rožič et al., ity-flow beds in the Tolminske Ravne section indicates their 2014). Furthermore, the demise of shallow water sedimenta- proximal position to the carbonate material source area, which tion on this platform at the end of the Pliensbachian (Šmuc, was the Dinaric Carbonate Platform. This is in obvious contrast 2005; Šmuc and Rožič, 2010) is directly recorded in the sharp to the underlying Jurassic formations, which is explained by upper boundary of the Krikov Formation (Rožič, 2009; Rožič major tectonic perturbation of the Dinaric Carbonate Platform and Šmuc, 2011). and Slovenian Basin transitional area that occurred between the two periods. The Toarcian is marked by the marl-dominated Perbla Forma- tion (3 in Fig. 14), a succession typical of this stage throughout The rest of the Cretaceous (which will not be visited) is marked the entire Alpine Realm (Cousin, 1981; Rožič, 2009; Rožič and by the Coniacian to Campanian Volče Limestone Formation (7 Šmuc 2011). In the first metre, calcareous shale is black and in- in Fig. 14), which is dominated by light grey pelagic limestones tensively impregnated with manganese, which is characteristic with globotruncanids and rarer calciturbidites (Ogorelec et al., of the early Toarcian OAE (Jenkyns et al., 1991). The Middle 1996; Buser, 1989). We note that all of the above-described 86 15TH WORKSHOP Fieldtrip guide. 15th Emile Argand Conference on Alpine Geological Studies, 12-14 September 2022, Ljubljana, Slovenia. Figure 14: Detailed geological map and stratigraphic column of the Tolminske Ravne area (after Rožič, 2006, 2009): the visited part of the succession is situated within the Rut Nappe, a middle lower-order thrust unit of the Tolmin Nappe that is entirely composed of a continuous Late Triassic to end-Cretaceous Slovenian Basin succession, which sedimented in the central part of the basin. 87 15TH WORKSHOP Fieldtrip guide. 15th Emile Argand Conference on Alpine Geological Studies, 12-14 September 2022, Ljubljana, Slovenia. cretaceous carbonates are to some degree replaced by nodular the Dinaric Carbonate Platform’s northern margin, from the chert. The succession of the Slovenian Basin ends with latest inner platform succession through slope sediments to the deep Campanian – Maastrichtian Upper Flyschoid Formation (8A and marine deposits. 8B in Fig. 14) that closely resembles the Aptian to Cenomanian part of the Lower Flyschoid Formation but lacks any silification Above, with the angular unconformity, the end Cretaceous of carbonate lithologies. Upwards, it gradually turns into flysch Lower Flyschoid Formation is deposited. Upper Cretaceous fly-deposits, i.e. contains progressively more abundant siliciclastic sch deposits occur in both the Southern Alps and the Dinarides turbidites (Cousin, 1981; Buser, 1989). and chronostratigraphically belong to the Maastrichtian, and partly to the Upper Campanian (Buser, 1996)(see also STOPs 2/2 & 2/3). In the Dinarides, i.e. in the northern part of the DAY 3, STOP 3/1 – AVČE: Trnovo Nappe, the formation begins with the basal limestone End-Cretaceous flysch on the northern margin of breccia that is deposited with a pronounced erosional uncon- the Dinaric Carbonate Platform formity on older platform carbonate rocks (Buser, 1987, 2010; Boštjan Rožič, Andrej Šmuc Miklavič and Rožič, 2008). As described above, basal limestone breccia locally overlies older basinal successions. The thickness Structurally, the Avče area belongs to the northernmost part of this basal package varies considerably, but often exceeds 100 of the Trnovo Nappe, which is the highest structural unit in m (Buser, 1986). The following flysch sequence can be divided the Dinaric nappe stack (Fig. 15). It is characterized by Upper into a lower and an upper part (Buser, 2010). In the lower Triassic and Early Jurassic shallow marine, often loferitic do- part, the flysch contains thick layers (in places more than 10 lomites and limestone (Main Dolomite, Dachstein Limestone, m) of limestone breccia with intercalated fine-grained calcitur-Podbukovje fms). At the Triassic Jurassic boundary, interlayers bidite and siliciclastic layers. In the upper part, the content of of limestone breccia beds are common (Ogorelec and Rothe, limestone layers decreases, while the grain size and abundance 1992). Above the stratigraphic gap, 30 meters of poorly dated of siliclastic turbidites increases. (probably end-Jurassic) crinoidal/tubiphytic calcarenites are deposited. They are overlain by olistolithic limestone breccia In the Avče area, the basal portion of the flysch deposits out-with muddy matrix with calpionellas (Kovač, 2016). In the crops along the Soča River (Fig. 16). The section begins with northern part of the Avče area, i.e. north of the E-W trending an internally bedded limestone breccia two meters thick that paleofault, the Volče Formation, which is several tens of meters gradually changes to fine-grained parallel and cross-laminat-thick, is outcropping (for description see STOP 2/3) (Ogorelec ed calcarenites. Later in the section, marl packages alternate et al., 1976). This succession records the gradual drowning of with rare beds of fine-grained siliciclastic turbidites, micritic limestones, and calciturbidites. The calciturbidites are medium bedded and show poorly defined partial Bouma sequences. An exception is a few layers of basal breccia more than one meter thick, overlain by a sharp contact with calcarenites in which partial Bouma sequence is preserved. The dominant layer in the Avče section is a package of limestone breccia 10 meters thick. It begins with a blocky limestone breccia with a marly matrix deposited on an erosional contact. The marl package, which lies directly beneath the breccia, has an unusual reddish colour, is plastically deformed, and contains large rip-up clasts that are in places still partially attached. The rip-up clasts are also present in the overlying lithologies. This breccia is overlain with erosion- al contact by a finer-grained breccia bed up to 7 m thick that sharply grades to calcarenite showing the Tb and Tc part of the Bouma sequence. The uppermost part of the section is marked by marls, with interbedded thick-bedded siliciclastic sandstones. The Avče section represents a typical deep-sea foreland succes- sion characterised by pelagic marls and limestones interbedded with various gravity-flow deposits. The composition of the cal- citurbidites/debrites (composed of contemporaneous bioclasts and diverse lithoclasts) indicates that they originated from the margins of the Dinaric Carbonate Platform, where rudist thick- ets predominated. In addition, the lithoclasts indicate a highly dissected slope between the basin and the platform, where car- bonate rocks of a wide range of structural types and sedimentary Figure 15: Locations of Avče (STOP 3/1) and Anhovo (STOP 3/2). environments were eroded. The formation of the thick limestone 88 15TH WORKSHOP Fieldtrip guide. 15th Emile Argand Conference on Alpine Geological Studies, 12-14 September 2022, Ljubljana, Slovenia. Figure 16: Distribution of flysch in western Slo- venia (upper left) with ages generally growing younger towards SW; generalized stratigraphic column of the Avče area recording the gradual deepening of the Dinaric Carbonate Platform’s northern margin (lower left); and a detailed sedimentological section (right) of the Upper Flyschoid Formation logged along the banks of the Soča River. 89 15TH WORKSHOP Fieldtrip guide. 15th Emile Argand Conference on Alpine Geological Studies, 12-14 September 2022, Ljubljana, Slovenia. breccias is related to the tectonic breakup of the Dinaric Carbon- area, however, the Paleocene flysch is separated from the older ate Platform. The sandstones in the Avče section were formed carbonate rocks by regional faults (Ogata et al., 2014). by distal turbidite flows. The origin of the grains was a mixed siliciclastic-carbonate shelf in the area of the internal thrust belts The Salonit Anhovo quarry boasts spectacular outcrops of of the uplifting Alpine-Dinaric orogeny. extremely large sedimentary bodies formed by various types of gravity mass flows (Fig. 17). In terms of size (up to 260 m thick), extent (100 km long), and mode of formation, these bod- DAY 3, STOP 3/2 – ANHOVO: ies extend from the Anhovo area to northeastern Italy (Ogata et Mass-flow megaevents of the Paleogene flysch al., 2014). Their internal organization is characterized by a re- Andrej Šmuc, Boštjan Rožič peating sequence of lithologic units. These large megasequences exhibit thinning and finning upward trends. They generally be- Like the Avče area (STOP 3/1), the Anhovo area also belongs gin with massive blocky carbonate breccias with a marly matrix to the Trnovo Nape, but is located in the southern part of this (unit 1), followed by blocks of carbonate breccias and eroded structural unit (Fig. 15). In contrast to the Avče area, this area bedrock in a marly-siliciclastic matrix (unit II) (Fig. 17). These is marked by more continuous shallow marine carbonate suc- breccias are overlain with a sharp contact at the horizon of nor-cession, which persisted almost up to the end of the Cretaceous mally graded carbonate breccias – calcirudites (Skaberne, 1987; (Buser, 2010; Jež and Otoničar, 2018). Above, with the strati- unit III) that grade into calcarenites (unit IV). The entire series is graphic gap the Paleogene flysch is deposited. In the Anhovo terminated by a pelagic rock stack of laminated to massive marls Figure 17: Generalized stratigraphic column of the Paleocene flysch in the Salonit Anhovo quarry (left) marked by three “megacyclothemes”, large olistolith of Cretaceous limestone within Perunk “cyclotheme” (upper right), and large flysch plasticlast from the U2 unit of the Perunk “cyclotheme” (lower right). 90 15TH WORKSHOP Fieldtrip guide. 15th Emile Argand Conference on Alpine Geological Studies, 12-14 September 2022, Ljubljana, Slovenia. (unit V). According to Ogata et al. (2014), these deposits formed drowning in the Eocene (Buser, 1989, 1996). The Kras (Karst) in the proto-dinaric orogen during the process of the collapse area structurally belongs to the Komen Thrust Sheet (Placer, of the submarine shelf or its sliding (with characteristic plastic 1999), which consists of the platform succession beginning in deformation of the base) into the deeper part of the developing the Cretaceous, exhibiting prominent disconformity in the Maas-foreland-type inner basin. trichtian and lasting until the final destruction and subsidence of Despite many years of geological research, the exact strati- the platform in the lower Eocene (Otoničar, 2007; Jurkovšek et graphic position of the deposits in the Anhovo quarry is still al., 2013). unknown. Based on the rich presedimented rudist assemblage and nanoplankton communities, the rocks of the lowermost The Škocjan Caves, together with the Kačna Jama cave, belong part of the Anhovo sequence are of Upper Paleocene, or more to the first few kilometres of the Reka River underground flow precisely, Thanethian age (Pleničar et al., 2001; Pogačnik, that is still accessible from the surface. In this area (Figs. 18, 19), 2003; Pleničar and Jurkovšek, 2009). On the other hand, the the oldest rocks belong to the Repen Formation (Cenomanian – resedimented planktonic foraminifer Morozovella velascoensis Turonian) representing limestone with pelagic fossils (Jurkovšek found in the middle part of the sequence points to the lower et al., 1996). The karst surface and underground of the Škocjan Eocene. Caves is composed of three lithological units (Jurkovšek et al., Due to the specific chemical and lithological composition of 1996, 2013). The oldest rocks belong to the Sežana Formation the lithologic members of the megacyclothems, these rocks (Turonian – Santonian) representing bedded limestone with rare are mined in open pits and used for the production of Portland rudist biostromas (Jurkovšek et al., 1996, 2013). The Sežana cement. To ensure safety during mining operations, various Formation is some 400 to 500 m thick. Above the Sežana Forma-geophysical methods have been employed, from geoelectrics tion we have the Lipica Formation (Santonian – Campanian) in (Pogačnik, 2010) to shallow radar (Zajc et al., 2014). the normal stratigraphic position with a thickness of 250 to 400 m (Jurkovšek et al. 1996, 2013). The Lipica Formation is repre- sented by bedded and massive limestone with rudist biostromas DAY 3, STOP 3/3 – ŠKOCJAN CAVES: and biohermas (Jurkovšek et al., 1996). The Liburnian Forma- Inside karst of the Dinaric Carbonate Platform tion (Maastrichtian – Paleocene) represents bedded limestones Stanka Šebela (with alveolinae) with a thickness of 50 to 300 m (Jurkovšek et al. 1996, 2013). The youngest rocks in this area are composed of The Dinarides of western Slovenia are dominated by a thick Slivje limestone (bedded, mainly miliolid limestone) within the Upper Triassic to Eocene carbonate succession of the Dinaric Liburnian Formation (Pc). Carbonate Platform also known as the Friuli (in Italian litera- ture) and Adriatic or Dinaric-Adriatic Carbonate Platform (in Croatian literature). The platform installed above the Carnian clastic deposits and continued in the SE part until its final Figure 19: Geology of the area of the Škocjan Caves and Kačna Jama, SW Slovenia. 1–fault with dextral horizontal strike-slip movement, 2– syncline, 3–Repen Formation (K21,2), 4–Sežana Formation (K22-4), 5–Lipica Formation (K24-5), 6–Liburnian Formation (K–Pc), 7–Slivje Figure 18: Location of the Škocjanske Caves (STOP 3/3). limestone within the Liburnian Formation (Pc). 91 15TH WORKSHOP Fieldtrip guide. 15th Emile Argand Conference on Alpine Geological Studies, 12-14 September 2022, Ljubljana, Slovenia. Passages of the Škocjan Caves are developed inside a lithologi- The Reka River only flows aboveground for some 50 km. Under-cal column 300 m thick of Cretaceous and Paleocene limestones ground, it flows through the Škocjan Caves towards the NW to (Šebela, 2009). Underground, the Reka River in the Šumeča Kačna Jama (20 km long and 280 m deep). However, the cave Jama and the Hankejev Kanal flows largely within 130 m-thick systems are not connected, as they are separated by some 870 Lipica Formation and follows in the direction of the bedding m of air distance. The Reka River emerges after 35 km from plane. The bedding planes with interbeddes slips were especially underground as the Timavo spring in Italy. Between Kačna Jama favourable for the development of the initial cave passages and the Timavo springs there are other vertical cave accesses to (Knez, 1996; Mihevc, 2001; Šebela, 2009). underground water flow. The extreme flood of 1965 reached a level of 321 m above the sea and caused the waters in Martelova The Škocjan Caves are the only karst cave in Slovenia inscribed Dvorana to rise to a level of 107 m (Mihevc, 2017). as UNESCO natural heritage since 1986. The caves are 6474 m long and 254 m deep (Fig. 20) with the lowest point at 212 The remains of older cave passages take the form of roofless m (Mrtvo Jezero). Martelova Dvorana boasts a volume of 2.55 caves or denuded caves. The longest roofless cave is 1800 m million m3 and is the 11th largest cave chamber in the world long and is situated at an elevation of 440 to 450 m above sea and the 2nd largest in Europe (Walters and Zupan Hajna, 2020). level (Mihevc, 2001), and can be traced in the area north from Hankejev Kanal passage. If we presume that the roof above what is today a roofless cave was about 150 m high and that the denudation rate is 20 to 50 m per 1 million years, this cave system could be some 3 – 7.5 million years old (Mihevc, 2001, 2017; Zupan Hajna et al., 2008). The second speleological peri- od represents passages at elevations of 340 to 300 m above sea level, as Tominčeva Jama, the upper part of Šumeča jama, and Tiha Jama. During the third period, the strong down-cutting of the water through the limestones was first active in Martelova Dvorana and later in the Hankejev Kanal and Šumeča Jama. 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FIELDTRIP B László Fodor1, Kristina Invančič2, Marian Janák3, Marko Vrabec4, Mirijam Vrabec4 1Eötvös Loránd University, Institute of Geography and Earth Sciences, Department of Geology, 1117 Budapest Pázmány p. sétány 1/C, Hungary (lasz.fodor@yahoo.com) 2Geological Survey of Slovenia, Dimičeva ulica 14, 1000 Ljubljana, Slovenia 3Slovak Academy of Sciences, Earth Science Institute, Department of Litosphere and Geodynamic Processes, Dúbravská cesta 9, 84005, Bratislava, Slovak Republic 4Department of Geology, NTF, UL, Aškerčeva cesta 12, 1000 Ljubljana, Slovenia Introduction nappes as the highest unit that has several subdivisions which vary according to author (Neubauer et al., 2000; Schuster et This excursion aims to present field observations and related al., 2004; Schmid et al., 2004, 2020). The Penninic units, com-laboratory data concerning the metamorphism, exhumation, posed of a dismembered ophiolite (Koller and Pahr, 1980) and and connected Miocene basin formation in the Pohorje and deep-marine sediments, are exposed in the Rechnitz windows Kozjak Mts., NE Slovenia (Fig. 1). (Fig. 1b), which is interpreted as a metamorphic core complex of Miocene age (Cao et al., 2013; Tari, 1996; Tari et al., 2020). The area is part of the Austroalpine nappe system and, at the same time, represents the western margin of the Pannonian The overlying nappe stack comprises the Austroalpine nappe Basin. The Pohorje occupies a specific place among metamor- system, most of which was composed of pre-Permian meta-phic petrologists, as it contains ultra-high-pressure metamor- morphic rocks and overlying Permian to Mesozoic successions phic rocks preserved in the Koralpe-Wölz nappe unit. The and stacked together during the Eoalpine orogeny during the formation, physical conditions, the relationship to subduction late Early to Late Cretaceous (Neubauer et al., 2000; Schmid processes, and the geodynamic interpretation of the UHP rocks et al., 2004). The Lower Austroalpine nappes represent the all represent important subjects and points of interest on the rifted margin of the Alpine Tethys (in the sense of Schmid et excursion. On the other hand, the Pohorje and Kozjak Domes al., 2004, 2008; Schuster et al., 2004). The overlying thick Up-have recently been interpreted as Miocene core complexes per Austroalpine nappe system (UAA) is composed of various (Fodor et al., 2021), and evidence of such interpretation, as metamorphic rocks; the most extensively distributed Koralpe-well as an alternative Late Cretaceous timing, are presented Wölz (KW) unit occupies a central position within the UAA and discussed during the trip. These extensional deformations (Froitzheim and Schuster, 2008). It comprises amphibolite to were temporally linked to important magmatism, thus the eclogite facies metamorphic rocks (Schuster et al., 2004), ex-structural features of the main Pohorje pluton and related hibiting high to ultrahigh-pressure conditions within the study dykes will be discussed. On the journey there and back the trip area, in the Pohorje Mts. (Hinterlechner-Ravnik et al., 1991; will cross some important tectonic features of the Eastern Alps Janák et al., 2004, 2006, 2015; Sassi et al., 2004, Vrabec et al., – the Periadriatic and Labot-Lavanttal Faults – whose tectonic 2012; Hauzenberger et al., 2016; Li et al., 2021). These (ul-aspects will be briefly mentioned (Fig. 1). tra-)high-pressure rocks could have formed during intra-con- tinental subduction (Janák et al., 2004; Schuster and Stüwe, 2008; Stüwe and Schuster, 2010; Miladinova et al., 2022) and 1. Main structural features of NE Slovenia and thus represent a major crustal-scale weakness zone. They were surroundings exhumed by large-scale isoclinal antiform and related shear zones (Kirst et al., 2010; Janák et al., 2015). 1.1. General introduction to pre-Cenozoic basement units Above the eclogitic rocks, the metamorphic degree decreas- es, and frequently a sharp jump appears in the metamorphic The crustal part of the Eastern Alps is composed of nappes grade. The low- to very low-grade metamorphic rocks and derived from (bottom to top) the subducted European plate metasediments are part of the Drauzug-Gurktal (DG) unit (exposed in the Tauern window, Scharf et al., 2013; Rosenberg (Schmid et al., 2004). The highest tectonic unit is the Trans-et al., 2018), oceanic crust and related sediments of the Alpine danubian Range (TR), composed of Variscan very low-grade Tethys (Penninic unit), and the Adria-derived Austroalpine rocks and non-metamorphosed Permian to Mesozoic sequenc-97 15TH WORKSHOP Fieldtrip guide. 15th Emile Argand Conference on Alpine Geological Studies, 12-14 September 2022, Ljubljana, Slovenia. es; its nappe position above other Austroalpine units is con- 1.2. Metamorphic domes firmed by structural studies (Tari, 1994; Fodor et al., 2003; Tari and Horváth, 2010). The Pohorje Mts. represent a metamorphic dome that mainly consists of the Koralpe-Wölz nappe, and is surrounded by low- A great number of geochronological data constrain nappe grade metamorphic rocks or directly by non-metamorphosed emplacement to the Cretaceous (~100 – ~70 Ma, Frank et nappes belonging to the Drauzug-Gurktal and the Transdanu-al., 1987; Dallmeyer et al., 1996, 1998). Late Cretaceous sed- bian Range units, respectively (Fig. 1b, 2). The boundaries of iments with depositional age from ~85–70 Ma occur on top these units were originally Cretaceous thrusts (Schmid et al., of the Drauzug-Gurktal and TR units (Fig. 2) (Willingshofer 2004), but now exhibit sharp changes in metamorphic degree et al., 1999). Although these basins were formed in an overall (Trajanova, 2002; Herg and Stüwe, 2018). In the core of the contractional setting of the entire Eoalpine orogen (Ortner et dome, the granodioritic Pohorje pluton and subvolcanic dacite al., 2015; Tari and Linzer, 2018), the Late Cretaceous basin bodies intruded upon the host metamorphic rocks in the Mio-subsidence near the study area coincided with the exhumation cene, at 18.6 Ma (Fig. 3) (Fodor et al., 2008; Trajanova et al., of the high-pressure Koralpe-Wölz unit from below low-grade 2008; Poli et al., 2020). Intrusive rocks largely penetrate into units along low-angle shear zones (Neubauer et al., 1995; Kurz the KW nappe, but in the northwest also into the rocks of the et al., 2002; Krenn et al., 2008; Herg and Stüwe, 2018). Drauzug-Gurktal unit. The northwesternmost part of the Pohor- Figure 1: Itinerary of the field trip with daily stopovers 98 15TH WORKSHOP Fieldtrip guide. 15th Emile Argand Conference on Alpine Geological Studies, 12-14 September 2022, Ljubljana, Slovenia. je Mts., situated north of the main dacite body, has a distinct within the ENE-trending Kungota Fault, which merges with the structure, where only low-grade metamorphics, non-metamor- NE corner of the Kozjak Dome (Fig. 3) (Žnidarčič and Mioč, phosed Permo-Mesozoic rocks, and Miocene sedimentary and 1987). dacitic volcanic formations occur (Mioč and Žnidarčič, 1976). In the eastward subsurface continuation of the Pohorje Dome, The Kozjak Dome and the E-W trending Remschnigg ridge the Murska Sobota (MS) Ridge is composed of the same KW me- (bounding the Styrian Basin) have a similar structure to the dium-grade rocks as the Pohorje itself (Lelkes-Felvári et al., 2002; Pohorje Dome but lacks Miocene magmatic rocks (Fig. 2). Here, Fodor et al., 2013). Small slivers of low-grade Paleozoic rocks Miocene synrift sediments occur in small patches on top of the and non-metamorphosed Permo-Triassic sediments encountered low-grade Paleozoic or non-metamorphic Permo-Mesozoic rocks. by several boreholes occur sporadically on the top of the medi-Slivers of Permo-Mesozoic rocks are incorporated as small lenses um-grade rocks (Fig. 1b, Gosar, 1995; Fodor et al., 2013). The Figure 1b: Geological setting of the Pohorje Mts. and surroundings. Pre-Miocene units and Miocene to Quaternary structures of the study area, the western Pannonian Basin (based on maps of Flügel and Neubauer, 1984; Flügel et al., 1988; Tomljenović and Csontos, 2001; Fodor et al., 2013; Schmid et al., 2020). Few thermochronological data from the Murska Sobota high is shown, see legend on Fig. 2. 99 15TH WORKSHOP Fieldtrip guide. 15th Emile Argand Conference on Alpine Geological Studies, 12-14 September 2022, Ljubljana, Slovenia. MS Ridge is surrounded in the north, east, and south by the ages, and zircon (U-Th)/He ages, data on which was recently Baján detachment, which is a low-angle shear zone imaged by summarized by Fodor et al. (2020, 2021) (Fig. 2). seismic data and penetrated by the Baján B-M-1 borehole (Fodor et al., 2013; Lelkes-Felvári et al., 2002; Nyíri et al., 2021). Cretaceous and Lu/Hf ages on garnets, U-Pb ages on zircon and a monacite age date the timing of metamorphism of the (ultra)high-pressure rocks between 97 and 87 Ma in the 2. Extension and exhumation in the Pohorje and southeastern Pohorje (Miller et al., 2005; Thöni et al., 2008; Kozjak Mts. Janák et al., 2009; Sandmann et al., 2016; Chang et al., 2020; Li et al., 2021). Muscovite K-Ar ages from mesograde rocks of 2.1. Thermochronological data the Kozjak Dome, and from low-grade rocks of the northern Kozjak and from the southern Pohorje Domes are Cretaceous, The exhumation of the Pohorje and Kozjak Domes is con- suggesting that cooling of the structurally higher units below strained by diverse geochronological data, including K-Ar ages ca. 420–350°C already occurred during the Eoalpine orogeny on variable mineral separates, zircon and apatite fission-track (Fodor et al., 2008). Figure 2: Geochronological ages from the Pohorje-Kozjak Mts. (summarized in Fodor et al., 2021, after Fodor et al., 2003, 2008; Thöni et al., 2008; Trajanova et al., 2008; Sandmann et al., 2016; Li et al., 2021). Base map after Mioč and Žnidarčič, 1976; Žnidarčič and Mioč, 1988, modified. Red squares indicate excursion stops. 100 15TH WORKSHOP Fieldtrip guide. 15th Emile Argand Conference on Alpine Geological Studies, 12-14 September 2022, Ljubljana, Slovenia. Few muscovite K/Ar ages in the western Pohorje Dome and 2.2. Structural observations zircon FT data of the Kozjak Dome indicate Oligocene cooling (Fig. 2). This cooling could follow the thermal input derived Evidence of Miocene extensional deformation comprises the from the Paleogene Periadriatic magmatism (Rosenberg, 2004; following, summarized by Fodor et al. (2021): (1) the exis-Schulz, 2012; Neubauer et al., 2018) or could also be connect- tence of sub-horizontal to low-angle detachment zones, (2) ed to the earliest stage of the lateral extrusion of the Eastern disposition and geometry of Permo-Mesozoic and low-grade Alps (Rosenberg et al., 2018). rocks above and around the domes, (3) large-scale tilting of the entire Pohorje Dome, (4) eastward younging thermochro- On the other hand, the Miocene zircon FT ages are close to nological ages, (5) anisotropy of magnetic susceptibility (AMS) the possible onset of sedimentation (~19–18 Ma) and the data, interpreted together with (6) mesoscale ductile structures somewhat younger zircon (U-Th)/He ages (18.7–16.7 Ma) in the Miocene plutonic and host metamorphic rocks, (7) om-are coeval with the earliest sediments (Fig. 2). Therefore, we nipresent brittle extensional structures, and the variable tilt of prefer connecting these ages to the extensional exhumation synrift sediments together with AMS data from sediments, (8) of the Kozjak Dome, although the exact onset cannot be more exposed basal contact of the exhumed metamorphic rocks and precisely constrained than ~25–23 Ma. syn-rift sediments, and (9) high vitrinite reflectance values and clay mineral alteration near the Kozjak detachment. Miocene exhumation is clearly documented by muscovite and biotite K/Ar ages from the mesograde metamorphic rocks in (1 and 2) In the Kozjak Mts. a completely flat tectonic contact the eastern and southern part of the Pohorje Dome; the ages occurs at the top of the medium-grade rocks (Figs. 3, 4a, b). range from 22 to 13 Ma (Fig. 2) (Fodor et al., 2003, 2008). Above this contact, the very low-grade Paleozoic and tilted Zircon (U-Pb)/He ages of Fodor et al. (2021) constraing the Permo-Mesozoic sequences are all truncated and only occur in late stage of cooling to around ~15–14 Ma (Fig. 2), although reduced thicknesses. At Ostri vrh, strongly tilted Upper Triassic they are in contrast to the apatite (U-Th)/He ages ranging from carbonate rocks are in near-direct flat-lying contact with me-20.4 to 13.9 Ma published by Legrain et al. (2014). dium-grade rocks, indicating at least 4–6 km of stratigraphic omission (Fig. 4a, b, Stop 2/3). The ~200 m thick contact The eastern part of the Kozjak detachment show a complex zone was mapped as a separate phyllite unit (Mioč and Žni-picture, and this is detailed in stops 2/1-2; the Palaeogene ages darčič, 1976), but was later interpreted as a mylonitic shear are interpreted as mixed ages derived from the Cretaceous de- zone (Fodor et al., 2002, 2008; Trajanova, 2002). We refer to formations and the Miocene exhumation, while Miocene ages this structure as the Kozjak Detachment. (Fig. 2, 4a, b; Fodor are related to activity of the Kozjak Detachment. et al., 2003). Stretching lineations are broadly ENE-trending within the mylonite. Shear bands within the mylonites and in In the pluton, biotite, feldspar, and whole-rock K-Ar ages the underlying medium-grade rocks both exhibit top-to-NE dis-are scattered between 18.1 and 15.7 Ma and the FT ages lie placement along the eastern Kozjak detachment (Stops 2/1-2 in the same range (Dolenec, 1994; Fodor et al., 2003, 2008; Fodor et al., 2008). Above the detachment, the strongly tilted Trajanova et al., 2008). Both are interpreted as cooling ages, synrift sequences corroborate large extensional deformation postdating the intrusion, which is dated with a zircon U-Pb along this segment (Stop 2/2; Fig. 4B). age of 18.64±0.11 Ma (Fodor et al., 2008). Fast cooling is also indicated by biotite K-Ar ages of 18-17 Ma from pebbles of the (3) Four independent datasets for pressure conditions for the Miocene sediments of the RS trough having roughly the same Pohorje intrusion (Altherr et al., 1995; Fodor et al., 2008; So-depositional age as the cooling of the source granodiorite (Fig. telšek, 2019; Poli et al., 2020) are consistent with the structur-2). In the dacite body, and in few isolated intrusions along al scenario that the entire massive tilted westward after pluton the Drava River, the biotite and whole-rock K-Ar age ranges emplacement. Uplift of the eastern tip of the intrusion ranges is 18.2–15.8 Ma, which may be close to formation age owing from 15 to 20 km, depending on the uncertainty range of the to shallower emplacement depth. The andesitic and rhyolitic pressure estimates (Fig. 4c). Values for the emplacement depth dykes show a K-Ar age range similar to the main dacite body of the upper part of the pluton in the west range between ca. (18.5–16 Ma; Fodor et al., 2008), with the exception of a sin- 7.5 km (2.5 kbar) to 12 km (Sotelšek, 2019; Poli et al., 2020). gle rhyodacite dyke dated as young as 14.9 Ma (Trajanova et As the upper and lower part of the pluton are presently at the al., 2008). same topographic level, this means that the amount of west- ward tilt amounts to ~20–25°. Three new zircon FT data from mesograde rocks and one pub- lished biotite K-Ar age from a micaschist (Fodor et al., 2003) (4) Fodor et al. (2008) demonstrated that low-temperature from three boreholes of the MS Ridge indicate Miocene cooling thermochronological data suggests a trend of eastward young- (Fig. 1b; 20.8–16.1 and 14 Ma, respectively). On the other ing ages (Fig. 2). K-Ar white mica ages are Oligocene (29.5–25 hand, mica separated from the footwall of the Baján detach- Ma) in the south-western and Miocene (19-15 Ma) in the ment yielded a latest Cretaceous age (65 Ma, Lelkes-Felvári et eastern and southern parts of the Pohorje Dome. The available al., 2002). zircon FT ages and three (U-Th)/He ages (14.9–13.9 Ma) from 101 15TH WORKSHOP Fieldtrip guide. 15th Emile Argand Conference on Alpine Geological Studies, 12-14 September 2022, Ljubljana, Slovenia. the basement also corroborates Miocene exhumation. Fodor et and Kozjak Domes (Fig. 4). However, the age of extension is al. (2008) interpreted this data as an argument for the west- not so well constrained. Part of the ductile structures could ward tilt of the pluton (Fig. 4c). have formed already during the Late Cretaceous, when ex- humation of the mid-crustal medium-grade rocks of the Aus- (5) AMS is a measure of the ductile strain of the rocks and troalpine nappe pile was a common process just north of the generally indicates ~E–W ductile stretching within the Pohorje Kozjak Dome (Kurz et al., 2002; Neubauer et al., 1995), and a pluton (Fodor et al., 2020, Stop 1/2). Mesoscopic stretching similar process has been suggested for the Pohorje (Kirst et al., lineations in the pluton and in some early dykes also trend in 2010). We consider lineations in medium-grade rocks, which the same direction as the AMS axes (Fig. 3). Since mesoscopic potentially formed near peak-metamorphic conditions, as being lineations are associated with extensional structures (e.g. shear of Cretaceous age. However, K-Ar ages on muscovite and bio-bands) AMS can probably be interpreted as having been relat- tite seem to suggest that at least in the eastern Pohorje Dome ed to extension rather than to pluton emplacement (Fodor et the extensional structures could be Miocene in age (Figs. 2, 3). al., 2020). This deformation is clearly of Miocene age, while The same can be assumed for the extensional shear bands of thermochronological ages constrain both the crystal plastic de- the eastern Kozjak, where the formation conditions of the brit-formation and the acquisition of the AMS signal between 18.6 tle-plastic structures were close to the retention temperature and ~15.5 Ma. for fission tracks in zircon. 6) In the host metamorphic rocks, prominent stretching linea- (7) Brittle extensional structures occur in map- and out-tions and extensional shear bands occur both in the Pohorje crop-scale (Fig. 3, stops 2/2, 3/2-3). West of the Ribnica-Selnica trough, map and dip data demonstrate the existence of Figure 3: Structural data from the Pohorje-Kozjak Mts., after Fodor et al. (2008, 2020, 2021). 102 15TH WORKSHOP Fieldtrip guide. 15th Emile Argand Conference on Alpine Geological Studies, 12-14 September 2022, Ljubljana, Slovenia. westward-tilted domino-style blocks (Primož and Golarjev Peak deformation was overprinted by strike-slip faults attributed to Faults, Fig. 3). Above the Kozjak detachment the Miocene sed- the Pliocene-Quaternary neotectonic D3 phase (Fodor et al., iments are moderately to strongly tilted to the west (Fig. 5B), 1998, 2008). This phase was associated with large-wavelength while east-dipping normal faults are postulated between the folding of the entire dome (Sölva et al., 2005). west-tilted blocks. 8) Two sites expose the contact of the mylonitic basement The main brittle deformation was characterized by a NE–SW to rocks and the deformed sediments; we visit these sites and disE–W directed extensional stress field designated as D1 phase cuss their characteristics (Fig 2,3, Stop 2/2 and 3/2). (Fodor et al., 2002, 2008, 2020) (Fig. 3). A great number of striated faults were formed when layers were still horizontal (9) Vitrinite reflectance values are very high (up to 2.5 % Rr), because the symmetry plane of conjugate faults are perpendic- and clay mineral alteration is up to thermally anchizonal con-ular to the now tilted beds. The directions of σ3 axes derived ditions around the eastern termination of the Kozjak Dome and from brittle faults are parallel to measured K1 axes of the around the Remschnigg Ridge (Sachsenhofer et al., 1998a, b). AMS (Fodor et al., 2020) (Fig. 3). The paucity of faults and These indicate significant thermal input, which was interpreted the lack of the tectonic AMS signal in rocks younger than ~14 as a sign of advective heat transport from the footwall of the Ma indicate that the deformation occurred before 15 or 14 Kozjak detachment (Fodor et al., 2002, 2008). This is in line Ma. This extensional phase was overprinted by the D2 phase with partially reset apatite FT ages from the sediments overly-characterized by E–W to SE–NW extension. The extensional ing the shallow part of the detachment (Fig. 2). Figure 4: Cross sections in the Pohorje, Kozjak Mts. after Fodor et al. (2021). a) Across the Kozjak Dome to the NE corner of the Murska Sobota Ridge. b) Detailed section of the gently dipping part of the Kozjak Detachment. c) Cross section from the Pohorje Dome to the MS Ridge (partly after Fodor et al., 2003, 2013). Moho depth is from Horváth et al. (2015) and Kalmár et al. (2018). 103 15TH WORKSHOP Fieldtrip guide. 15th Emile Argand Conference on Alpine Geological Studies, 12-14 September 2022, Ljubljana, Slovenia. Excursion stops The early extensional deformation could facilitate the formation of aplitic veins, which can be less overprinted by foliation than DAY 1, STOP 1/1 – CASTLE NEAR SLOVENSKE the host rock. Finally, the plutonic rocks and dykes are cut by KONJICE: brittle-plastic shear zones and brittle faults with variable degrees View of the Pohorje Dome, and the Lavant- of drag folding (Fig. 5a). All these deformations show coaxial ex- tal-Labot fault tension indicated by stretching lineation, AMS axes, shear bands, and faults (Fig. 5e). This stop offers a general view approximately W-E of the entire Pohorje Dome. The gently dipping eastern slope of the moun- tains is close to but does not correspond exactly to the Pohorje DAY 1, STOP 1/3 – SOUTHEAST POHORJE MTS.: Detachment. Also, the southerly dip of the detachment near UHP metamorphism Zreče can be seen. The present view shows the denudation of the post-detachment period, and also the neotectonic gentle Eclogites (Fig. 6), according to Vrabec et al. (2012), contain a folding (Sölva et al., 2005) that contributed to the elevated posi- peak metamorphic assemblage of garnet, omphacite, kyanite, and tion of the dome. phengite. Pyrope-rich garnet is unzoned and almost free of inclu- sions. The non-stoichiometric supersilicic omphacite contains up The long-lived NW-SE striking Pöls-Lavanttal-Labot Fault system to 5 mol% of Ca-Eskola molecules. The breakdown of omphacite (PLLF) runs along the northeastern margin of the Karavanke during decompression resulted in the exsolution of oriented rods Mts; the castle sits on a small fault block of this brittle shear of silica. Phengite contains up to 3.5 Si a.p.f.u. Polycrystalline zone. As part of the Karavanke Mts., this block is mostly com- quartz inclusions in peak-pressure minerals – garnet, omphacite posed of Triassic carbonates. Between the castle and the main and kyanite – are surrounded by radial fractures evidencing the Karavanke block late Early Miocene (Karpatian) sediments are former presence of coesite. Peak-pressure minerals are replaced entrapped by the shearing (Mioč and Žnidarčič, 1976). In the by symplectites of diopside+plagioclase+amphibole after om-Eastern Alps branches of the PLLF zone form the boundary of phacite, plagioclase+biotite after phengite, and sapphirine+co-several small Miocene basins (Strauss et al., 2001; Kurz et al., rundum+spinel+anorthite after kyanite. Sapphirine generally 2011; Reischenbacher and Sachsenhofer, 2013), while it bounds has a composition close to (Mg,Fe)12.4 Al38.9 Si4.5 O80, which the Slovenj Gradec Basin W of the Pohorje Dome (Ivančič et al., is amongst the most aluminous yet reported. Peak metamorphic 2018), which contains late Early to middle Miocene (Ottnang- conditions were constrained from calculated phase equilibria in ian–Karpatian and early Badenian, ~18–13.8 Ma). The fault the NKCFMASH system with the fixed bulk-rock composition, has a dextral separation of ~14 km (Ratschbacher et al., 1991; and conventional geothermobarometry. This approach led to con-Fodor et al., 1998; Frisch et al., 2000; Wöfler et al., 2011). An sistent results, the calculated peak P–T conditions of 3.0–3.7 GPa important feature is that the PLLF displaces the eastern continu- and 710–940 °C, in the stability field of coesite and in the same ation of the Periadriatic Fault but merges with the active Šoštanj range as metamorphic conditions recorded by the associated fault in the south; thus it is also a neotectonic feature. On the garnet peridotites. This implies that eclogites and their host rocks final day we cross the neotectonic folds of the Slovenj Gradec were subducted to depths of about 100 km. basin between the Periadriatic and PLL Faults. The garnet peridotites (Fig. 6) are closely associated with UHP eclogites. At least four stages of recrystallization have been DAY 1, STOP 1/2 – CEZLAK QUARRY: identified in the garnet peridotites based on an analysis of re- Pohorje pluton and associated dykes action textures and mineral compositions (Janák et al., 2006). Stage I was most probably a spinel peridotite stage, as inferred The excursion will visit the main quarry and perhaps a second from the presence of chromian spinel and aluminous pyroxenes. if exploitation permits (Stop 1/2b). The granodiorite exhibits Stage II is a UHPM stage defined by the assemblage garnet + well-developed foliation, which is gently dipping foliation in olivine + low-Al orthopyroxene + clinopyroxene + Cr-spinel. most parts of the pluton. This was formed during the cooling Garnet formed as exsolutions from clinopyroxene, coronas of the pluton, from 18.65 to ~15 Ma, indicated by thermochro- around Cr-spinel, and porphyroblasts. Stage III is a decompres-nological ages (Fig. 2). The main quarry exposes this foliation, sion stage, manifested by the formation of kelyphitic rims of while shear bands were observed in another quarry nearby high-Al orthopyroxene, aluminous spinel, diopside, and parg- (Fodor et al., 2020), indicating top-to-east slip (Fig. 5c). This asitic hornblende replacing garnet. Stage IV is represented by direction is parallel to stretching lineation and to the AMS axes the formation of tremolitic amphibole, chlorite, serpentine and (Fig. 3, 5e). Thus, we relate these deformation features to verti- talc. Geothermobarometric calculations using (i) garnet-olivine cal flattening and an early phase of ~E–W extension during the and garnet-orthopyroxene Fe-Mg exchange thermometers and cooling process, at temperatures of roughly 350–400 °C. This (ii) the Al-inorthopyroxene barometer indicate that the peak of flattening also affected mafic enclaves in the granodioritic main metamorphism (stage II) occurred at conditions of around 900 body. On the other hand, few quartz monzodioritic lenses be- °C and 4 GPa. These results suggest that garnet peridotites in the haved rigidly during this deformation, as observed in the small Pohorje Mountains experienced UHPM during the Cretaceous quarry in Fig. 5c, d, Fodor et al., 2020). orogeny. On the basis of petrochemical data, garnet peridotites 104 15TH WORKSHOP Fieldtrip guide. 15th Emile Argand Conference on Alpine Geological Studies, 12-14 September 2022, Ljubljana, Slovenia. Figure 5: Deformation features in the Pohorje granodiorite, Stop 1/2. a) Foliated granodiorite, flattened mafic enclaves cut by aplite dykes and crosscut by east-dipping late fault. b) Dynamically recrystallized quartz and internally undeformed, zoned feldspars in granodiorite. Quartz fabrics indicate grain-boundary migration (GBM) as recrystallization mechanism. Northwestern pluton, shallow intrusion depth. c) Gently tilted foliation and top-to-E shear zones in the pluton, Stop 1/2b (site 137b). d) Map view of foliated granodiorite wrapping internally undeformed quartz monzodiorite. A larger body was sampled for AMS study. Locations of sites see Fig. 2. e) stereoplots of structures and AMS axes for different lithologies. Note dominant ~E–W extension in the main granodiorite and a separate phase in rigid quartz monzodiorite bodies. After Fodor et al. (2008, 2020, 2021) using AMS data of Márton et al. (2006). The Angelier software package (1984) was used to visualise and interpret the data 105 15TH WORKSHOP Fieldtrip guide. 15th Emile Argand Conference on Alpine Geological Studies, 12-14 September 2022, Ljubljana, Slovenia. Figure 6: Characteristic rock samples of ultra-high pressure metamorphic rocks; eclogite (left) and garnet peridotite (right). could have been derived from depleted mantle rocks that were DAY 2, STOP 2/1 – NORTH OF BRESTERNICA, DAY subsequently metasomatized by melts and/or fluids either in 2, STOP 2/2 – NORTHWEST OF BRESTERNICA, the plagioclase-peridotite or the spinel-peridotite field. SREDNJE, FARMS OF ČEPE AND VUTE: Structures of the highest blocks of basement, We propose that UHPM resulted from the deep subduction of phyllonites, overlying Miocene sediments continental crust, which incorporated mantle peridotites from the upper plate in an intracontinental subduction zone. Sinking These series of outcrops expose the contact of the tilted Mio-of the overlying mantle and lower crustal wedge into the asthe- cene synrift sediment and strongly deformed basement rocks nosphere (slab extraction) caused the main stage of unroofing near the eastern Kozjak Detachment (Fig. 4, 7, 8) The Stop of the UHP rocks during the Late Cretaceous. Final exhumation 2/2a (site 94a) exposes the tilted Miocene syn-rift sediments was achieved by Miocene extensional core complex formation. above a 10 cm-thick fault gouge and the underlying mylonitic metamorphic rocks (Fig. 7a, b). The contact zone is marked by a dark grey fault gouge which is sub-horizontally lying. Few DAY 2, STOP 2/1 – NORTH OF BRESTERNICA, striae and associated faults indicate N–S extension. JAMŠEKOV POTOK (CREEK): Structures of the highest blocks of basement, The Miocene clastic beds were tilted by a different direction – phyllonites to the SW – much like the same direction of nearby outcrops (Stop 2/2b). On the other hand, post-tilt fractures partly dis- This outcrop exposes the strongly deformed “phyllite” unit that placing the sub-horizontal contact indicate ENE–WNW exten-separates the mesograde metamorphics from the overlying Mio- sion. cene sediments. Here, the low-grade Paleozoic units are missing. In addition to mylonitic to ultramylonitic texture (photo), the Somewhat below the main tectonic contact, in a sharp road rocks exhibit nice extensional shear bands, which have top-to- cut, mylonitic gneiss (“phyllonite”) are exposed (Stop 2/2c). NE kinematics (Fig. 7d, e). These bands are highlighted by later These rocks exhibit top-to-the-ENE shear bands (Fig. 7c). Fe mineralization. Few porphyroclasts also indicate the same Asymmetric folds were also observed, though their age is un-kinematics. The parent rock could be a gneiss, which is exposed clear (could be related to nappe emplacement or to extension). in the main valley. In other outcrops (e.g., site 215) garnet-bear- ing micaschist or gneiss were overprinted by mylonitisation. Nearby outcrops of the Miocene synrift sediments (site 95) The K-Ar age from muscovite from this site is 29 Ma, which is also exhibit fractures having been formed before, during, and interpreted as of mixed age, between Cretaceous and Miocene after the tilting event. In these sites the extensional directions tectonic phases (Fig. 2, see also paragraph at the next site). remained the same NNE–SSW during the tectonic tilt. In a series of outcrops ~5km east of this site, a number of tilted blocks were observed in the Miocene sedimentary rocks (sites 64, 205). Faulting was associated with drag folding (Fodor et al., 2002). Considering the symmetry of conjugate fractures to tilted beds, one part of the fractures was formed before the tilt, while others have a vertical symmetry plane; this latter set is regarded as post-tilt in origin (Fig. 8). 106 15TH WORKSHOP Fieldtrip guide. 15th Emile Argand Conference on Alpine Geological Studies, 12-14 September 2022, Ljubljana, Slovenia. This site has been sampled for AMS study (Sipos et al., 2018; stress axes indicate a good match with maximum AMS axes (Fig. Fodor et al., 2020). After tilt correction, the minimum K3 axes 8), despite a ~30° difference in angle. are approximately vertical, whereas the maximum K1 axes are between NE–SW and E–W directions (Fig. 8). This geometry All of this data shows that early extension in the syn-rift sed-demonstrates that AMS fabric is found in bedding planes and iments could be between NNE-SSW and ENE-WSW (N030E reflects an early deformation episode before the tectonic tilting and N065E) (more precise values cannot be deduced from of the sediments. In fact, AMS fabric mostly registers early defor- the data) (Fig. 8). Note that a clockwise change in extensional mation when beds were not cemented (and deformed). A com- direction is systematically present in the data set of the entire parison with brittle fractures that had also formed at sub-hori- Pohorje (Fodor et al., 2020), and this may have characterized zontal bed positions show that the early stage of fractures and the late syn-rift or early post-rift evolution of faulting. Figure 7: Structures near the Kozjak Detachment. a) The contact of the Miocene syn-rift sediments and the mylonitic basement rocks. Stop 2/2a, site 94a. b) Photomicrograph of the fault gauge, with scattered quartz grain and one larger grain, probably derived from the Miocene. c) Extensional shear bands in mylonitic gneiss (Stop 2/2c, site 94c). Feldspar porphyroblast indicate top-to-ENE shear, the age of which would be Cretaceous and/ or Miocene. d), e) Extensional shear bands in ultramylonite (“phyllonite”, Stop 2/1, site 202). White shear indicators refer to an earlier (?) shearing. 107 15TH WORKSHOP Fieldtrip guide. 15th Emile Argand Conference on Alpine Geological Studies, 12-14 September 2022, Ljubljana, Slovenia. Figure 8: Stereoplots of deformation features near the eastern Kozjak Detachment. 108 15TH WORKSHOP Fieldtrip guide. 15th Emile Argand Conference on Alpine Geological Studies, 12-14 September 2022, Ljubljana, Slovenia. Thermochronological data of stops 2/1 and 2/2 the lateral side of the pluton, probably closer to the bottom side (Fodor et al., 2008). The thermochronological data from the eastern part of the Kozjak detachment presents a complex picture (Fig. 3). The The most dominant outcrop-scale ductile structure is the weakly mylonitic rocks just under the brittle detachment fault yielded to moderately developed foliation subparallel to the dyke–host 42 Ma and 29 Ma muscovite ages (Stop 2/2c and Stop 2/1a, rock contact, and its intensity generally changes within a single respectively) (Fodor et al., 2021). In Stop 2/2a (site 94a), illite dyke. In closely spaced dacite dykes, the foliation drastically K-Ar age of 34 Ma of the fault gouge was obtained. One zircon changes from one dyke to another, although spatially they are FT (Stop 2/2c) and one zircon (U-Th)/He age (near Stop 2/1) only 10 m apart. Dykes in the north exhibit poorly developed fall in the early Miocene (23 and 18.7 Ma, respectively). In the mineral lineation. The intensity of the foliation is stronger in the syn-rift sediment, located just above the detachment zone, detri- granodiorite than in the intruding andesite dykes, thus the onset tal apatite grains show partially reset ages (Fig. 3; Sachsenhofer of crystal-plastic deformation in the pluton preceded the dyke et al., 1998a). As a result, we interpret the Paleogene K-Ar ages emplacement (Fig. 9). The granodiorote and the metamorphics as mixed ages derived from the Cretaceous post-orogenic cool- show crystalplastic lineation which, however, is only weakly ing and from the Miocene exhumation along the eastern Kozjak present in the dykes. detachment. Exhumation of the footwall rock could have started in the early Miocene (around 23 Ma). Tilted geometry of the On a microscale, the original magmatic quartz has been inter-Miocene syn-rift rocks and their tectonic contact show that de- nally deformed into elongated lenses, locally up to ribbon quartz formation was still active after 16 Ma. The thermally overprinted (Fig. 5). Relic grains display undulose extinction and subgrains, syn-rift sediments just above the detachment also argue for Mio- whereas new grains with serrated grain boundaries were formed cene exhumation and advective heat transport to the base of the by dynamic recrystallization. Biotite and amphibole grains are Mura Basin. often sheared and suffered pressure solution along foliation planes. Amphiboles are twinned along their long axis. Part of However, an onset of exhumation in the Late Cretaceous is not the feldspars phenocrysts are idiomorphic with magmatic zoning excluded in this region. In fact, Neubauer et al. (1995) interpret- and show brittle fracturing (Fig. 9a-c). The shape-preferred ori-ed the origin of the Late Cretaceous basins as the result of exten- entation of quartz grains in dynamically recrystallized quartz ag-sional exhumation of the footwall and subsidence of the hanging gregates, feldspar sigma-clasts, mica, and amphibole fishes, (Fig. wall. Tilted blocks are also present near the Baján detachment, 9a, c, d), and weakly developed shear bands indicate a top-to-which may argue for a separate Late Cretaceous extensional ESE (normal-sinistral) shear sense (Fig. 3). It is the same sense phase preceding the Miocene one (Héja, 2019). as was deduced from shear bands in the host metamorphics, but this latter could also be a Cretaceous feature. DAY 2, STOP 3 – ROAD TO SVETI DUH NA Dynamically recrystallized quartz, boudinaged biotite, and de- OSTREM VRHU: formation features in feldspars broadly place the deformation Contact of Mesozoic extensional allochton with into the higher greenschist facies. Variably deformed feldspars “phyllite” (mylonite) indicate progressively lower temperature for the initiation of de- formation. This can be a sign of deformation during cooling, just The outcrops along the road to the village of Sveti Duh na Os- after dyke emplacement, when the dyke temperature was still trem vrhu exposes Triassic carbonates, probably Upper Triassic high enough to enhance its crystal-plastic deformation process. formations. They are in almost direct contact with the phyllite unit. Although a little patch of Permian is present, the Mesozoic Within andesite and dacite dykes, the orientation of magnetic fo-sequence is not continuous anywhere, and is in tectonic contact liations and lineations are close to that of the dyke margins and with the “phyllite” rather than the medium-grade rocks. The to the solid-state foliation and weak lineation. It is suggested contact is not exposed, but the mylonitic “phyllite” can be seen therefore that the AMS reflects the crystal-plastic deformation of in road cuts. The illite K/Ar method yielded an age of 24 Ma, these dykes (Fig. 9e). The AMS value is highest when the folia-which can be connected to exhumation along the detachment. tion and shearing is strongest. DAY 2, STOP 2/4 – SOUTHWEST OF LOVRENC NA DAY 3, STOP 3/1 – SOUTH OF RIBNICA NA POHORJU: POHORJU: Variably deformed magmatic dykes at the con- Granodiorite dykes in host metamorphic rocks tact of granodiorite and metamorphic host rock This section exposes a similar tectonic situation as Stop 2/4. Sev-The outcrop in the creek exposes foliated granodiorite cut by eral granodiorite dykes and one darker mafic dyke intruded into aplitic quartz veins and a dark andesite dyke. In the roadcut, the host metamorphic rocks parallel to the boundary of the main several dacite dykes intruded into the metamorphic host rocks. granodiorite pluton. Dyke thickness varies from 15 cm up to 12 All structures dip steeply to the south, thus this site represents m. Dyke boundaries dip steeply SSW. Dyke margins are parallel 109 15TH WORKSHOP Fieldtrip guide. 15th Emile Argand Conference on Alpine Geological Studies, 12-14 September 2022, Ljubljana, Slovenia. Figure 9: Deformation features in variably deformed dacite and andesite dykes in Stop 2/4, site 281, SW of Lovrenc na Pohorju, Radoljna creek. a) Contact of granodiorite and metamorphic host rock. The magmatic rock shows foliated texture. Quartz grains are recrystallized with GBM, show undulose extinction, and sub-grains. Vertical view. b) Sigma clasts in foliated andesite dyke, intruded into granodiorite, sub-horizontal view. Note recrystallized quartz grains and zoned undeformed feldspar grains. c) Weakly oriented texture in a dacite dyke intruding metamorphic rocks, just near the northern contact of the granodiorite. Section perpendicular to dyke margin. d) Dynamic recrystallization of primary feldspar phenocrysts at the margin of the same dacite dyke as in c), 20 cm away. Locations of the site see Fig. 2, 3. e) Stereoplots of mesoscale structures in metamorphic rocks, granodiorite, dacitic and andesitic dykes, after Fodor et al. (2020). For legend, see Fig. 7. 110 15TH WORKSHOP Fieldtrip guide. 15th Emile Argand Conference on Alpine Geological Studies, 12-14 September 2022, Ljubljana, Slovenia. to foliation in host metamorphic rocks for both rock types (Fig. DAY 3, STOP 3/2 – SOUTH OF VUHRED, 10). Lineation is gently ESE plunging, similar to the features in ROAD WESTWARD FROM BREKOVA KOCA TO stop 2/4. Sinistral shear sense is indicated by quartz lenses (Fig. SVETI ANTON NA POHORJU: 10). The temporal relationship of this structure to granodiorite Strong deformation of Miocene sediments near emplacement is not clear – they could be Cretaceous or Miocene, the contact with basement rocks as in Stop 2/4. Foliation in granodiorite is expressed in a thin section and by AMS fabric (Fig. 10). This exposes the syn-rift sediments located very close to the con- tact with underlying metamorphic rocks. The main feature is the Structural evolution may be similar to stop 2/4; (1) formation of strong deformation of the clastic rocks. Near this site, the Kozjak foliation in host metamorphic rocks, (2) their tilting (folding?) Detachment dips below the NW branch of the Ribnica-Selnica to steep position, (3) intrusion of the granodiorite and mafic synform (Fig. 2, 3) roughly to WSW (Fig. 4). The underlying dykes, (4) acquisition of AMS fabric and foliation, (5) cooling rock pile consists of Triassic(?) sandstone, phyllite, (not shown and post-cooling fracturing. Tilting could be related to pluton on the map) and amphibolite; the two former units are strongly emplacement, but this was not further explored nor analysed. reduced in thickness. The exposed basal syn-rift beds exhibit Figure 10: Structures at the northern contact of the pluton, in Stop 3/1, site 360. a) Quartz aggregates recrystallized by sub-grain rotation along the northern pluton margin. b) Map view at the northern contact of the granodiorite, in host metamorphics. Quartz lens indicates sinistral shear sense. c) Stereoplots of the measured structures and AMS data (Fodor et al., 2020). 111 15TH WORKSHOP Fieldtrip guide. 15th Emile Argand Conference on Alpine Geological Studies, 12-14 September 2022, Ljubljana, Slovenia. strong cataclastic deformation with a dense network of fractures scatter of data do not allow for a firm conclusion (Fig. 11e). Two with rigid clasts cut by extensional quartz veins (Fig. 11a, c). sets of normal faults were formed before the tilt of the layers, The veins are oblique to the main shear fractures indicating nor- by NE–SW and E–W extension. The latter direction of extenmal shearing. The organic-rich fine-grained layers are plastically sion affected the rocks after the tilt (observed ca. 100m to the deformed and cut by numerous calcite veins (Fig. 11d). The ro- west), while NNE-SSW trending sinistral strike-slip faults also tated decimetre-scale dominoes and intervening low-angle faults deformed the main outcrop. dip both to NE and W-SW and show no definite shear direction, although top-to-the west shear dominates (Fig. 11b). AMS data points to WNW–ENE elongation when restored to hor- izontal bed position (Fodor et al., 2020). Although this direction With detailed fault-slip analysis several faulting episodes can is between the two early faulting events, the data also points to be deduced, although paucity of well-preserved striae and the early extensional strain (Fig. 11e). Figure 11: Brittle structures at Stop 3/2. a) Polished surface of strongly fractured Miocene syn-rift sediments. b) Field view of west-tilted beds dissected by low-angle faults. c) Cataclastic structure of the sample in a). d) Fractured sandstone layers and deformed organic-rich clay dissected by thin calcite veins. e) Stereoplots of fractures and AMS data (completed after Fodor et al., 2020, 2021). 112 15TH WORKSHOP Fieldtrip guide. 15th Emile Argand Conference on Alpine Geological Studies, 12-14 September 2022, Ljubljana, Slovenia. The pre-tilt fracturing and the AMS fabric formed in connection contacts between Paleozoic, Cretaceous, and Miocene rocks are with the Kozjak Detachment. From these structures it is not steeply dipping or sub-vertical and only slightly disrupted; this is evident whether the shearing had top-to-NE or top-to-SW kine- the segment the excursion visits. The fault’s displacement varies matics. along the strike and seems to follow the amount of exhumation of the Pohorje Dome, because Triassic rocks occur at the same elevation all along the hanging wall. DAY 3, STOP 3/3 – SOUTH OF VUHRED, SVETI ANTON NA POHORJU, FARMS CAVK, HRIBERNIK, Stress data from the hanging wall of the Lovrenc Fault (the R-S LESNIK: trough) indicates two extensional deformation phases with the Lovenc fault, geometry, kinematics σ3 axes trending NE–SW to E–W (D1 phase) and E–W to ESE– WNW (D2 phase) (Fig. 3). The data implies that the Lovrenc This series of outcrops exposes the formations near the Lovrenc Fault acted as a steep dextral fault with a normal slip component Fault, a prominent E-W striking fault of the Pohorje. The fault during the main syn-rift phase, while the kinematics during bounds the mesograde rocks in the south, while the Ribnica-Sel- the D2 phase is less clear. Alternatively, the fault could also nica synform is in its northern side. In the outcrops, steeply dip- act as a reverse fault or would represent the vertical limb of a ping Senonian, moderately dipping Miocene sedimentary rocks contractional fold that could develop during the D3 neotectonic occur in an N-S section (Fig. 12). phase of N–S compression. However, fault slip data for the D3 phase always exhibits a strike-slip component and never dip-slip The map view of the fault implies its steep to sub-vertical dip reverse faulting, which makes a single-phase contractional char- (Fig. 2, 3). In the eastern part, the fault has a few parallel acter of the Lovrenc Fault much less viable or likely. branches which join the N-S trending gently dipping main Po- horje Detachment. In the west, the Lovrenc Fault is connected The most plausible kinematic scenario for the Lovrenc Fault is a to the NW-trending normal fault system of the northwestern syn-rift transfer fault, superimposed by contraction and vertical-Pohorje (Primož and Golarjev faults), via direct fault segments, ization of the fault (Fig. 12). Because the Lovrenc Fault accom-relay ramps, and a postulated E-W trending branch concealed modates the exhumation of the Pohorje Dome, it could also be a by the dacite body (Fig. 2, 3). In this transitional area, the fault stretching fault, like those observed around the eastern Tauern could change laterally to a monoclinal fold because there the window (Kurz and Neubauer, 1996; Schmid et al., 2013). Figure 12: Observations along the Lovrenc Fault near Stop 3/3. Note the sub-vertical position of Paleozoic and Mesozoic units, and steeply dipping Miocene rocks. 113 15TH WORKSHOP Fieldtrip guide. 15th Emile Argand Conference on Alpine Geological Studies, 12-14 September 2022, Ljubljana, Slovenia. DAY 3, STOP 3/4 – ČRNI POTOK TRIBUTARY OF sub-vertical Eocene layers formed due to dextral transpression THE VELUNJA RIVER: (Fig. 14a) (Fodor et al., 1998). The Donat Fault is a narrow zone Sedimentary evolution of the Slovenj Gradec Basin that includes dozens of Permo-Mesozoic and Oligocene strike-slip duplexes (Fodor et al., 1998) and also separates domains of The road cut sections provide insight into the Miocene evolution different Cenozoic stratigraphy (Jelen et al., 1992). of the Slovenj Gradec Basin in northern Slovenia, which was studied by mapping, section logging, nannoplankton biostratig- The Šoštanj Fault bifurcates from the Smrekovec Fault from the raphy, and petrography. The results are correlated with the lith- southern side of the Oligocen Karavanka tonalite, then forms the ological column of the MD-1/05 borehole. The evolution of the southern boundary of the Velenje Basin, and eastward merges basin is connected with the development of the Pannonian Basin with the PLL Fault (Fig. 2). Fault-slip data on the surface indi-System, and the global 3rd order cycles, which influenced the cates dextral kinematics of the fault (Fodor et al., 1998), while connection with the Mediterranean Sea. Sedimentation started subsurface fault branches displacing the Velenje lignite deposit in the Karpatian in a fluvial to lacustrine environment and termi- are considered Riedel shears of the main fault (Vrabec, 1999). nated at the end of the Early Badenian (Fig. 13). Lenses of Mesozoic rocks involved in the fault zone are interpret- ed as strike-slip duplexes (Fodor et al., 1998). The dextral step During this period, three transgression–regression cycles were of the Paka river and tributaries supports the active role of the recorded. The first transgression occurred in the Karpatian and fault in the drainage network and may document a Quaternary corresponds to the TB 2.2. cycle. The sediments reflect the prox- dextral slip. However, short-duration GPS campaigns were not imity of the hinterland. After a short break in sedimentation, able to verify recent dextral slip (Vrabec et al., 2006). the Early Badenian deposition followed (Fig. 13). It marks the second transgression into the SGB, the first Badenian, correlated The Velenje Basin is a unique element that determines the age of with the TB 2.3 cycle. There are signs of a transitional envi- faulting (Fig. 14b). The basin contains up to 1000 m of Pliocene ronment, which evolved to marine in advanced stages. At the to Quaternary deposits that thicken considerably southward to-highstand system tract, the sea flooded the entire Slovenj Gradec ward the Šoštanj Fault (Brezigar, 1986). The extremely thick ba-Basin. The subsequent diminished quantity and diversity of the sin fill, with the observed en echelon fault zones, demonstrates microfossils marks the onset of the second regression stage. It is Pliocene transtensional slip along the Šoštanj Fault. On the followed by the third transgression, the second in the Badenian, other hand, the basin fill covers all the faults of the Southeastern correlated with the TB 2.4 cycle. The late Early Badenian depo- Karavanka and the Donat Fault, demonstrating their pre-Plio-sition continued in the lower-energy, though occasionally still cene activity. In this way, the activity of the Donat Fault can be turbulent environment. Silty sediments with increasingly higher constrained as post-Badenian and pre-Pliocene, ~13-5 Ma. This organic matter content indicate a shallowing of the basin, until time span may correspond to a regional contractional or transits final disappearance. Layers of fresh-water coal already bear pressional phase that characterizes the southwestern Pannonian witness to the existence of restricted swamps. After the Early Basin (Fig. 14b). Badenian, the area of the Slovenj Gradec Basin became dry land, exposed to erosion. DAY 3, STOP 3/5 – ROAD SOUTH FROM VELENJE: Dextral faulting along the Šoštanj Fault This stop allows for discussion of the evolution of the wide shear belt associated with the Periadriatic Fault and other related faults in this part of Slovenia. This segment of the Periadriatic Fault comprises duplexes of the Oligocene Karavanka tonalite, Permian Granite, Paleozoic rocks, and a thin metamorphic rock belt (Fig. 14a). Fault-slip data and the strike-slip duplexes in- dicate clear dextral kinematics. The eastern part of the fault is covered with Karpatian sediments of ca. 17.2–16 Ma (Fodor et al., 1998), suggesting that the major displacement is pre-17Ma (Fig. 14a, b). This precisely matches the time constraints from the Pannonian Basin. The southern part of the Slovenj Gradec Basin has been considerably folded (Stop 3/4), which may rep- resent a Pliocene to Quaternary deformation (Fig. 14). The internal structure of the Southeastern Karavanka Mts. is not known in detail, but here we emphasize their strongly sheared character. The best example is a narrow zone composed of 114 15TH WORKSHOP Fieldtrip guide. 15th Emile Argand Conference on Alpine Geological Studies, 12-14 September 2022, Ljubljana, Slovenia. Figure 13: Simplified sedimentological column of borehole MD-1/05 (with the range of biostratigraphic markers) correlated with the sections recorded in the Slovenj Gradec Basin, and their common correlation with the regression-transgression stages in the Karpatian and Early Badenian, correlated to the Haq et al. (1988). There are differences in the type of sedimentary environment, due to the location of the borehole (distal part) and separate sections (marginal part). b) Location of sections on a geologic map that also shows the younger (neotectonic?) folding. Inset shows the wider location of sections and the MD-1/105 borehole. All figures are after Ivančič et al. (2018). 115 15TH WORKSHOP Fieldtrip guide. 15th Emile Argand Conference on Alpine Geological Studies, 12-14 September 2022, Ljubljana, Slovenia. Figure 14: Fault systems around Stops 3/4 and 3/5, after Fodor et al. (1998). b) Schematic illustrations showing the evolution of some major structures in the transitional segment of the Periadriatic Fault to the Balaton Fault Zone. 116 15TH WORKSHOP Fieldtrip guide. 15th Emile Argand Conference on Alpine Geological Studies, 12-14 September 2022, Ljubljana, Slovenia. Acknowledgment M., Horváth, P., Vrabec, M., Jelen, B., Balogh, K., Frisch, W. (2008). Miocene emplacement and rapid cooling of the Pohorje pluton at the This compilation of excursion guides was prepared with financial Alpine-Pannonian-Dinaric junction: a geochronological and structural support for the research project led by L. Fodor and supported study. Swiss Journal of Earth Sciences, 101, 255–271. https://doi. by the National Research, Development, and Innovation Office org/10.1007/s00015-008-1286-9 of Hungary, project number 134873 Fodor L., Uhrin A., Palotás K., Selmeczi I., Tóthné Makk Á., Riznar, I., Trajanova, M., Rifelj, H., Jelen, B., Budai T., Muráti J., Koroknai B., Mozetič, S., Nádor A., Lapanje, A. (2013). Geological and structural References model of the Mura–Zala Basin and its rims as a basis for hydrogeologi- cal analysis. Ann. Report Geol. Inst. Hungary, 47–91. Altherr, R., Lugović, B., Meyer, H.P., Majer, V. (1995). Early Miocene Fodor, L., Márton, E., Vrabec, M., Koroknai, B., Trajanova, M., Vrabec, post-collisional calc-alkaline magmatism along the easternmost segM. (2020). Relationship between magnetic fabrics and deformation of ment of the Periadriatic fault system (Slovenia and Croatia). Mineralo- the Miocene Pohorje intrusions and surrounding sediments (Eastern gy and Petrology 54, 225–247. Alps). Int. J. 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Marine reptile-bearing Anisian limestone of the Velika planina mountain pasture FIELDTRIP C Luka Gale1,2, Marko Vrabec1, Tomaž Hitij3 1Department of Geology, NTF, UL, Aškerčeva cesta 12, 1000 Ljubljana, Slovenia (luka.gale@ntf.uni-lj.si) 2Geological Survey of Slovenia, Dimičeva 14, 1000 Ljubljana, Slovenia 3Dental School, Faculty of Medicine, University of Ljubljana, Hrvatski trg 6, 1000 Ljubljana, Slovenia Introduction we will then backtrack our way back and take the cable-car to the Velika planina pasture on the Velika planina plateau The Early Triassic transgression at the eastern tropical margin (field-stop 3). After filling our lungs with fresh air, we take a of Pangea led to the establishment of a mixed, carbonate-si- one-hour easy walk to the southern part of the plateau. Our liciclastic ramp, which to the east gradually sloped towards feet will initially be trampling the Middle Triassic – Carnian the Palaeotethys Ocean. The variegated mixture of bedded platform limestone and dolomite, rich in dasycladacean algae, dolostone, marlstone, carbonate sandstone, siltstone, and but, after passing a fault, we then focus on the spectacularly oolithic limestone is known as the Werfen Formation. Well- folded beds of the Velika planina Member. We stop at the Jarški known exposures of it are known from Austria (Krainer and dom hut (field-stop 4) for lunch and an examination of the Vachard, 2011), and northern Italy (Posenato, 2008; Brandner Anisian platform carbonates and the base of the Velika plani-et al., 2016), as well as from Slovenia (Novak, 2001) and other na Member. The typical facies of the lower part of the Velika countries along the Dinarides mountain chain (e.g., Aljinović planina Member is exposed around the Gojiška planina pasture et al., 2011, 2018). Towards the top of the Werfen Formation, (field-stop 5). After returning to the cable-car and catching our the siliciclastic component gradually gives way to purely breath, we descend back down to the valley. carbonate sedimentation, where a shallow marine carbonate platform developed (Buser, 1989). Although this carbonate platform generally disintegrated only in the latest Anisian or earliest Ladinian (Buser, 1989; Celarc et al., 2013), when the area experienced crustal extension due to the spreading of the Neotethys Ocean, a few tens of meters of early – middle Anisian dark, bituminous and finely-laminated, thin-bedded limestone from the Kamnik-Savinja Alps and the Julian Alps testifies to an earlier formation of (probably normal fault-con- trolled) intra-platform basins. Named for its occurrence on the Velika planina mountain pasture as the Velika planina Member, this unit yielded some spectacular finds of marine reptiles and fishes, as well as some other fossils (Hitij et al., 2010a; Tintori et al., 2014a). Outline of the field trip The fieldtrip will take us into the southern parts of the Kam- nik-Savinja Alps. We make our first stop in the town of Kamnik (Fig. 1) for an introduction to the structure of the Kamnik-Sav- inja Alps (field-stop 1). We continue along the narrow valley of the Kamniška Bistrica River, strewn with glacial deposits, pass the Predaselj canyon, where the river carved its bed into massive (Middle Triassic to lower Upper Triassic) limestone, and finally stop at the Dom v Kamniški Bistrici hut for an intro- duction to the stratigraphic succession of the Kamnik-Savinja Alps (field-stop 2). Providing the conditions are in our favour, Figure 1: Locations of field-stops (see text for description). 121 15TH WORKSHOP Fieldtrip guide. 15th Emile Argand Conference on Alpine Geological Studies, 12-14 September 2022, Ljubljana, Slovenia. STOP 1 – KAMNIK: STOP 2 – DOM V KAMNIŠKI BISTRICI: Geological structure of the Kamnik-Savinja Alps Triassic stratigraphy of the Kamnik-Savinja Alps The Velika planina plateau is situated in the southern part of The Triassic succession in the Kamnik-Savinja Alps starts with the Kamnik-Savinja Alps (KSA), which structurally belong to the Lower Triassic Werfen Formation, comprising bedded micrit-the eastern Southern Alps (Placer, 1999). The KSA and the ic limestone, subordinately marly limestone, siltstone, and oo-neighbouring Karavanke range together form a transpressive lithic limestone (Mioč, 1983; Celarc, 2004). The Werfen Forma-structure between the two major Neogene dextral strike-slip tion is followed by light grey thick bedded to massive dolomite faults: the Periadriatic fault and the Sava fault (Fig. 2). The (locally limestone) with oncoids, stromatolites, bivalves, and lens-shaped domain between the two faults is dissected by gastropod lumachellas, equivalent to the Lower Serla Dolomite sinistral NE-SW-striking faults, along which significant verti- (Fig. 3). The peritidal facies laterally and vertically abruptly pass cal-axis rotations occurred, as demonstrated by paleomagnetic into an early to middle Anisian succession of dark platy and fine-data (Fodor et al., 1998). This transpressive deformation, ly laminated limestone of the Velika planina Member (Hitij et al., which is likely post-6 Ma in age, complicates the original geo- 2010a). The latter gradually grades back into peritidal facies. logical relationships, which are still poorly understood. Many The Lower Serla Dolomite upwards passes into marlstone, mud-geological, geomorphological, and geodetic indicators demon- stone, thin- to medium-thick bedded limestone and dolomite of strate that this system is tectonically still active. According to the middle to upper Anisian Strelovec Formation (Miklavc et al., Placer (1999) and Celarc et al. (2014), the entire area of the 2016). The Strelovec Formation is concordantly overlain by the KSA belongs to the Julian Nappe, a part of the late Neogene upper Anisian Contrin Formation, comprising shallow marine South-Alpine thrust system. After the nappe emplacement, be- bedded and massive limestone, or locally dolomite. Near the tween 10 and 20 km of dextral displacement on the Sava fault top, the Contrin Formation locally constraints small half-grabens separated KSA from the Julian Alps. filled with upper Anisian red radiolarian-bearing limestone of the Loibl Formation, upper Anisian and/or lower Ladinian vol- The Mali Grad viewpoint provides an excellent panorama of canics and volcaniclastics, polymictic breccias, marls and hemi-the central KSA. At the foot of the mountains the Sava fault pelagic limestones of the Buchenstein Formation (Celarc et al., makes a restraining bend, which folded the thick succession of 2013). Massive limestone of the Ladinian Schlern Formation fol-Miocene sediments of the Tunjice Hills in its foreland into an lows. At the top, the platform carbonates locally truncate at the overturned syncline. The steep southern slopes of the Velika upper Ladinian volcaniclastics, platy cherty limestone, and calca-Planina plateau dominate the eastern half of the panorama. In the central part, the barren peaks of Mts. Skuta, Turska gora, Brana, and Planjava reach up to 2500 m in elevation. These peaks are built exclusively of mid- to late Triassic carbonate rocks. Figure 2: Generalized geological structure of northern Slovenia with the Velika planina plateau marked with a star. PAF – Periadriatic Fault; ŠF – Šoštanj Fault. Figure 3: Stratigraphic successions for Triassic units in the Kamnik-Savinja Alps (from Žalohar and Celarc, 2010). 122 15TH WORKSHOP Fieldtrip guide. 15th Emile Argand Conference on Alpine Geological Studies, 12-14 September 2022, Ljubljana, Slovenia. renite of the Korošica Formation (Jurkovšek, 1984; Celarc, 2004; Žalohar and Celarc, 2010), or end with breccias, which mark a stratigraphic gap with the lower Carnian Razor Limestone. The later comprises peritidal limestone in Lofer cycles and is similar to the Norian-Rhaetian Dachstein Limestone. The two peritidal units are separated by the upper Carnian Martuljek Platy Lime- stone, which is relatively rich in conodonts, ammonoids, and brachiopods (Ramovš, 1986; Celarc and Kolar-Jurkovšek, 2008; Celarc et al., 2014). From the Dom v Kamniški Bistrici hut, a panoramic view opens towards the Kamnik-Savinja Mountains. The highest visible sum- mits belong to Mt. Grinovec (2558 m) and Mt. Skuta (2532 m) (Fig. 4). The lower slopes of the mountains are made of lower Carnian Razor Limestone. Its sedimentological characteristics have not yet been studied in the Kamnik-Savinja Alps. In the Julian Alps, this unit comprises bedded as well as mas- Figure 4: Panoramic view of Mt. Skuta (2532 m) and its geological features sive reef limestone (Ramovš, 1987; Celarc and Kolar-Jurkovšek, 2008). The bedded limestone appears as thick-bedded peritidal and uppermost slopes of Mt. Skuta and Mt. Kočna. Reef slope limestone organized into asymmetric cycles 1–1.5 m thick. The and crest are nearly impossible to distinguish macroscopically, subtidal parts comprise packstone and grainstone with peloids, and together they comprise a unit at least 400 m thick. Corals intraclasts, oncoids, gastropods, bivalves, corals, dasycladacean predominate over sponges as reef builders. Subordinate are algae, and foraminifers. The intertidal facies contain stromat- sponges. Sponges and microbialites act as binding organisms. olites, fenestrae, and small palaeokarst cavities. The Razor Microproblematica (Baccanella floriformis Pantić) is common Limestone is sharply overlain by the upper Tuvalian – lower within the sediment. Bedded peritidal Dachstein Limestone is Norian Martuljek platy limestone (Ramovš, 1989), marking a present on the top and on the NW slopes of Mt. Kočna. The major drowning unconformity (Ramovš, 1989; Celarc et al., bedding and facies here are nearly identical to the far older 2014). A relatively thin unit (25 m) consists of red and grey Razor Limestone (Celarc et al., 2014). limestone with slightly nodular to planar bedding. The limestone is slightly dolomitized packstone with glauconite, rare fragments of bivalves, filaments, lagenide foraminifers, and peloids. Fine- STOP 3 – VELIKA PLANINA PASTURE: grained bioclastic wackestone and packstone with filaments, “Cordevolian limestone and dolomite” brachiopods, and foraminifers prevail in the upper part of the unit. The Velika planina plateau has been geologically mapped by Teller (1898a, b), Premru (1983a, b), and Vičič (2014). The On Mt. Kočna, two members of the Martuljek platy limestone northern part is dominated by shallow marine dolomites and can be distinguished. The lower member is identical to the subordinate limestones of the “Cordevolian limestone and dolo-already described facies below Mt. Skuta, while the upper mite”. To the south, this unit is in fault contact with the Anisian member comprises a lot of grains redeposited from shallow wa- Lower Serla Dolomite and the Velika planina Member. Further ter, such as corals and crinoids (Celarc et al., 2014). Upwards, south, the former is in normal stratigraphic contact with the the Martuljek Platy Limestone is sharply overlain by the lower Lower Triassic Werfen Formation. This sequence is part of the to upper Norian limestone with chert (Ramovš and Jamnik, same tectonic block, which is thrusted over the Middle Triassic 1991; Jamnik and Ramovš, 1993; Celarc et al., 2014), occu- dolomite. Lineation on the thrust plane indicates initial thrusting pying most of the high karst plateau visible from the hut. The to the SW, overprinted by younger thrusting to the S. The area limestone with chert is approximately 150 m thick. Ramovš is additionally transacted by steep faults of SSW-NNE, NE-SW, and Jamnik (1991), and Jamnik and Ramovš (1993) compared NEE-SWW, and NW-SE strikes, respectively. It is unclear whether it to the Hallstatt facies of the Northern Calcareous Alps. Two some of these are reactivated synsedimentary faults. members can be distinguished. The lower member is composed of medium-bedded limestone with chert nodules and lenses. The The “Cordevolian limestone and dolomite” unit comprises limestone is fine-grained bioclastic packstone with filaments, undifferentiated massive platform carbonates of approximately subordinately wackestone with brachiopods, crinoids, peloids, Ladinian to early Carnian age. Due to the lack of leading fossils, sponge spicules, and radiolarians. The upper member consists poor paleontological determinations, predominant fault contacts more of thick-bedded and lacks chert. It is bioclastic, intraclastic, with the neighbouring units, and a general lack of interest in re-and peloidal grainstone. Reef breccia is common in the upper- search, these platform carbonates have not yet been satisfactori-most part, marking a gradual transition into the slope and reef ly resolved and divided into formations. Dasycladacean algae are crest of the Dachstein reef limestone. The latter forms the peaks commonly present, but their determinations are dubious. The 123 15TH WORKSHOP Fieldtrip guide. 15th Emile Argand Conference on Alpine Geological Studies, 12-14 September 2022, Ljubljana, Slovenia. limestone and dolomite from Velika planina are probably equiv- Also present are laminae of sparse wackestone up to 1 cm thick alent to the Schlern Formation or the Cassian Dolomite from the with small peloids, Earlandia, small lagenid and miliolid for-Italian Dolomites (Celarc, 2004). Dasycladacean algae, encrust- aminifers, ostracods, and thin-shelled bivalves. Elliptical hori-ed by microbialite, foraminifers (Duostominidae, Aulotortus sp., zontal and vertical burrows are rarely present. Also common Cucurbita sp.), ostracods, and bivalves have been recognized in in the lower part of the Velika planina Member is the Earlandia thin sections. Other common grains are peloids and oncoids. mustone, characterised by this foraminifer and not so clearly laminated. Subordinate to mudstone are peloid wackestone with ostracods, intraclastic-peloid wackestone to packstone, STOP 4 – JARŠKI DOM HUT: intraclastic-bioclastic grainstone, and rare bivalve rudstone. Lower Serla Dolomite These are interpreted as distal turbidite deposits. The base of the Velika planina Member is represented by the The laminated facies yielded some remarkable fossils (Fig. Lower Serla Dolomite. A large variety of facies of this dolomite 7). The most common fossil is the Chondrites ichnofossil. The can be seen below the Jarški dom hut, where the unit is some bivalve of the genus Modiolus and the lingulid brachiopods tens of meters thick. The dolomite is light grey, thick bedded to have accumulated in some beds. Rarer is the bivalve Bakevellia massive. Macroscopically, it contains numerous oncoids, stromat- costata, articulated sea lilies, small ammonoids, other small olites, bivalve and gastropod lumachellas (Fig. 5). Foraminifer inarticulated brachiopods, and crustaceans. The most spectac-Citaella dinarica (Kochansky-Devidé and Pantić) indicates lower ular finds belong to sauropterygian marine reptiles of the order to middle Anisian age. The overlying Velika planina Member is Nothosauroidea (Hitij et al., 2010a), and actinopterygian fishes exposed immediately above the hut and along the road, where (Tintori et al., 2014a) and a coelacanth. Genera Saurichthys, intraformational (flat pebble) breccias can be seen. Eosemionotus, Placopleurus, and Furo have been identified. Coprolites are abundant as well. Sedimentary textures are commonly disrupted by slumping, STOP 5 – GOJŠKA PLANINA PASTURE: which is common in the lower and middle part of the Velika Velika planina Member planina Member but was not observed in its uppermost part. The Velika planina Member has been divided into two parts. The lower part of the succession is easily recognisable as Interpretation of the Velika planina Member dominated by thin bedded bituminous and finely laminated mudstone (Fig. 6). Some nice outcrops of this facies are pres- The upper part of the Velika planina Member was logged north ent along the path from the Velika planina pasture to the Mala of field-stop 4, around the Dovja Raven. Upwards, the bedding planina pasture. A small exposure can be examined there along becomes thicker and the lamination less pronounced. Wavy a small road cut. lamination, birdseye fenestrae, and oncoids gradually appear. Along with microbial bindstone (stromatolite), grainstone The laminae in the finely laminated mudstone are mostly hori- with bioclasts and peloids, and oncoid floatstone predominate. zontal and parallel to each other. The light brown laminae are Upwards, bedded limestone gradually gives way to massive up to 2.5 mm thick, while the darker are even thinner. Both limestone. This gradual transition of the Velika planina Mem-are texturally mudstone. The darker laminae likely represent ber into the bedded peritidal limestones suggests only a basin microbial mats on the basin floor. of only minor depth, which supposition is also supported by Figure 5: Microfacies from the Lower Serla Dolomite below the Velika planina Member 124 15TH WORKSHOP Fieldtrip guide. 15th Emile Argand Conference on Alpine Geological Studies, 12-14 September 2022, Ljubljana, Slovenia. Figure 6: Lower part of the Velika planina Member. a: Platy limestone with celestine crystals. b: Slumped finely laminated mudstone. c: Finely laminated mudstone. d: Wackestone with ostracods and Earlandia foraminifers. Fossils probably represent autochthonous biota living in oxygen-poor conditions. Figure 7: Fossils from the Velika planina Member. a: An undescribed species of crinoids. Length of the crown is 9 mm. b: The oldest occurrence of actinopterygian fish Eosemionotus sp. Length of the specimen 6 cm. c: Sacral part of a sauropterygian. Length of the specimen is 9 cm. 125 15TH WORKSHOP Fieldtrip guide. 15th Emile Argand Conference on Alpine Geological Studies, 12-14 September 2022, Ljubljana, Slovenia. other observations, such as the lack of prominent breccias at References the base, the near-absence or even lack of open-marine plank- ton and nekton, such as radiolarians and ammonoids, the Aljinović, D., Horacek, M., Krystyn, L., Richoz, S., Kolar-Jurkovšek, T., composition of the vertebrate fauna (i.e. the finds of nothosau-Smirčić, D., & Jurkovšek, B. (2018). Western Tethyan epeiric ramp roids, which were limited to shallow intraplatform basins and setting in the Early Triassic: An example from the Central Dinarides shallow epicontinental seas; Rieppel, 1999; Černansky et al., (Croatia). J. Earth Sci. , 29, 806–823. 2018), and the gradual transition towards the platform facies Aljinović, D., Kolar-Jurkovšek, T., Jurkovšek, B., & Hrvatović, H. (2011). at the top. Slumping is common in the lower and middle part Conodont dating of the Lower Triassic sedimentary rocks in the of the member, but not in the uppermost part, again suggesting External Dinarides (Croatia and Bosnia and Herzegovina). Riv. Ital. a gradual levelling of the topography as the basin filled. This is Paleontol. Stratigr. , 117, 135–148. confirmed by the change in the facies association. Brandner, R., Gruber, A., Morelli, C., & Mair, V. (2016). Pulses of Neo- tethys-rifting in the Permomesozoic of the Dolomites. Geo.Alp, 13, The intraclastic breccias at the base of the member are in-7–70. terpreted as indicators of the initial subsidence of the basin Bromley, R. G., & Ekdale, A. A. (1984). Chondrites: A trace fossil indi-floor, which took place sometime during the early to middle cator of anoxia in sediments. Science, 224, 872–874. https://doi. Anisian. In the initial stage of the basin’s evolution, the water org/10.1126/science.224.4651.872 column was likely stratified, and hypoxic to anoxic conditions Buser, S. (1987). Development of the Dinaric and Julian carbonate plat-prevailed at the bottom. This is supported by the preservation forms and the intermediate Slovenian basin (NW Yugoslavia). In G. of articulated skeletons of vertebrates and rare sea lilies, the B. Carulli, F. Cucchi, & C. P. Radrizzani (Eds.), Evolution of the karstic lack of large and diverse bioturbations, and the near absence carbonate platform: Relation with other periadriatic carbonate platforms of benthic organisms. As mentioned, however, some levels are (pp. 313–320). slightly bioturbated. Ostracods, Earlandia, and lagenids likely Celarc, B. (2004). Geološka zgradba severovzhodnega dela Kamniško – represent autochthonous biota, as suggested by the preserva- Savinjskih Alp = Geological structure of the northwestern part of the tion of both valves in ostracods and the random orientation of Kamnik-Savinja Alps. Univerza v Ljubljani. the microfossils. Earlandia is interpreted as a benthic opportun- Celarc, B., Gale, L., & Kolar-Jurkovšek, T. (2014). New data on the pro-ist (Krainer and Vachard, 2009), and thin-shelled lagenids are gradation of the dachstein carbonate platform (Kamnik-Savinja Alps, tolerant of low-oxygen conditions (Stockar, 2010). Chondrites, Slovenia) = Novi podatki o progradaciji dachsteinske karbonatne plat- which is also typical for poorly ventilated sediments (Bromley forme (Kamniško-Savinjske Alpe, Slovenija). Geologija, 57(2), 95–104. and Ekdale, 1984). https://doi.org/10.5474/geologija.2014.009 Celarc, B., Goričan, Š., & Kolar-Jurkovšek, T. (2013). Middle Triassic car- Higher up in the succession, bedding becomes thicker and bonate-platform break-up and formation of small-scale half-grabens lamination less pronounced. Bioturbation is more common, (Julian and Kamnik-Savinja Alps, Slovenia). Facies, 59(3), 583–610. and several indicators of small depth gradually appear (wavy https://doi.org/10.1007/s10347-012-0326-0 stromatolites, fenestrae, and oncoids). Finally, the Velika Celarc, B., & Kolar-Jurkovšek, T. (2008). The Carnian-Norian basin-plat-planina Member gradually gives way to well-aerated massive form system of the Martuljek mauntain group (Julian Alps, Slovenia): limestone. Progradation of the Dachstein carbonate platform. Geologica Carpathi- ca : International Geological Journal, 59(3), 211–224. Čerňansky, A., Klein, N., Soták, J., Olšavský, M., Šurka, J., & Herich, P. Conclusion to the field trip (2018). A Middle Triassic pachypleurosaur (Diapsida: Eosauropte- rygia) from a restricted carbonate ramp in the Western Carpathians The Velika planina Member is a relatively “newly” researched (Gutenstein Formation, Fatric Unit): Paleogeographic implications. lithostratigraphic unit in Slovenia. Many more spectacular fos- Geologica Carpathica : International Geological Journal, 69(1), 3–16. sil finds can be expected from this unit and many stratigraphic https://doi.org/10.1515/geoca-2018-0001 questions raised. The similar yet younger and more widespread Fodor, L., Jelen, B., Márton, E., Skaberne, D., Čar, J., & Vrabec, M. Strelovec Formation from the middle to upper Anisian testifies (1998). Miocene-Pliocene tectonic evolution of the Slovenian Peri- to another episode of crustal extension and eventually unsuc- adriatic fault: Implications for Alpine-Carpathian extrusion models. cessful differentiation of the shelf. Finally, the late Anisian (?) Tectonics, 17(5), 690–709. https://doi.org/10.1029/98TC01605 to early Ladinian extension resulted in the creation of horst- Hitij, T., Križnar, M., Žalohar, J., Reneseto, S., & Tintori, A. (2010). Hori-and-graben topography and long-lasting deeper sedimentary zont Velike planina – dom triasnih morskih pošasti. In J. Gregori (Ed.), basins, such as the Tolmin Basin (the Slovenian Basin, s.str.) The kingdom of Tethys. The fossilized world of Triassic vertebrates from and the Bled Basin, which are the subject of other field excur- the Kamniško-Savinjske Alps (pp. 68–83). sions. Jurkovšek, B. (1984). Langobardske plasti z daonelami in pozidonijami v Sloveniji [Langobardian beds with daonellas and posidonias in Slove- nia. Geologija, 27, 41–95. Kreiner, K., & Vachard, D. (2011). The Lower Triassic Werfen Formation of the Karawanken Mountain (Southern Austria) and its disaster survi- 126 15TH WORKSHOP Fieldtrip guide. 15th Emile Argand Conference on Alpine Geological Studies, 12-14 September 2022, Ljubljana, Slovenia. vor microfossils, with emphasis on Postcladella n. Gen. (Foraminifera, Vičič, B. (2014). Tectonic position of the Velika planina limestone [Dip-Miliolata, Cornuspirida). Rev. Micropal. , 54, 59–85. lomsko delo = diploma thesis]. Univerza v Ljubljani. Miklavc, P., Celarc, B., & Šmuc, A. (2016). Anisian Strelovec formation Žalohar, J., & Celarc, B. (2010). Geološka zgradba Kamniško-Savinjskih in the Robanov kot, Savinja Alps (Northern Slovenia) = Anizijska Alp = Geological structure of the Kamniško-Savinjske Alps. In J. Strelovška formacija v Robanovem kotu, Savinjske Alpe (Severna Gregori (Ed.), The kingdom of Tethys. The fossilized world of Triassic Slovenija). Geologija, 59(1), 23–34. https://doi.org/10.5474/geologi-vertebrates from the Kamniško-Savinjske Alps (pp. 43–51). ja.2016.002 Mioć, P. (1983). Osnovna geološka karta SFRJ 1:100000. Tolmač za list Ravne na Koroškem L33−54 [Basic Geological Map of SFRY 1:100000, Geology of the Ravne na Koroškem sheet. Geološki zavod ljubljana. Novak, M. (2001). Scythian beds in the Toško Čelo area (Slovenia). Geologija, 44, 295–303. Placer, L. (1999). Contribution to the macrotectonic subdivision of the border region between Southern Alps and External Dinarides. Geologi- ja, 41, 223–255. https://doi.org/10.5474/geologija.1998.013 Posento, R. (2008). Global correlations of mid Early Triassic events: The Induan/Olenekian boundary in the Dolomites (Italy). Earth-Sci. Rev. , 91, 93–105. Premru, U. (1983a). Osnovna geološka karta SFRJ 1:100000, list Ljublja- na L33−66 [Basic Geological Map of SFRY 1:100000, Ljubljana sheet [Map]. Zvezni geološki zavod Beograd. Premru, U. (1983b). Osnovna geološka karta SFRJ 1:100000. Tolmač za list Ljubljana L33−66 [Basic Geological Map of SFRY 1:100000, Geolo- gy of the Ljubljana sheet. Zvezni geološki zavod Beograd. Ramovš, A. (1986). Paläontologisch bewiesene Karn/Nor-Grenze in den Julischen Alpen. Newsl. Stratigr. , 16, 133–138. Ramovš, A. (1987). Ausbildung der Karn-Stufe im östlichen Teil der nördlichen Julischen Alpen. Geologija, 30, 67–82. Ramovš, A. (1989). Upper Tuvalian limestones (Carnian, Upper Triassic) in the Hallstatt development also in Kamniško-Savinjske Alps. RMZ – Min. Metal. Quart. , 36, 191–197. Ramovš, A., & Jamnik, A. (1991). The first proof of deeper marine No- rian (Upper Triassic) beds with conodonts and holothurian skeletons in the Kamnik Alps (Slovenia). RMZ – Min. Metal. Quart. , 38(3), 365–367. Rieppel, O. (1999). Phylogeny and paleobiogeography of Triassic Sauropterygia: Problems solved and unresolved. Palaeogeography, Palaeoclimatology, Palaeoecology, 153, 1–15. https://doi.org/10.1007/ s00015-010-0008-2 Stockar, R. (2010). Facies, depositional environment, and palaeoecology of the Middle Triassic Cassina beds (Meride Limestone, Monte San Giorgio, Switzerland). Swiss Journal of Geosciences, 103, 101–119. https://doi.org/10.1007/s00015-010-0008-2 Teller, F. (1898a). ): Geologische Spezialkarte der k. K. Österreichisch – Un- garischen Monarchie 1:75 000, Blatt Eisenkappel und Kanker, Zone 20, Col. 11 [Geological Map of Österreichisch – Ungarischen Monarchie 1:75 000, Eisenkappel and Kranj sheet [Map]. K. k. Geologische Reichsan- stalt. Teller, F. (1898b). Geologische Spezialkarte der k. K. Österreichisch – Un- garischen Monarchie 1:75 000. Erläuterungen zur Blatt Eisenkappel und Kanker [Geological Map of Österreichisch – Ungarischen Monarchie 1:75 000, Geology of the Eisenkappel and Kranj. K. k. Geologische Reichsan- stalt. Tintori, A., Hitij, T., Jiang, D., Lombardo, C., & Sun, Z. (2014). Triassic actinopterygian fishes: The recovery after the end-Permian crisis. In- tegr. Zool. , 9(4), 394–411. https://doi.org/10.1111/1749-4877.12077 127 15TH WORKSHOP Fieldtrip guide. 15th Emile Argand Conference on Alpine Geological Studies, 12-14 September 2022, Ljubljana, Slovenia. Lower to Middle Jurassic limestone succession at the margin of the Ljubljana Moor: From microfacies to the Romans FIELDTRIP D Rok Brajkovič1, Petra Žvab Rožič2, Luka Gale1,2 1Geological Survey of Slovenia, Dimičeva 14, 1000 Ljubljana, Slovenia (rok.brajkovic@geo-zs.si) 2Department of Geology, NTF, UL, Aškerčeva cesta 12, 1000 Ljubljana, Slovenia Introduction la beds as defined by Dozet and Strohmenger, 2000), 3) the Lithiotid Limestone Member, 4) the Oolitic Limestone Member, Large, thick masses of Mesozoic carbonates that form the and 5) the Spotty Limestone Member (Fig. 2). The Podbukovje northern Dinarides (southern Slovenia) deposited on isolated Formation is best correlated with the Calcari Grigi Group from the intraoceanic Southern Tethyan Megaplatform and its suc- the Trento Platform in NE Italy, and with successions from the cessor, the Adriatic Carbonate Platform (Vlahović, 2005). The NE parts of Dinarides. topic of this field trip is a small part of this succession, namely the Lower Jurassic Podbukovje Formation, which is exposed in many places along the southern rim of the Ljubljana Moor Basin (Fig. 1). Structurally, this area belongs to the External Di- narides – more precisely to the Hrušica Nappe (Placer, 1999). Figure 1: Topographic map with field trip stops marked Figure 2: Stratigraphic composition of the Podbukovje Formation Lower Jurassic stratigraphy of the Krim-Mokrec The Krka Limestone Member is Hettangian to Sinemurian in Mountains age and consists mainly of micritic limestone and rare beds with fragments of molluscs. The lower parts of this member are The Lower Jurassic sedimentary succession, deposited con- commonly dolomitized. Micritic and stromatolitic limestone cordantly on the Upper Triassic Main Dolomite Formation deposited under shallow subtidal and peritidal conditions of and overlain by the Middle Jurassic Laze Formation, consists the inner restricted parts of the platform. Thicker oolitic beds of limestone and dolomite. The Lower Jurassic succession is of limestone are subordinate, but their proportion increases called the Podbukovje Formation and consists of five members. higher up (Dozet and Strohmenger, 2000; Dozet, 2009). Ac-From oldest to youngest, these are: 1) the Krka Limestone cording to Ramovš (1990, 2000), some of the micritic beds Member, 2) the Orbitopsella Limestone Member (Orbitopsel- were exploited as a local source of stone during Roman rule. 128 15TH WORKSHOP Fieldtrip guide. 15th Emile Argand Conference on Alpine Geological Studies, 12-14 September 2022, Ljubljana, Slovenia. Possible quarries may have been located near Staje, where the STOP 1 – TOMIŠELJ: remains of a Roman settlement have been uncovered (Rožič et Hettangian – Pliensbachian succession al., 2018). The road-cut follows the transition from the upper part of the The Orbitopsella Limestone Member was deposited during the Krka Member to the Orbitopsella, and from there to the Lithiot-late Sinemurian and lower Pliensbachian. This member con- id Limestone Members of the Podbukovje Formation. The Krka sists of grey to dark grey micritic limestones. Micritic limestone Member is characterised by fine-grained and in places stro-alternates with oolitic, intraclastic, and bioclastic limestone. matolitic limestones (Fig. 3), locally cut by bodies of mud-sup-The limestone deposited in a confined, shallow marine envi- ported breccias. The latter are interpreted as Neptunian dykes, ronment (Dozet and Strohmenger, 2000; Gale and Kelemen, and may be more than 50 m wide (Gale and Rožič, in prep.). 2017). The Orbitopsella Limestone Member from the northern The presence of Neptunian dykes in this area is explained by tip of the St. Anna hill in Podpeč was commonly used in the the incipient extension of the crust in this area related to the architecture of Roman Emona (modern Ljubljana) (see field- initial opening of the Southern Penninic Ocean. The extension stop 3). is more pronounced to the north, in the area of the Slovenian Basin and on the Julian Carbonate Platform. The most distinctive part of the Podbukovje Formation is the Pliensbachian Lithiotid Limestone Member. This member and its equivalents (e.g. Rotzo Formation from the Trento Platform) are characteristic of many tropical and subtropical carbonate platforms. The main feature consists of numerous occurrences of lithiotid bivalves. Other important fossils from this member are brachiopods and small megalodontid bivalves. Limestone is grey to dark grey, thick-bedded and micritic, biomicritic to biosparitic. This member formed in an internally differentiated lagoon under subtidal and intertidal conditions (Dozet and Strohmenger, 2000; Gale, 2015; Gale and Kelemen, 2017). Po- sitioned immediately south of the antique quarry, this member became an important source of natural stone and lime during the 19th and 20th centuries (Ramovš, 2000). Numerous archi- tectural elements were produced from it. Lithiotid facies, char- acterised by white shells surrounded by almost black micritic limestone was particularly valued. It is said that this was the favourite decorative stone of renown Slovenian architect Jože Plečnik. The Oolitic Limestone Member is late Plienbachian in age and consists of thick to very thick beds. Grains are dominat- ed by large tangential ooids up to 1 mm in size (Dozet and Strohmenger, 2000). It (or the Lithiotid Limestone Member) is followed by the Spotty Limestone Member. This limestone is dark grey and mostly micritic, with some bioturbations. Fossils (foraminifera, algae, echinoderms) are of low diversity. The sediment was deposited in a ramp environment under unfavourable conditions that accompanied and followed the Toarcian Anoxic Event (Sabatino et al., 2013). Due to the thin nature of the beds, this member was also a common source of stone plates, that were often left unshaped or were only partly shaped and used for pavements or to cover the Roman cloaca. The Podbukovje Formation is overlain by the Laze Formation, comprising brown to dark grey oolitic limestones in the lower part, followed by light grey medium-thick beds of oolitic lime- stone higher up. Ooids are 0.5 mm to 0.75 mm in diameter and have a radial structure. Round intraclasts, bioclasts, pellets, and foraminifera also occur. The limestones were formed in Figure 3: The middle part of the Tomišelj subtidal and intertidal environments near tidal channels (Dozet section, logged in greater detail by Gale and and Strohmenger, 2000; Dozet, 2009). Kelemen (2017) 129 15TH WORKSHOP Fieldtrip guide. 15th Emile Argand Conference on Alpine Geological Studies, 12-14 September 2022, Ljubljana, Slovenia. The Orbitopsella Limestone Member is characterised by thicker beds of light grey micritic and fine-grained oolitic (“peloidal”) limestone. Bioclasts are small and of low diversity. Bivalve floatstone is present in a single level. The foraminiferal as- semblage consists of Amijiella amiji, Ammobaculites spp., Cor- onipora sp., Duotaxis metula, Everticyclammina praevirguliana, Involutina sp., Nodosariidae, ? Lituolipora termieri, ? Lituosepta recoarensis, Meandrovoluta asiagoensis, Ophthalmidium sp., Pseudopfenderina butterlini, Siphovalvulina spp., Trocholina spp., Valvulinidae and Textulariidae (Gale and Kelemen, 2017). The section continues to the Pliensbachian and ends within the Lithiotid Limestone Member. STOP 2 – LEDENICA CAVE: Pliensbachian – Aalenian succession The sedimentological section Ledenica – Planinca represents the uppermost part of the Podbukovje Formation. It is com- posed of the Oolitic Limestone Member at the base of the section, the Spotty Limestone Member (Fig. 4), and the Middle Jurassic Laze Formation. The Oolitic Limestone Member is characterised by oolitic packstone to grainstone with benthic foraminifera and bivalve fragments. The transition from Oolitic to Spotty Limestone Member is sharp. Toarcian age of the Spot- ty Limestone Member was determined based on its superpo- sition and its distinct change in foraminifera assemblage. The present facies in this member are mudstone, peloidal mudstone to packstone, and ooidal wackstone to packstone with rare echinoderms. Several ferruginous hardgrounds and marly lime- stone layers were observed. Based on the measurements of car- bon isotopes, the contact with the Oolitic Limestone Member is discordant, as negative carbon excursions are missing. Figure 4: Spectacular outcrop of the Spotty Limestone Member in the Leden- STOP 3 – PODPEČ QUARRY: ica cave Pliensbachian succession of the Global Heritage Stone Railway between Vienna and Trieste (Trst) in the middle of the 19th century, and after the devastating Ljubljana earth- The Podpeč quarry has been studied from geological (Buser quake of 1895. Quarrying probably peaked at this time, as the and Debeljak, 1995; Debeljak and Buser, 1997; Gale, 2015; material was needed for construction (Kramar et al., 2015) Gale and Kelemen, 2017; Brajkovič et al., 2022) and archae- and lime production (Bras, 1977). In the first half of the 20th ological perspectives (Djurić et al., 2022). Based on the dating century, the limestone quarried at Podpeč became a favourite of stone monuments from Emona, the Pliensbachian limestone of the renowned Slovenian architect Jože Plečnik. The already succession at Podpeč was certainly quarried between the 1st mentioned facies with lithiotid bivalves decorates many of the and 3rd centuries AD (Djurić et al., 2022). The production of buildings designed by him (Ramovš, 2000). During the 20th stone from this area, however, might stretch even further back century, most of the smaller quarries ceased operation. The in time to the earliest beginnings of the Roman colony (Djurić main quarry at Podpeč remained active until 1967, at which & Rižnar, 2017). According to Djurić et al. (2022), the Roman time it was owned by the Mineral company (Kramar et al., quarry was positioned at the northernmost tip of the St. Ana 2015; Djurić et al., 2022). hill, topographically closest to the floor of the Ljubljana Moor. The further development of the area from the 4th century to Throughout history, limestone from the Podpeč quarries was the 19th century is obscured by the lack of historical data. valued and used for its good physical properties, low water The Franciscan cadastre of 1823 records two quarry parcels porosity, and high strength, which make it suitable for both in the area of the modern quarry. The quarries gained greater indoor and outdoor use (Mirtič et al., 1999), and was proposed use and recognition during the construction of the Southern as a location of the global heritage stone (Kramar et al., 2015). 130 15TH WORKSHOP Fieldtrip guide. 15th Emile Argand Conference on Alpine Geological Studies, 12-14 September 2022, Ljubljana, Slovenia. Figure 5: The historic “Špica” outcrop within the quarry at Podpeč, where numerous foraminifera, lithiotids, megalodontid bivalves, and brachiopods have been found Limestone beds in the quarry run in a W-E direction and are began as early as the 19th century (Müllner, 1879). Most of the almost vertically inclined (Fig. 5). They comprise various types stone used was local. Carboniferous limestone from the area of limestone: micritic, oolitic, bioclastic, including lumachellas of Ljubljana castle hill was mainly used for city construction, of lithiotid bivalves, megalodontid bivalves, and brachiopods. while the Lower Jurassic Podbukovje Formation was primarily At the microscopic level, the limestone is rich in green algae sourced for limestone used for architectural and sepulchular and foraminifera, including Orbitopsella praecursor, O. pri- applications. As it contains several petrologically indistinguish-maeva, Amijiella amiji, Siphovalvulina spp. , Meandrovoluta able facies types, a spatially more precise definition of the asiagoensis, Duotaxis metula, Involutina farinacciae, Lituolipora provenance of stone products is possible only through multi-termieri, Bosniella oenesis, Pseudopfenderina butterlini, and disciplinary knowledge of the source areas and specific rock Everticyclammina praevirguliana. The lithiotids are dominated properties. Using a multilevel approach (I. Petrology and pa-by Cochlearites and Lithioperna. Lithiotis is rare and limited to leontology; II. Geochemistry; III. Chemostratigraphy), we were the upper part of the quarry. Shells are usually in a parautoch- able to determine the provenance for all facies types present in thonous position, and rarely preserved in vivo. the Podbukovje formation, even those made from uncharacter- istic micritic limestone (Brajkovič et al., 2021, 2022). STOP 4 - LJUBLJANA: Lapidarium of the National Museum of Slovenia In the absence of other (written or pictorial) sources, stone products indirectly provide information on the development, economic activity, trade, and importance of former settlements and cultures (Djurić and Rižnar, 2017). Knowledge about the provenance of stone and its properties links the geological and archaeological disciplines. Research on the provenance of the natural stone used in Emona (present-day Ljubljana) 131 15TH WORKSHOP Fieldtrip guide. 15th Emile Argand Conference on Alpine Geological Studies, 12-14 September 2022, Ljubljana, Slovenia. References Lower Jurassic succession at the site of potential Roman quarry Staje near Ig (Central Slovenia). Geologija, 61(1), 49–71. https://doi. Brajkovič, R., Gale, L., & Djurić, B. (2022). Multi-method study of the org/10.5474/geologija.2018.004 Roman quarry at Podpeč sedimentary succession and stone prod- Sabatino, N., Vlahović, I., Jenkyns, H. C., Scopelliti, G., Neri, R., Pr-ucts. Geologija, 65(1), 101–121. https://doi.org/10.5474/geologi-toljan, B., & Velić, I. (n.d.). Carbon-isotope record and palaeoenvi- ja.2022.007 ronmental changes during the Early Toarcian oceanic anoxic event Brajkovič, R., Žvab Rožič, P., Rožič, B., & Gale, L. (2021). Methodolog- in shallow-marine carbonates of the Adriatic Carbonate Platform ical approach to provenance determination of stone products made in Croatia. Geological Magazine, 150(6), 1085–1102. https://doi. from micritic and fine-grained limestones. Razprave, Poročila = Trea- org/10.1017/S0016756813000083 tises, Reports: 25. Posvetovanje Slovenskih Geologov = 25th Meeting of Vlahović, I., Tišljar, J., Velić, I., & Matičec, D. (2005). Evolution of Slovenian Geologists. the Adriatic Carbonate Platform: Palaeogeography, main events, Bras, L. (1977). Apnenice v Podpeči pod Krimom. Slovenski Etnograf, and depositional dynamics. Palaeogeography, Palaeoclimatology, 30, 75–91. Palaeoecology, 220(3/4), 333–360. https://doi.org/10.1016/j.pa- Buser, S., & Debeljak, I. (1995). Lower Jurassic beds with bivalves in laeo.2005.01.011 South Slovenia. Geologija, 37/38, 23–62. https://doi.org/10.5474/ geologija.1997.001 Debeljak, I., & Buser, S. (1997). Lithiotid Bivalves in Slovenia and Their Mode of Life. Geologija, 40(1), 11–64. https://doi.org/10.5474/ geologija.1997.001 Djurić, B., Gale, L., Brajkovič, R., Bekljanov Zidanšek, I., Horn, B., Lozić, E., Mušič, B., & Vrabec, M. (2022). Kamnolom apnenca v Pod- peči pri Ljubljani in njegovi izdelki. Arheološki Vestnik, 73, 155–198. https://doi.org/10.3986/AV.73.06 Djurić, B., & Rižnar, I. (2016). Kamen Emone = The rocks for Emona. In B. Županek, Emona MM: urbanizacija prostora – nastanek mesta = Urbanisation of space – beginning of a town (pp. 121–144). Dozet, S. (2009). Lower Jurassic carbonate succession between Predole and Mlačevo, Central Slovenia. RMZ - Materials and Geoenviron- ment : Periodical for Mining, Metallurgy and Geology, 56, 164–193. Dozet, S., & Strohmenger, C. (2000). Podbukovje Formation, Central Slovenia. Geologija, 43(2), 197–212. https://doi.org/10.5474/ geologija.2000.014 Gale, L. (2015). Microfacies characteristics of the Lower Jurassic lithi- otid limestone from Northern Adriatic Carbonate Platform Central Slovenia. Geologija, 58(2), 121–138. https://doi.org/10.5474/ geologija.2015.010 Gale, L., & Kelemen, M. (2017). Early Jurassic foraminiferal assemlage in platform carbonates of Mt. Krim, central Slovenia. Geologija, 60(1), 99–115. https://doi.org/10.5474/geologija.2017.008 Kramar, S., Bedjanič, M., Mirtič, B., Mladenović, A., Rožič, B., Skab- erne, D., Gutman, M., Zupančič, N., & Cooper, B. (1999). Podpeč limestone: A heritage stone from Slovenia. In D. Pereira (Ed.), Global heritage stone: Towards international recognition of building and orna- mental stones (pp. 219–231). The Geological Society. Mirtič, B., Mladenović, A., Ramovš, A., Senegačnik, A., Vesel, J., & Vižintin, N. (1999). Slovenski naravni kamen. Geološki zavod Slovenije : ZAG : NTF, OG. Müllner, A. (1879). Emona, archäologische Studien aus Krain. I.V. Klein- mayr & F. Bamberg. Placer, L. (1999). Contribution to the macrotectonic subdivision of the border region between Southern Alps and External Dinarides. Geologija, 41, 223–255. https://doi.org/10.5474/geologija.1998.013 Ramovš, A. (1990). Gliničan od Emone do danes. FNT, Odsek za geologijo. Ramovš, A. (2000). Podpeški in črni ter pisani lesnobrdski apnenec skozi čas. Mineral. Rožič, B., Gale, L., Brajkovič, R., Popit, T., & Žvab Rožič, P. (2018). 132 15TH WORKSHOP Fieldtrip guide. 15th Emile Argand Conference on Alpine Geological Studies, 12-14 September 2022, Ljubljana, Slovenia. Geological tour of Ljubljana FIELDTRIP E Matevž Novak Geological Survey of Slovenia, Dimičeva 14, 1000 Ljubljana, Slovenia (matevz.novak.@geo-zs.si) Introduction The first settlers to use large quantities of stone for building were the Romans. The first Roman settlement was a military This guided tour is intended to help you learn about the cul- stronghold called Colonia Iulia Emona, built in the 1st century tural history of a Middle-European city, as written in natural AD. It was protected with a wall, whose remains are best seen (building and ornamental) stone. It will showcase the City of today along Mirje. The Romans had already opened most of Ljubljana as a small open-space geological museum. Natural the quarries in the surroundings of the Ljubljana Basin, which stone is here presented as a window between natural and were excavated long after World War II. They had quarried Up-cultural heritage. Its great variety enables the study of its per Carboniferous quartz sandstone and conglomerate on the geological features (rock type, fossils, structures) and technical southern slopes of the Ljubljana Castle Hill. They had found properties. On the other hand, it documents Ljubljana’s inter- high quality Lower Jurassic Podpeč Limestone on the southern esting history from the Antiquity through modern times. Here margins of the Ljubljana Moor (see this Guidebook, Field Trip we learn about the most important touristic landmarks of Lju- D) and Glinice Limestone on the northern outskirts of Ljublja-bljana through the types of stone used and the quarries where na at Podutik, which could also have been sources of lime the they originate. Romans used in construction (Ramovš, 1990, 2000). Traces of the Roman transport of heavy products from either the Podutik The highlight of the tour is the stone-built cultural monuments or Podpeč quarries have not been preserved. However, several designed by the renowned architect Jože Plečnik (1872–1957). hypotheses been made regarding that part of the production Very few cities in Europe are marked in such a degree by the cycle in the past. As for the Podpeč Quarry, it has always architecture and urbanistic solutions of a single architect. Jože been – and still is – believed that its products were mainly Plečnik valued natural stone greatly and used it in his most transported along the Ljubljanica River. It is also supposed that monumental works in Ljubljana. Moreover, his post-World War the course of the river was altered in length by roughly 6 km, II work is a good example of the sustainable re-use of natural from Podpeč towards Vrhnika, to flow in the immediate vicin-stone as a building material and as ornamental architectural el- ity of the quarry for purposes of easier transport. Today, this ement. All of these considerations led to the inscribing of “The supposition is widely accepted, despite its rather shaky grounds works of Jože Plečnik in Ljubljana – Human Centred Urban (Djurić and Rižnar, 2016). There were also white to yellowish Design” on the UNESCO World Heritage List in 2021. Here, the varieties of detritic Neogene limestone, which came from a architectural heritage of Jože Plečnik is presented from a dif- number of sources in the vicinity of Moravče and was probably ferent angle, adding another dimension of understanding and only used later, in the 3rd century. The limited use of Peračica appreciation of his opus. Tuff for construction purposes has not yet been determined chronologically, while the colourful, mostly calcareous Škofja Loka Conglomerate was used for architectural elements in A short history of Ljubljana and the use of natural Late Antiquity. As for interregional rocks, the use of Cretaceous stone Aurisina Limestone from Italy has been proven, at least for the earliest period of the Roman colony, while white Eastern Alpine The Ljubljana region was already settled by pile dwellers be- marbles were used in the period for the construction of the de-fore 2,000 BC. Excavations have shown that the quartz sand- fensive walls of Emona (from Gummern) and later for funerary stone rubble was occasionally used to construct the earliest monuments and architectural elements (from Pohorje). Medi-Late Bronze Age settlement (10th–9th c. BCE), but also appeared terranean marbles have only been documented as floor and in later Early and Late Iron Age settlements in foundations, wall veneers (Djurić and Rižnar, 2016). drywalls, and retaining walls. The source of this building ma- terial should certainly be sought in the quarry (or quarries) In the 6th century, Roman Emona was destroyed by the barbaric located in the immediate vicinity of these settlements, some- invasions of the Huns. All of the inhabitants left, and the town where on the southern slopes of Ljubljana Castle Hill (Djurić sank into oblivion. The name Ljubljana was first mentioned and Rižnar, 2016). in the mid-12th century. In 1335, the town passed into the hands of the Habsburgs and became an important stronghold on the way to the sea, and in the hinterland on the border to- 133 15TH WORKSHOP Fieldtrip guide. 15th Emile Argand Conference on Alpine Geological Studies, 12-14 September 2022, Ljubljana, Slovenia. ward the Ottoman Empire. In 1461, the diocese of Ljubljana In addition to the black Lesno Brdo Limestone, variegated, was established, and the church of St. Nicholas became the red, pink, and grey limestone are also still quarried near Lesno cathedral. Medieval Ljubljana evolved around three squares: Brdo. This type of limestone is slightly older than black lime-first around the square of Stari trg, then around the square of stone and formed during the same age and in a shallow reef Mestni trg, and around Novi trg square on the other side of environment, much like Hotavlje Limestone, as described later. the Ljubljanica River. Houses in medieval times were largely constructed of wood, and stone was only used for the walls, The end of the 18th century brought the Age of Enlightenment, independently surrounding all three parts. The medieval walls a period that rediscovered antiquity, among other things. In on Vegova Street were built atop roughly the exact site of the terms of architecture, it marked the emergence of Classicism, former Roman wall; however, Emona was located to the west, which returned to the models of Greek antiquity. In Ljubljana, and medieval Ljubljana to the east of the wall. Until 1484, they started to pull down the wall that had halted expansion of when the City Hall was built on the same site it occupies today, the town. the medieval town centre was at Tranča, next to the Cobblers’ Bridge (Spanžel et al., 2020). After Napoleon’s wars with the Austrian monarchy, Lju- bljana was occupied by the French, and for a short period In 1511, a major earthquake (the Idrija Earthquake, estimat- (1809−1813) became the capital of the Illyrian Provinces. ed M6.8, X EMS), struck Ljubljana and caused a great deal While this was not an important period in terms of architecture of damage all over Carniola. During the restoration process, it had far-reaching implications for Slovenian national aware-narrow medieval houses were linked, and roof ridges were ness, as it was the first time ever that the Slovenian language oriented parallel to the street. was taught in higher schools. For this reason, Napoleon has never been seen as an oppressive occupier, and the inhabitants In the 17th and 18th centuries stone buildings began to replace of Ljubljana even erected a monument in his honour. The four the wooden ones. What proved more defining were the reli- years of the Illyrian Provinces represented the only break in the gious conflicts that arose when the triumphant Counter-Ref- Habsburg regime, which lasted a whole 579 years, from 1335 ormation introduced the Baroque. For the Jesuits, who came to 1918 (Spanžel et al., 2020). to Ljubljana in 1597 and decisively contributed to the defeat of the Reformation, both Gothic and Renaissance architecture After Napoleon’s defeat the town rose from anonymity once were unacceptable. Only Baroque churches, with their magnif- again. In 1821 it hosted the congress of the Holy Alliance, an icence and ceremonial grandeur, had the power to inspire in association of triumphant states striving to maintain the mo-rituals of worship. Baroque art was therefore more than simply narchic system. For this occasion, the site of the abandoned a matter of taste; it was a symbol of affiliation with the Roman Capuchin monastery was transformed into Congress Square, Catholic church. The Baroque reached its peak at the beginning which served to host public events and parades. This was a of the 18th century when, also on the initiative of the Academia period marked by the first attempts at a systematic designing of Operosorum Labaciensis (1693−1701), some prominent Ital- the town. Biedermeier, a reflection of the simple and comfort-ian artists, mainly from the neighbouring Venetian Republic, able style of the Viennese middle class, dominated in art. came to work in Ljubljana: architect Andrea Pozzo and sculp- tors Francesco Robba and Jacopo Contieri, to name but a few. In 1848, a railway was built from Vienna to Ljubljana, and in Houses were raised with a third floor and dressed in luxurious 1857 it was extended south to the port of Trieste. The train was Baroque façades. Interiors were decorated with arcaded court- a symbol of a new era based on industrialization. It triggered yards and staircases. They also renovated or built most of the an accelerated development of cities and posed new challenges churches in the Baroque style, including the cathedral, as well for architecture. Work was now divided between architect and as the new town hall (Spanžel et al., 2020). This period proved engineer. The latter designed a frame that the architect-artist a major milestone in terms of the use of stone in Ljubljana. The adorned with an appropriate façade. Classical architectural ele-dark Upper Triassic limestone quarried on the slopes of Lesno ments gradually embraced neo-Renaissance, neo-Romanesque, Brdo/Drenov Grič (west of Ljubljana) was very popular in Lju- and neo-Gothic elements. During this fertile period, a number bljana and vicinity from the end of the 17th century onwards of important institutions were built in Ljubljana: the Provincial (Ramovš, 2000). Lesno Brdo limestone is distinguished by its Museum, the National Hall, the Philharmonic Hall, and the Pal-uniform black colour, which is animated by numerous white ace of the Provincial Government (Spanžel et al., 2020). calcite veins. It formed in the shallow lagoon environment in the Late Triassic (Carnian) and it often contains numerous The 1895, a hugely destructive earthquake (“the Big Ljublja-fossils, especially bivalve shells. Interlayers of the softer black na Earthquake”, M6.1, VIII–IX EMS) proved a turning point marlstone are less resistant to weathering and give way to in Ljubljana’s development. Some ten percent of the city’s decomposition. The entrance portal to the Seminary Palace buildings were severely damaged or destroyed. The whole of with its two stone giants is one of the finest Baroque portals in the monarchy assisted in the rebuilding effort, and what had Ljubljana. started as utter destruction became an opportunity for new development. A young architect, Maks Fabiani, who at the time 134 15TH WORKSHOP Fieldtrip guide. 15th Emile Argand Conference on Alpine Geological Studies, 12-14 September 2022, Ljubljana, Slovenia. worked for Professor Otto Wagner at the Vienna Academy, took however, their white cross sections are beautiful adornments to the initiative to propose an urban design plan. It was Fabiani the otherwise deep, dark stone. Plečnik, as well as some other who introduced the Viennese Secession style, closely related to architects, used this stone in many other prominent buildings, Art Nouveau, to Ljubljana. During this period of national awak- such as in the Parliament building, Nebotičnik (Ljubljana Sky-ening, when Slovenians were establishing their own cultural scraper), the Montanistika building, City Hall, etc. (Kramar et institutions in parallel to the existing German ones, the choice al., 2014). of architectural style became a sign of nationality (Spanžel et al., 2020). In the mere first 14 years after the earthquake, One of the most appreciated decorative stones in Ljubljana more than 400 buildings were built and more than 600 were was, and still is, the Upper Triassic Hotavlje Limestone. This renovated. Most of Ljubljana’s bridges, monuments, parks, and reef limestone is characterized by its non-homogeneous texture main buildings date back to the post-earthquake development. and richly varied colour, which ranges from dark grey to grey Already two years after the earthquake, the first Austro-Hun- and pink, to scarlet red. The colours are further enriched by garian seismological observatory was established in the base- veins of reddish claystone and green tuff. Larger nests are filled ment of the Realka High School on Vegova Street in Ljubljana. with bright calcite, tiny grains of pyrite, and yellow or purple rhombohedral dolomite crystals, which formed during diagen- The post-earthquake (1895) renovation allowed Ljubljana to esis. Its larger-scale quarrying begun after WW II; however, develop from its earlier provincial appearance into a modern the first stone-cutters’ products from this limestone are docu-European city. After the dissolution of the Austro-Hungarian mented from the early 18th century (Ramovš, 1995). Today, this Monarchy the city became the capital of Slovenia – and the limestone is still being excavated in the underground galleries people’s capital; and was looking for its own architectural iden- of a large modern quarry. In the interior of the Cankarjev dom, tity, which was to be shaped by architect Jože Plečnik. He was the largest culture and congress centre in Slovenia, as many certainly one of the most talented of Otto Wagner’s students. as 2000 m2 of surface is covered with panels of Hotavlje Lime-Prior to World War I, he had already designed several build- stone. ings in Vienna, the most important being the Zacherl House (1905). The Vienna Academy had even proposed Plečnik as Some of the most widely used stones in modern Ljubljana are Wagner’s successor, but for political reasons the proposal was various “karst stones”, the common name for light-grey lime-not approved. In 1911, Plečnik moved to Prague to teach at the stones of Cretaceous age with cross sections of rudist bivalves. college of arts and crafts, and in 1920 was appointed by Presi- They come from the quarries of Aurisina/Nabrežina near Trident Masaryk as chief architect for the restoration of Hradcany este, Lipica, Doline, and Kazlje in Slovenian Kras, and Rasotica with Prague Castle, which was to be transformed into a symbol on the Croatian island of Brač. In Lipica in Kras, two different of the new, democratic state. Despite this prestigious position, grey limestones are quarried; they are called “uniform” (Lipica Plečnik returned to Ljubljana in 1921 when he was offered the unito) and “rosy” (Lipica fiorito) limestone. In Lipica unito, post of professor at the newly founded school of architecture. It rudist bivalves are finely crushed and give the impression of a was in Ljubljana that he wanted to see his vision of the nation’s unified grainy rock, while in Lipica fiorito, the cross sections capital come to life. He respected the qualities of the old quar- of whole rudists resemble flower petals. The Repen and Koter of Ljubljana, the natural, architectural, and historic char- priva limestones from the Doline quarry are very fine grained acteristics with their intangible aspects, which he emphasised and considered the highest quality calcareous natural stones with both small and large interventions. He interpreted anew in Slovenia (Mirtič et al., 1999). The Karst limestones were a series of public spaces (squares, parks, streets, promenades, used in the construction of several important buildings and bridges) and public institutions (national library, churches, monuments in many other European Countries, and around markets, funerary complex), which he sensitively integrated the world. Nowadays, they are most commonly used in the into the pre-existing urban, natural, and cultural context and construction of façade cladding, pavements, staircases, indoor which contributed to the city’s new identity. The dialogue be- and outdoor flooring and wall cladding, and are also held in tween the architect and the town developed to the extent that high esteem by sculptors. today Ljubljana is known as “Plečnik’s Ljubljana” (Spanžel et al., 2020). We tore the stone from our mountains, our hands formed and smoothed it: saxa loquuntur (rocks speak). – Arch. Jože It can be said that the most iconic Plečnik’s building in Lju- Plečnik, 1926 bljana, the National and University Library, is his monument to Podpeč Limestone. He used it in the façade, the entrance We welcome you to learn more about the natural stones of Lju-lobby, the staircase colonnade and the large lobby. The exte- bljana from the booklet A geological tour of Ljubljana: natural rior is made of this lagoonal limestone, most of it without the stone in cultural monuments. Available as a PDF at: typical lithitoid bivalves. On the polished interior surfaces, www.ljubljana.si/assets/Uploads/Geoloski-sprehod-po-Ljubljani-ANG.pdf 135 15TH WORKSHOP Fieldtrip guide. 15th Emile Argand Conference on Alpine Geological Studies, 12-14 September 2022, Ljubljana, Slovenia. Figure: List of Slovenian and foreign natural stones used in Ljubljana with their stratigraphic position (Novak, 2016) 136 15TH WORKSHOP Fieldtrip guide. 15th Emile Argand Conference on Alpine Geological Studies, 12-14 September 2022, Ljubljana, Slovenia. References Djurić, B., & Rižnar, I. (2016). Kamen Emone = The rocks for Emona. In B. Županek, Emona MM: urbanizacija prostora – nastanek mesta = Urbanisation of space – beginning of a town (pp. 121–144). Kramar, S., Bedjanič, M., Mirtič, B., Mladenović, A., Rožič, B., Skab- erne, D., Gutman, M., Zupančič, N., & Cooper, B. (1999). Podpeč limestone: A heritage stone from Slovenia. In Global heritage stone (pp. 219–231). The Geological Society. Mirtič, B., Mladenović, A., Ramovš, A., Senegačnik, A., Vesel, J., & Vižintin, N. (1999). Slovenski naravni kamen. Geološki zavod Slovenije : ZAG : NTF, OG. Novak, M. (2016). A geological tour of Ljubljana: Natural stone in cul- tural monuments. Municipality of Ljubljana, Department for environ- mental protection. Ramovš, A. (1990). Gliničan od Emone do danes. FNT, Odsek za geologijo. Ramovš, A. (1995). Hotaveljčan skozi čas. Marmor Hotavlje. Ramovš, A. (2000). Podpeški in črni ter pisani lesnobrdski apnenec skozi čas. Mineral. Spanžel, Š., Štoka, T., Karo, Š., Kavčič, M., & Zupančič, B. (2020). Ljubljana: The timeless, human capital designed by Jože Plečnik: Nom- ination for Inscription on the World heritage List. Ministry of Culture, Cultural Heritage Directorate. The works of Jože Plečnik in Ljubljana – Human Centred Urban Design. (2021). UNESCO : World Heritage Center. UNESCO website: The works of Jože Plečnik in Ljubljana – Human Centred Urban Design 137 15TH WORKSHOP Fieldtrip guide. 15th Emile Argand Conference on Alpine Geological Studies, 12-14 September 2022, Ljubljana, Slovenia. 138 15TH WORKSHOP Abstract book & Fieldtrip guide. 15th Emile Argand Conference on Alpine Geological Studies, 12-14 September 2022, Ljubljana, Slovenia. Index of authors Geological tour of Ljubljana FIELDTRIP E Aherwar Kishan ................................... 11 Fellin Maria Giuditta ........................... 60 Janák Marian ...................................... 97 Al Najjar Lina ...................................... 65 Ferenc Štefan ...................................... 31 Janots Emilie ....................................... 24 Alvaro Matteo ......................... 22, 23, 46 Festa Andrea ....................................... 12 John Timm .................................... 15, 69 Angel Ross J. ....................................... 23 Filippi Marco ....................................... 70 Jozi-Najafabadi Azam ......................... 39 Fuček Ladislav..................................... 67 Babajić Elvir ........................................ 66 Fodor László ............................ 19, 61, 97 Karádi Viktor ....................................... 34 Badurina Luka ..................................... 64 Katanić Petar ....................................... 66 Baize Stephane ................................... 65 Gaidzik Krzysztof ................................ 36 Kazmer Miklos .................................... 36 Balázs Attila ........................................ 19 Gale Luka ................ 37, 59, 75, 121, 128 Kästle Emanuel ................................... 35 Balestro Gianni ................................... 12 Gallhofer Daniela .......................... 58, 62 Kelemen Péter ..................................... 19 Ballèvre Michel ............................. 42, 50 Garašić Vesnica ................................... 14 Klotz Thomas ................................ 54, 63 Balling Philipp ............................... 13, 40 Gautheron Cécile ................................ 51 Kocjančič Anja ............................... 37, 59 Barbero Eedoardo ............................... 12 Gawlick Hans-Jürgen .............. 20, 48, 68 Kohn Victoria ...................................... 15 Barretto Jenny Anne ........................... 45 Genser Johann .................................... 17 Kolar-Jurkovšek Tea ...................... 37, 59 Baumgartner Lukas ............................. 51 Gerčar David ................................. 21, 25 Konečný Patrik .................................... 57 Belak Mirko ......................................... 64 Germer Marisa .................................... 15 Kopáčik Richard .................................. 31 Bellahsen Nicolas .......................... 16, 32 Ghiglione Matias ................................. 51 Könemann Vincent .............................. 15 Bereczki László.................................... 30 Ghignone Stefano ............................... 22 Kövér Szilvia ................................. 19, 61 Bernet Matthias ................................... 51 Gilio Mattia ............................. 22, 23, 46 Krobicki Michał ................................... 38 Bergemann Christian .......................... 24 Girani Alice ......................................... 23 Kukoč Duje .............................. 64, 67, 75 Berger Alfons ...................................... 24 Giuntoli Francesco .............................. 46 Kylander-Clark Andrew ....................... 18 Bienveignant Dorian ........................... 65 Gnos Edwin ......................................... 24 Bilić Šime ............................................ 14 Görög Ágnes ....................................... 61 Langone Antonio ........................... 18, 41 Bobek Kinga ........................................ 33 Grabowski Jacek ................................. 25 Lasseur Eric ......................................... 32 Bogićević Katarina .............................. 68 Grgasović Tonći ............................. 64, 67 Le Breton Eline ................................... 39 Borleanu Felix ..................................... 28 Greenwood Andrew ............................ 26 Lemoine Anne ..................................... 65 Borghi Alessandro ...............................12 Grenier Mattis ..................................... 27 Li Botao ............................................... 44 Brajkovič Rok .............................. 59, 128 Grujic Djordie ..................................... 51 Liesegang Moritz ................................ 69 Braucher Régis ....................................11 Grützner Christoph ................. 27, 49, 56 Liu Yongjiang ...................................... 17 Braun Jean ..........................................51 Guan Qingbin ...................................... 17 Livio Franz .................................... 22, 60 Briais Justine .......................................32 Gyorfi Istvan ....................................... 28 Loget Nicolas ...................................... 32 Bruno Marco .......................................22 Lőrincz Katalin .................................... 30 Brunsmann Olga .................................15 Haberland Christian ............................ 39 Löwe Georg ......................................... 40 Brunsmann Quentin ............................16 Handy Mark R ............................... 29, 39 Bućković Damir ...................................43 Hannouz Estelle .................................. 65 Maino Matteo .......................... 18, 41, 52 Bujtor László .......................................68 Héja Gábor .................................... 19, 30 Manzotti Paola .............................. 42, 50 Hérman Fréderic ................................. 51 Markos Gábor ..................................... 30 Casini Leonardo ..................................41 Hermann Markus ................................ 27 Márton Emö ........................................ 43 Celarc Bogomir ...................................37 Hetényi György ................................... 26 Maros Gyula ........................................ 30 Chang Ruihong ...................................17 Hitij Tomaž ....................................... 121 Martinez Mathieu................................ 33 Chmielewski Andrzej ..........................25 Hoppanová Eva ................................... 31 Martinod Joseph ................................. 51 Corvò Stefania .............................. 18, 41 Hók Jozef ............................................ 11 Massonne Hans-Joachim ..................... 44 Csillag Gábor....................................... 19 Huang Qianwen .................................. 17 McPhee Peter J. ................................... 39 Chyba Andrej ...................................... 11 Huet Bastien ....................................... 32 Milsom John ....................................... 45 Hurai Vratislav .................................... 57 Mingardi Giulia ................................... 46 Ćosović Vlasta .....................................43 Huraiová Monika ................................ 57 Mladenović Ana .................................. 47 Husson Laurent ................................... 51 Molčan Matejová Marína .................... 53 De Caroli Sara .....................................12 Molli Giancarlo ................................... 16 Drobne Katica .....................................43 Iglseder Christoph ......................... 58, 62 Moro Alan ........................................... 43 Dunkl István ........................................19 Imre Gábor .......................................... 43 Mrdak Milica ....................................... 48 Ivančič Kristina ................................... 97 Mullis Josef ......................................... 24 Đerić Nevenka ............................... 48, 68 Iwańczuk Jolanta .......................... 25, 33 Musiyachenko Kira A. ......................... 46 Đaković Martin ................................... 48 Mücklisch Mark ................................... 49 139 15TH WORKSHOP Abstract book & Fieldtrip guide. 15th Emile Argand Conference on Alpine Geological Studies, 12-14 September 2022, Ljubljana, Slovenia. Müntener Othmar ............................... 26 Shuster David...................................... 51 Sieberer Anna-Katharina ............... 54, 63 Nabhan Sami ...................................... 40 Simon-Labric Thibaud ......................... 51 Nemec Ondrej ..................................... 66 Slapnik Lucjia ..................................... 25 Németh András ................................... 19 Slovenec Damir ............................. 64, 67 Nenadić Draženko ............................... 68 Smirčić Duje ........................................ 64 Neubauer Franz .................................. 17 Soós Balázs ......................................... 19 Nosenzo Francesco ........................ 42, 50 Spalla Maria Iole ................................. 70 Novak Matevž ............................. 75, 133 Sperner Blanka ................................... 40 Nyerges Anita ...................................... 19 Sternai Pietro ...................................... 51 Nyíri Dániel ......................................... 19 Stubenrauch Jakob ............................. 27 Sudar Milan ........................................ 48 Oravecz Éva ........................................ 19 Sue Christian................................. 51, 65 Ortner Hugo ........................................ 63 Šebela Stanka .....................................75 Paiva Muller Veleda Astarte ................. 51 Šegvić Branimir ................................... 64 Palotai Márton .................................... 30 Šimonová Viera ................................... 31 Pavšič Jernej ........................................ 21 Šmuc Andrej ....................................... 75 Perozzo Michele ............................ 41, 52 Šujan Michal ....................................... 11 Petrescu Laura ..................................... 28 Pfänder Jörg A. ................................... 40 Tomljenović Bruno .............................. 13 Piazolo Sandra .................................... 18 Tőkés Lilla ........................................... 19 Pistone Mattia ..................................... 26 Tropper Peter ...................................... 54 Pitra Pavel ........................................... 42 Tsukamoto Sumiko ....................... 49, 56 Plašienka Dušan ............................ 53, 55 Pleuger Jan ................................... 15, 69 Ustaszewski Kamil....... 13, 27, 40, 49, 56 Pohl Alexandra .................................... 15 Ustalić Samir ....................................... 66 Pomella Hannah ............................ 54, 63 Popit Tomislav ..................................... 59 Valla Pierre .......................................... 51 Potočný Tomáš .............................. 53, 55 Vodnik Primož ............................... 37, 59 Prelević Dejan ..................................... 40 van Schrojenstein Lantman Hugo W. ... 23 Prince Erick ................................... 49, 56 Vojtko Rastislav ................................... 11 Putiš Marián ........................................ 66 von Quadt Wykradt-Hüchtenbruck Albrecht .............................................. 40 Reato Luca .......................................... 57 Vrabec Marko .................. 19, 56, 97, 121 Regorda Alessandro ............................ 70 Vrabec Mirijam .................................. 97 Rehakova Daniela ............................... 25 Vukovski Matija ............................. 64, 67 Reicherter Klaus .................................. 27 Vuletić Marija ...................................... 68 Reiners Peter ....................................... 51 Reiser Martin .......................... 54, 58, 62 Walpersdorf Andrea ............................ 65 Ricchi Emmanuelle ............................. 24 Wannhoff Iris ...................................... 69 Roda Manuel ....................................... 70 Waśkowska Anna ................................ 21 Rosenberg Claudio .............................. 16 Willingshofer Ernst ............................. 63 Rózsová Barbara ................................. 11 Woodland Alan B. ............................... 14 Rožič Boštjan......... 21, 25, 37, 59, 61, 75 Ružička Peter ...................................... 66 Yuan Sihua .......................................... 17 Scaramuzzo Emanuele .................. 22, 60 Zadravecz Csilla .................................. 19 Scambelluri Marco .............................. 23 Zanetti Alberto .................................... 26 Scherman Benjamin ............................ 61 Zanoni Davide ..................................... 70 Schneider David .................................. 58 Zhong Xin ..................................... 15, 69 Schneider Susanne .............................. 40 Ziberna Luca ....................................... 26 Schenker Filippo ........................... 41, 52 Zupančič Nina ............................... 21, 59 Schiavi Federica .................................. 42 Schuster Ralf ........................... 54, 58, 62 Žvab Rožič Petra ................... 25, 59, 128 Selmeczi Ildikó .................................... 19 Seno Silvio .............................. 18, 41, 52 140 15TH WORKSHOP Abstract book & Fieldtrip guide. 15th Emile Argand Conference on Alpine Geological Studies, 12-14 September 2022, Ljubljana, Slovenia. Financially supported by: 141 Mangart Saddle, photographed in direction to the south. Document Outline Abstract book Dating a long-lived lake in an intermontane basin: Late Miocene Lake Turiec in the Western Carpathians Multistage tectono-stratigraphic evolution of the Canavese Zone (Western Alps) The inversion of a passive continental margin portrayed by a 2D balanced kinematic forward model across the Velebit Mt. in the northern external Dinarides fold and thrust belt Two types of peridotites in the area of Banovina, Croatia and their Petrogenesis Barometric studies on different rock types from the Adula Nappe (Central Alps) by Raman spectroscopy of quartz inclusions in Garnet The arc of the western Alps: a review and new kinematic model Hf isotopic constraints for Austroalpine basement evolution of Eastern Alps: review and new data Multiscale lithological and structural heterogeneity control on the nucleation of a crustal shear zone: petro-structural investigation and U-Pb titanite dating from the Anzola shear zone (Ivrea-Verbano Zone, Southern Alps) Migration of basin formation and contrasting deformation style in the south-western Pannonian Basin (central Europe) Middle-Late Jurassic ophiolite obduction and formation of sedimentary mélanges in the Western Tethys Realm Upper Campanian bentonites of volcaniclastic origin in the Scaglia-type limestones of the Adria continental margin First evidence of UHP in the Lago Superiore Unit (Monviso, Western Alps) The prograde history of three Mn-rich garnets from the UHP Lago di Cignana Unit (Italy) Episodes of open fissure formation in the Alps Magnetic susceptibility and chemostratigraphy of the Jurassic/Cretaceous boundary interval – new data from the Slovenian Basin Project DIVE (Drilling the Ivrea-Verbano zonE): A joint petrological, geochemical, and geophysical exploration of the lower continental crust Remote sensing of active tectonics in NE Italy, eastern Southern Alps Alpine-Carpathian-Pannonian Geodynamics: the McKenzie and Royden models and the limitations of their applicability How AlpArray is guiding us to a new model of Alpine orogenesis A buried fold and thrust belt: the structural geometry of the central part of the Tisza Unit, East Hungary New knowledge about U-Cu mineralization in the Kozie Chrbty Mts. and its relationship to the late (Neotectonic) structures (Hronic Unit, Western Carpathians, Slovakia) Palaeoenvironmental and drainage network reconstitution of the Oligocene Western Alpine Foreland Basin Recording of cyclicity in the sediments of the Bajocian and Lower Bathonian on the basis of magnetic susceptibility (Carpathians, Poland) On the way to building the Norian conodont biozonation of the Circum-Pannonian Region Crustal structure in the eastern Alps from ambient-noise Tomography Seismic activity along the Periadriatic and Sava Faults in the past two millennia – an archaeoseismological assessment Facies analysis of Ladinian and Carnian beds in the area of Rute Plateau (External Dinarides, Central Slovenia) Origin of submarine swell (Czorsztyn Ridge of the Pieniny Klippen Belt, Polish/Ukrainian Carpathians) and it’s geotectonic consequences by biostratigraphy/volcano-sedimentary record Variation in style of Adriatic lower crust indentation west and east of the Giudicarie Fault Exhumation of metamorphic core complexes of the internal Dinarides was triggered by the opening of the Pannonian Basin Challenges in the interpretation of the structural and metamorphic record in the Adula and Cima Lunga units (Central Alps) A journey towards the forbidden zone: a new, cold, UHP unit in the Dora-Maira Massif (Western Alps) Tectonic implications of paleomagnetic results from the Northern Adriatic area: an overview Pressure-temperature-time evolution of Austroalpine metamorphic rocks from the southeastern Pohorje Mountains Anagolay: the shape of the Philippines and the Luzon Syntaxis Quartz and zircon in garnet elastic geobarometry of HP rocks from the Sesia Zone How active is recent tectonics in the central Balkans: Evidence from the Serbian Carpatho-Balkanides Partial drowning or backstepping of the Early Norian Dachstein Carbonate Platform in the Dinarides (Poros, Montenegro) New data on the Late Pleistocene evolution of the Klagenfurt Basin, Austria Nappe stacking and syn-nappe folding in the northern Dora-Maira Massif (Western Alps) Exhumation response to climate and tectonic forcing in the southern Patagonian Andes (Torres del Paine and Fitz Roy plutonic complexes) Discovery of sheath folds in the Adula nappe and implications for the tectonic evolution (Central Alps) Lower to Middle Jurassic clastic formations of the Western Carpathian Klippen Belt: testimony to the rifting-breakup-drifting Processes The thermotectonic evolution in front of the Dolomites Indenter Calcite microstructures recording polyphase deformation history of the Meliata Unit Finding Quaternary Seismogenic Activity Along the Eastern Periadriatic Fault System: Dating of Fault Gouges via Electron Spin Resonance Formation of esseneite and kushiroite in calc-silicate skarnoid xenoliths from Southern Slovakia Age and structure of the Stubai Alps (Ötztal-Nappe, Tyrol/Austria) Architecture and sedimentary evolution of the Ladinian Kobilji curek Basin of the External Dinarids (Rute Plateau, central Slovenia) From Permian to rift-inception: new insight from the Western Southern Alps (Varese Area) Platform to basin transitions: mapping observations at the Krvavica Mountain, and Čemšeniška Planina, in the Sava Folds Region Geological history of the Troiseck-Floning Nappe (Austroalpine unit, Styria/Austria) Internal deformation and tectonic evolution of the Dolomites Indenter, eastern Southern Alps: A combined field and analogue modelling study Differentiation and genesis of the Middle Triassic mafic volcanic and volcaniclastic facies in NW Croatia - case study from Vudelja quarry Tectonic Transfer from the Western Alpine Front to the French Rhône Valley in its 3D-Structural Context Petrography of ultrabasic and basic rocks from the Ozren ophiolite complex (Bosnia and Herzegovina) Jurassic pelagic succession of NW Croatia – a key to better understanding tectonic setting of the Southern Alps – Dinarides transition zone The Albian/Cenomanian Boundary Event (OAE1d) reflected in ammonite-rich layers in central Serbia (Topola area) Peak pressure estimates of Koralpe-Saualpe-Pohorje Complex based on Raman Spectroscopy Tectonic and metamorphic record in the Badstub Formation, Carboniferous of Nötsch, Austroalpine Fieldtrip guide Adria margin of the Alpine-Dinaric transition area – sedimentary view and a structural glimpse Metamorphism, deformation, exhumation, and basin formation in NE Slovenia, in the Pohorje-Kozjak Mts. Marine reptile-bearing Anisian limestone of the Velika planina mountain pasture Lower to Middle Jurassic limestone succession at the margin of the Ljubljana Moor: From microfacies to the Romans Geological tour of Ljubljana Index of authors