FIELD TRIP GUIDEBOOK

Edited by Ewa Głowniak, Agnieszka Wasiłowska IX ProGEO Symposium

Geoheritage and Conservation: Modern Approaches and Applications Towards the 2030 Agenda

Chęciny, Poland 25-28th June 2018

FIELD TRIP GUIDEBOOK

Edited by Ewa Głowniak, Agnieszka Wasiłowska This publication was co-financed by Foundation of University of Warsaw and ProGEO – The European Association for the Conservation of the Geological Heritage

Editors: Ewa Głowniak, Agnieszka Wasiłowska

Editorial Office: Faculty of Geology, University of Warsaw, 93 Żwirki i Wigury Street, 02-089 Warsaw, Poland

Symposium Logo design: Łucja Stachurska

Layout and typesetting: Aleksandra Szmielew

Cover Photo: A block scree of Cambrian quartzitic sandstones on the slope of the Łysa Góra Range – relict of frost weathering during the Pleistocene. Photograph by Peter Pervesler

Example reference: Bąbel, M. 2018. The Badenian sabre gypsum facies and oriented growth of selenite crystals. In: E. Głowniak, A. Wasiłowska (Eds), Geoheritage and Conservation: Modern Approaches and Applications Towards the 2030 Agenda. Field Trip Guidebook of the 9th ProGEO Symposium, Chęciny, Poland, 25–28th June 2018, 55–59. Faculty of Geology, University of Warsaw, Poland.

Print: GIMPO Agencja Wydawniczo-Poligraficzna, Marii Grzegorzewskiej 8, 02-778 Warsaw, Poland

©2018 Faculty of Geology, University of Warsaw

ISBN 978-83-945216-5-3

The content of abstracts are the sole responsibility of the authors

Organised by Faculty of Geology, University of Warsaw Institute of Nature Conservation, Polish Academy of Science Kielce Geopark Polish Geological Institue – National Reserach Institute

Under the auspices of ProGEO – The European Association for the Conservation of the Geological Heritage IUGS International Commission on GeoHeritage IUCN WCPA Geoheritage Specialist Group Marshal of the Holy Cross Province Mayor of the Chęciny Town and Municipality Rector of the University of Warsaw

Co-financed by Faculty of Geology, University of Warsaw ProGEO – The European Association for the Conservation of the Geological Heritage Rector of the University of Warsaw University of Warsaw Foundation

Partners European Center of Geological Education of the University of Warsaw Bochnia Salt Mine Museum of the Kielce Village Ojców National Park Journal of GeoHeritage PATRONS

PARTNERS

THE ORGANISING COMMITTEE WOULD LIKE TO ACKNOWLEDGE THE VALUABLE SUPPORT OF OUR PATRONS AND PARTNERS CONTENTS

Pre-symposium Field Trip – Top Geosites of the Kraków Region ...... 9 Convener and Leaders ...... 9 Itinerary of the Pre-symposium Field Trip ...... 10 Geological framework of the Kraków Region Jan Urban ...... 11

Bochnia area ...... 14 Stop 1.1. Bochnia Salt Mine Leaders: Michał Flasza and The Bochnia Salt Mine Guides ...... 14 Geological history of the Bochnia Salt Mine Michał Flasza ...... 14

Kraków City ...... 18 Stop 1.2. Krakus Mound Leader: Jan Urban ...... 18 Lithostratigraphy and tectonics as a factor controlling geomorphology of the Kraków area Jan Urban ...... 18 Stop 1.3. Bonarka Nature Reserve Leader: Jan Urban ...... 22 Mesozoic history of the Kraków area Jan Urban ...... 22 Stop 1.4. Wawel Hill and Royal Castle Leader: Jan Urban ...... 24 Kraków Old City and Wawel Royal Castle as an illustration of geological constraints of human history Jan Urban ...... 24 Stop 1.5. Wawel Hill and Smocza Jama (Dragon’s Den) Cave Leaders: Michał Gradziński and Jan Urban ...... 27 Smocza Jama Cave ‒ its origin, scientific potential and cultural importance Michał Gradziński, Jan Urban ...... 27

Ojców National Park ...... 30 Stop 2.1. The Kraków Gate rock Leaders: Piotr Ziółkowski and Józef Partyka ...... 30 Highlights of the Ojców National Park Józef Partyka ...... 30 Origin of the Upper Jurassic limestone Piotr Ziółkowski ...... 30 Stop 2.2. Ciemna Cave Leader: Michał Gradziński and Jan Urban ...... 33 Geomorphology and genesis of Ciemna Cave Michał Gradziński ...... 33 Stop 2.3. Władysław Szafer Natural History Museum Leader: Józef Partyka ...... 35 Bio- and cultural heritage of the Ojców National Park and its protection and conservation Józef Partyka ...... 35

6 CONTENTS

Stop 2.4. The Maczuga Herkulesa (Hercules’ Club) crag and Pieskowa Skała Castle Leader: Piotr Ziółkowski ...... 37 Neogene morphogenesis of the Ojców Plateau Piotr Ziółkowski ...... 37 Poniedzie Region ...... 38 Stop 2.5. Chotel Czerwony Leaders: Maciej Bąbel, Jan Urban and Anna Chwalik-Borowiec ...... 38 The Badenian Nida Gypsum deposits and their unique giant crystal facies Maciej Bąbel ...... 38 Structural morphology and karst developed in various rocks e.g. gypsum and marl Jan Urban and Anna Chwalik-Borowiec ...... 43 Stop 2.6. Skorocice and Skorocicka Valley Leaders: Jan Urban, Maciej Bąbel and Anna Chwalik-Borowiec ...... 46 The facies of the lower selenite unit of the Nida Gypsum deposits at Skorocice Maciej Bąbel ...... 46 Blind karst valley with numerous associated caves (karst conduits) as a unique example of active karst Jan Urban and Anna Chwalik-Borowiec ...... 49 Stop 2.7. Siesławice Leaders: Maciej Bąbel and Jan Urban ...... 54 The Badenian sabre gypsum facies and oriented growth of selenite crystals Maciej Bąbel ...... 54 Gypsum karst developed in stagnant underground water: underground chambers and lakes Jan Urban ...... 60

Post-symposium Field Trip ‒ Top Geosites of Góry Świętokrzyskie ...... 63 Convener and Leaders ...... 63 Itinerary of the Post-symposium Field Trip ...... 64 Geology of Góry Świętokrzyskie (Holy Cross Mountains) Stanisław Skompski ...... 65 Stop 1. Miedzianka Hill Leader: Stanisław Skompski ...... 67 Geological panorama of south-western corner of the Holy Cross Mountains Boguslaw Waksmundzki ...... 67 Stop 2. Northern wall of Ostrówka Quarry Leader: Stanisław Skompski ...... 70 Frasnian (Upper Devonian) to Permian stratigraphic succession demonstrating depositional evolution from carbonate platform trough condensed pelagic limestones to basinal setting with sediment-gravity flows and finally epi-Variscan unconformity Stanisław Skompski ...... 70 Stop 3. Kadzielnia Quarry Leader: Stanisław Skompski ...... 75 Devonian carbonate build-up covered by stratigraphically condensed Famennian section; neptunian dykes Stanisław Skompski ...... 75 Stop 4. Górno Quarry Leader: Stanisław Skompski ...... 77 Upper Devonian succession typical of Kostomłoty facies: transition from deep basin to slope allochthonous deposits, redeposited from the Central Carbonate Platform of Kielce Region Stanisław Skompski ...... 77

7 9th ProGEO Symposium, Chęciny, Poland, 2018

Stop 5. Krzemionki Opatowskie – prehistoric flint mines Leader: Stanisław Skompski ...... 79 Upper Jurassic shallow water succession with horizons of striped flint concretions; underground route presenting prehistoric flint mines functioning for most of the Neolithic age and at the beginning of the Bronze Age (3900–1600 B.C.); a candidate for the UNESCO World Heritage List Stanisław Skompski ...... 79 Stop 6. Łysa Góra Leader: Ewa Głowniak ...... 82 The highest range of the Holy Cross Mountains; boulder fields (gołoborze) of periglacial origin; biostratigraphic data on the Cambrian of Łysogóry Anna Żylińska ...... 82 Stop 7. Mogiłki Quarry Leader: Stanisław Skompski ...... 84 Upper Devonian succession typical of Kostomłoty facies: transition from deep basin to slope allochthonous deposits, redeposited from the central carbonate platform of Kielce Region. Stanisław Skompski ...... 84 Stop 8. Zachełmie Quarry near Zagnańsk Leader: Stanisław Skompski ...... 86 Epi-Variscan unconformity in the Holy Cross Mountains: Devonian dolomites of the Wojciechowice and Kowala formations, unconformably covered by Buntsandstein deposits; tidal sedimentation with record of emersion episodes Stanisław Skompski ...... 86 Stop 9. Tumlin Quarry Leader: Ewa Głowniak ...... 90 Eolian sediments in the Lower Triassic succession of the Mesozoic margin of the Holy Cross Mountains Stanisław Skompski ...... 90

8 PRE-SYMPOSIUM FIELD TRIP – TOP GEOSITES OF THE KRAKÓW REGION

Convener: Jan Urban Institute of Nature Conservation Polish Academy of Sciences, Kraków, e-mail: [email protected]

Leaders: Maciej Bąbel Faculty of Geology, University of Warsaw, Żwirki i Wigury 93, 02-089 Warsaw, Poland; e-mail: [email protected] Anna Chwalik-Borowiec The Complex of Świętokrzyskie and the Nida River Landscape Parks in Kielce, ul. Łódzka 244, 25-655 Kielce, Poland; e-mail: [email protected] Michał Flasza Kopalnia Soli Bochnia (Bochnia Salt Mine) Sp. z o.o., Campi 15, 32-700 Bochnia, Poland; e-mail:[email protected] Michał Gradziński Institute of Geological Sciences, Jagiellonian University, Gronostajowa 3a, 30-387 Kraków, Poland; e-mail: Michal.gradziń[email protected] Józef Partyka Ojcowski Park Narodowy, Ojców 9, 32-045 Sułoszowa, Poland; e-mail: [email protected] Jan Urban Institute of Nature Conservation Polish Academy of Sciences, Kraków, e-mail: [email protected] Piotr Ziółkowski Faculty of Geology, University of Warsaw, Żwirki i Wigury 93, 02-089 Warsaw, Poland; e-mail: [email protected]

9 9th ProGEO Symposium, Chęciny, Poland, 2018

Itinerary of the Pre-symposium Field Trip

Saturday, 23th June 2018 14:00‒22:00 Registration 17:00‒20:00 Dinner Sunday, 24th June 2018 7:00‒7:45 Breakfast 8:00 Departure for the Bochnia Salt Mine (1 h, 50 km) 9:00 Stop 1.1. Bochnia Salt Mine (4 h, 50 min) 9:00 Go down to the mine for the guided underground tour (1.5 h) 11:30 Lecture in the Ważyn Chamber (1 h) 12:30 Lunch in the underground (1 h) 13:30 Go up from the mine 13:50 Departure for Kraków ‒ Krakus Mound (1 h, 55 km) 14:50 Stop 1.2. Krakus Mound (40 min) 15:30 Walk to the Bonarka Natural Reserve (30 min, 1 km) 16:00 Stop 1.3. Bonarka Nature Reserve (30 min) 16:30 Departure for Kraków ‒ Wawel Hill (30 min, 10 km) 17:00 Stop 1.4. Wawel Hill and Royal Castle (30 min) 17:30 Stop 1.5. Wawel Hill and Smocza Jama (Dragon’s Den) Cave (30 min) 18:00 End of the Field Trip and walk to the Żaczek Hotel (30 min, 1 km) 19:00‒20:00 Dinner in the Żaczek Hotel 20:00 Departure for the optional English speaking guided tour in Kraków (1.5 h) ~21:30 Return to the Żaczek Hotel Monday, 25th June 2018 7:00‒7:45 Breakfast 8:00 Departure for the Ojców National Park (50 min, 25 km) 8:50 Walk to the Kraków Gate rock in the Prądnik Valley (30 min, 1 km). 9:20 Stop 2.1. The Kraków Gate rock (30 min) 9:50 Walk to Ciemna Cave (10 min, 0.2 km) 10:00 Stop 2.2. Ciemna Cave (50 min) (optionally: Ojców National Park Museum) 10:50 Walk to the Władysław Szafer Natural History Museum (50 min, 2 km) 11:40 Stop 2.3. Władysław Szafer Natural History Museum (20 min) 12:00 Departure for the Maczuga Herkulesa crag and Pieskowa Skała Castle (30 min, 10 km) 12:30 Stop 2.4. The Maczuga Herkulesa (Hercules’ Club) crag and Pieskowa Skała Castle (30 min) 13:00 Lunch in the Pieskowa Skała Castle restaurant (50 min) 13:50 Departure for Ponidzie Region (2 h, 100 km) 15:50 Stop 2.5. Chotel Czerwony (30 min) 16:20 Departure for Skorocice (10 min, 8 km) 16:30 Stop 2.6. Skorocice and Skorocicka Valley (40 min) 17:10 Departure for Siesławice (10 min, 5 km) 17:20 Stop 2.7. Siesławice (30 min) 17:50 Departure for Chęciny (1 h 20 min, 60 km) 19:30–23:00 Conference registration and Dinner in the symposium venue ‒ The European Centre for Geological Education in Chęciny

10 GEOLOGICAL FRAMEWORK OF THE KRAKÓW REGION Jan Urban

The pre-symposium field trip takes place in very sediments and called the Carpathian Foredeep. specific – in geological terms – area, situated And, consequently, the margin of the Carpathian within the boundary zone of several geological overthrust (boundary of the Outer Carpathians) units of different age and nature (Fig. 1). The area is situated close to this city, a few kilometres far situated to the north of Kraków belongs generally from its southern suburbs (Fig. 1). Moreover, the to the West and Central European Phanerozoic Varis can Platform, which obviously forms a sub- (Variscan) Platform (Jarosiński et al. 2009) built stratum of the Fore-Carpathian depression and of Palaeozoic rocks deformed during the Cale- the Outer Carpathians (in the zone accessible for donian and Variscan orogeneses, which are cov- human detection), is divided into two blocks of ered by Mesozoic sediments only slightly mod- much deeper and older (at least Caledonian) foun- ified during the Alpine tectonic movements. dation and different geological history: western However, the city of Kraków itself, is located Upper Silesian Block (a part of Brunovistulicum) in the area of much more intensive Alpine tec- and eastern Małopolska Block, which are sep- tonic impact, namely within the Carpathian fore- arated with the principal, transcontinental tec- land depression filled with the Neogene marine tonic boundary called Hamburg-Kraków Tecto-

Fig. 1. Sites visited during the pre-symposium field trip against the simplified geological map of this area (geolog- ical background after Rühle et al. 1977, modified). Symbol explanations: 1-7 – geological units (1 – Palaeozoic, 2 – Triassic, 3 – Upper Jurassic, 4 – Lower Cretaceous, 5 – Upper Cretaceous, 6 – Cretaceous and Palaeogene of the Carpathian flysch, 7 – Neogene); 8 – main faults; 9 – northern margin of folded Neogene; 10 – Carpathian overthrust; 11 – sites visited and a route of field trip.

11 9th ProGEO Symposium, Chęciny, Poland, 2018 nic Zone (Buła et al. 2008; Jarosiński et al. 2009). elements of relief and landscape in some parts of This is probably the reason that the Kraków area the Silesian‒Kraków Homocline, namely in the is just located within the narrowest segment of Kraków‒Częstochowa Upland (also called ‛Polish the Fore-Carpathian depression, i.e. the Carpa- Jura Chain’). A spectacular, picturesque landscape thian Foredeep. of rocky relief has been a first and evident reason The Palaeozoic basement of the European of practical and legal protection of many areas Phanerozoic Platform (Devonian and Carboni- and sites in this region (Matyszkiewicz 2008). As ferous) is outcropped several ten kilometres west a consequence, in the proximity of Kraków, there of Kraków (Fig. 1) and these outcrops will not be are some 200 rock forms protected as nature mon- visited during the field trip. Rocks of its Mesozoic uments, about 10 landscape and geological nature cover form the direct or sub-Quaternary sub- reserves and the Ojców National Park famous for stratum north of Kraków and crop out as tec- its limestone crags, cliffs and karst caves, which tonic horsts within this city area. The Mesozoic will be visited during the second day of the field succession outcropped in the Kraków vicinity is trip (Stops 2.1–2.4). practically composed of the Upper Jurassic se- The Carpathian Foredeep, within which quence (with relatively very thin Middle Jurassic the city of Kraków is situated, is a part of the layer at the bottom) and the Upper Cretaceous Parathetys system of basins formed as a tectonic sequence of marine sediments. Upper Jurassic depressions in front of the advancing Carpathian sequence is built of limestone series several overthrust in the Early Miocene and then func- hundred meters thick generally gently dipping tioning as a marine basin up to the Late Miocene northeast, which forms extensive geological (Jarosiński et al. 2009). Consequently, this tec- unit called the Silesian-Kraków Homocline to tonic depression was filled with marine sedi- the north and northwest of Kraków. The natural ments, which currently are partly covered by the outcrops of these rocks will be visited during the overthrust Carpathian orogen and partly form a first day of the field trip in Kraków and in its sec- (sub-Quaternary) substratum of morphological ond day in the Ojców National Park. The Upper basin between the Carpathians (to the south) and Jurassic limestones were truncated during the south-central Polish uplands (to the north). Early Cretaceous terrestrial period and covered The Badenian–Sarmatian (Langhian–Serra- by carbonate, mainly marly Upper Cretaceous valian) depositional sequence of the sediments fill- depositional sequence which is also up to several ing the Carpathian Foredeep ranges in a thickness hundred meters thick. The Cretaceous sequence from several or several ten meters in the northern that forms the ground surface (or sub-Quater- marginal part of the unit up to some 2 000 m in nary substratum) north and northeast of Kraków its southern part and 3 500 m in south-eastern belongs to the southeastern segment of the Mid- part. The sequence is composed predominantly of Polish Synclinorium (a unit that crosses Polish monotonous fine siliciclastic and clay (silty-clay) territory from the southeast to the northwest, rocks with inserts of coarser clastics and evaporite parallel to the Trans-European Suture Zone) series, as well as carbonate (biodetrital) facies that which is called Miechów Synclinorium (Fig. 1) occur in the northern, coastal zone of the basin. (Karnkowski 2008; Matyszkiewicz 2008). Various thickness and differentiated facies devel- The territory built of Jurassic and Cretaceous opment of these sediments are due to the active carbonate rocks north of Kraków city comprises tectonic evolution of the basin during its existence upland area characterised by hilly relief or pla- and afterwards, which results in very complex teau dissected by deep stream valleys. A lith- fault (blocky) tectonics of the basin and its fills ified pre-Quaternary rocks are partly covered (Oszczypko et al. 2006; Jarosiński et al. 2009). by Quaternary sediments, predominantly by The Badenian evaporite series is a relatively thin Pleistocene loess layers that reach a thickness up to unit (reaching from several meters up to 200 m) 20–30 m. Upper Jurassic massive limestones form in the Miocene sequence of the Carpathian numerous monadnocks, crags and cliffs as well as Foredeep, however it is widespread within whole karst landforms and caves which are important basin and differentiated in lithology: from ha-

12 FIELD TRIP: Geological framework of the Kraków Region lite in the south-central part of the basin (near basement (Fig. 1) (Dżułyński 1953; Rutkowski Kraków), through anhydrite up to gypsum in its 1986; Gradziński 1993). Such geological structure northern marginal zone with occasional sulphur is a reason of very specific morphology of this bearing limestone deposits (Bąbel 2004; Garlicki area characterised by the occurrence of tectoni- 2008). Salt deposits of Bochnia and Wieliczka – cally driven hills surrounded by marshy plains, the towns situated southeast of Kraków – were which, as a consequence, affected a human set- extracted since the 13th century up to the end of tlement and history in this area (Alexandrowicz 20th century and both mines are currently accessi- et al. 2009). This problem will be a matter of ble for public as historical and natural monuments discussion during the first day of the field trip inscribed into the World Heritage UNESCO List (Stops 1.2–1.4). as ‛Wieliczka and Bochnia Royal Salt Mines’. The The third principal geological unit that oc- Bochnia Salt Mine will be visited in the first day curs near Kraków, the Carpathians, comprises a of this field trip (Stop. 1.1). large Alpine orogen whose northern part, called The morphological basin constituted by the the Outer Carpathians, is built of flysch rocks tectonic depression of the Carpathian Foredeep (sandstones, siltstones and claystones) mainly displays diversified relief in its different parts. of the Cretaceous–Palaeogene age (Fig. 1). The The central part of this basin is a plain of the Outer Carpathians are composed of several tec- upper-middle section of the Wisła (Vistula) River tonic-lithological units (nappes) overthrust each Valley, in which the Miocene rocks are overlain other towards the north. In morphological terms by Quaternary fluvial sediments: clays, muds they represent low and predominantly interme- (silts) and sands as well as in some places aeolian diate mountains surrounded from the north with sediments: sands and silts. Both its marginal seg- foothills (Malata 2008; Oszczypko et. al. 2008). ments, southern and northern, are characterised Our field trip does not reach this region, but most by hilly relief usually of structural nature, i.e. probably we will see this mountain range from controlled by lithology and tectonic structures, several sites in Kraków, e.g. from the Krakus however in some places apparently affected by Mound (Stop. 1. 2). the neo-tectonic movements. In the northern mar- References ginal zone of the basin, which is called Ponidzie or Nida Basin in geographic terms, Miocene gyp- Alexandrowicz, Z., Urban, J., Miśkiewicz, K. 2009. sum and biodetritic limestones are the most im- Geological values of selected Polish properties of the UNESCO World Heritage List. Geoheritage, portant morpho-structural units responsible for 1, 43–52. local relief. The sequence and sedimentary struc- Bąbel, M. 2004. Badenian evaporite basin of the north- tures (i.e. depositional environment) of gypsum ern Carpathian Foredeep as a drawndown salina ba- as well as gypsum karst and morphology will be sin. Acta Geologica Polonica, 54, 3, 313–338. a matter of consideration in the second day of this Buła, Z., Żaba, J., Habryn, R. 2008. Tectonic subdi- field trip (Stops 2.5–2.7) vision of Poland: southern Poland (Upper Silesian The narrowest segment of the Carpathian Block and Małopolska Block). Przegląd Geolo- Foredeep, where the city of Kraków is located giczny, 56 (10), 912–920. (In Polish with English (Fig. 1), is one of the most interesting parts of the summary). southern Poland. In this part of the Carpathian Dżułyński, S. 1953. Tektonika południowej części Foredeep its substratum is crossed by the trans- Wyżyny Krakowskiej (Tectonics of the southern continental Hamburg-Kraków Tectonic Zone part of the Cracovian Upland). Acta Geologica Polonica, 3 (3), 325–440. (In Polish). (that runs WNW-ESE) and adjoined secondary Garlicki, A. 2008. Salt mines at Bochnia and Wieli- structure of the Rzeszotary Horst (NNW-SSE) czka. Przegląd Geologiczny, 56 (8/1), 665–669. (Buła et al. 2008). The Carpathian Foredeep is Gradziński, R. 1993. Geological Map of Kraków Re- very narrow here (10–15 km wide), and densely gion without Quaternary and terrestrial Tertiary divided by faults into numerous tectonic blocks deposits, scale 1:10.000. Geological Museum, In- among which are horsts built of the Jurassic and stitute of Geological Sciences of Polish Academy Cretaceous rocks of the Carpathian Foredeep of Sciences; Kraków.

13 9th ProGEO Symposium, Chęciny, Poland, 2018

Jarosiński, M., Poprawa, P., Ziegler, P.A. 2009. Ce- namic evolution. In: J. Golonka, F.J. Picha (Eds), nozoic dynamic evolution of the Polish Platform. The Carpathians and their foreland: Geology and Geological Quaterly, 53, 1, 3–26. hydrocarbon resources. American Association of Karnkowski, P.H. 2008. Tectonic subdivision of Po- Petroleum Geologists Memoir, 84, 293–350. land: Polish Lowlands. Przegląd Geologiczny, 56 Oszczypko, N., Ślączka, A., Żytko, K. 2008. Tectonic (10), 895–903. (In Polish with English abstract). subdivision of Poland: Polish Outer Carpathians Malata, T. 2008. Development of Polish Flysch Car- and their foredeep. Przegląd Geologiczny, 56 (10), pathians revealed in outcrops and landscape. Prze- 927–935. (In Polish with English abstract). gląd Geologiczny, 56 (8/1), 688–691. Rühle, E., Ciuk, E., Osika, R., Znosko, J. 1977. Geo- Matyszkiewicz, J. 2008. The Kraków-Częstochowa Up- logical map of Poland without Quarternary depos- land (Southern Poland) – the land of white cliffs and its, scale 1:500000. Wydawnictwa Geologiczne; caves. Przegląd Geologiczny, 56 (8/1), 647–652. Warszawa. (In Polish). Oszczypko, N., Krzywiec, P., Popadyuk, I., Peryt, T. Rutkowski, J. 1986. On Tertiary fault tectonics in the 2006. Carpathian Foredeep basin (Poland and vicinities of Kraków. Przegląd Geologiczny, 36 Ukraine): its sedimentary, structural and geody- (10), 587–590. (In Polish with English abstract).

BOCHNIA AREA

Stop 1.1. Bochnia Salt Mine Leaders: Michał Flasza and The Bochnia Salt Mine Guides

Keywords: salt deposit, Miocene, Carpathian Foredeep, protection, salt mine, UNESCO World Cultural And Natural Heritage List GPS coordinates: 49°58’8,7” N; 20°25’2,8” E Location: Bochnia Salt Mine is located in the south of Poland, about 45 km to the east of Kraków.

Geological history of the Bochnia Salt Mine Michał Flasza Lithostratigraphy and tectonics: In the limited connection with the ocean and inflow of Miocene Epoch the Carpathian Foredeep in the fresh, river water. At a later stage, during the so- territory of southern Poland was occupied by called Badenian salinity crisis, salt precipitation a sea, which was a part of a larger marine ba- occurred on a large scale (Poborski, Skoczylas- sin, the Paratethys. Under favourable conditions Ciszewska 1963; Bąbel 2004; Wiewiórka et al. about 13.8 million years ago evaporites started 2007, 2009; Garlicki 2008). to deposit in the sea, including deposition of ha- The Bochnia salt deposits, situated in the lite, which constitutes the Badenian salt-bearing southern part of the Carpathian Foredeep, over- formation called also the Wieliczka Beds. The lie (in the Miocene depositional succession) precipitation of salt started due to the climate marly shales, sandstones and conglomerates cooling during which ocean waters were trapped (with Car pa thian flysch material) of the Skawina in the polar zones, which resulted in lowering of Beds (Fig. 2). The salt-bearing formation is, in the ocean level by ca. 50 m. The effect of this turn, overlain by the Chodenice Beds composed was the reduction of connections between the of sandy-marly shales with dolostone interca- ocean and the Paratethys Basin. As a result of lations. Above the Chodenice Beds clayey and intensive evaporation of sea water, the brine was sandy layers of the Grabowiec Beds (Badenian– not diluted by less mineralised water, due to the Sarmatian) occur. The deposition of salt forma-

14 FIELD TRIP: Geological framework of the Kraków Region tion occurred in conditions of relatively high deposits (Poborski 1952; Poborski, Skoczylas- tectonic stress caused by the movements of the Ciszewska 1963; Wiewiórka et al. 2007, 2009, Carpathian orogenic belt. Frequent earthquakes 2016; Garlicki 2008; Fig. 2). caused submarine debry flows and the thrusts of sediments each over others. Such salt forma- Volcanic activity: The intensive volcanic ac- tions have a particular structure: they consist tivity during the Miocene is testified to by the of large olistolites embedded in poorly sorted tuffite layers encountered in the Badenian sed-

Fig. 2. Geological cross-section through the Miocene salt-bearing formation (13.6 million years ‒ radiometric dating of Badenian pyroclastic sediments) at the Campi shaft and its vicinity (C1–C10 exploitation levels) (after Poborski 1952).

15 9th ProGEO Symposium, Chęciny, Poland, 2018 iments of the Bochnia deposit. Interestingly, in in villages of Łapczyca, Moszczenica, Siedlec and the tuffite layer underlying the salt formation Łężkowice. The Skawina Beds frame the Bochnia and signed WT1, the material originated from deposit from the south. In a lithostratigraphic se- the andesites of the Pieniny Mountains (Inner quence above the Skawina Beds the Badenian salt Carpathians) was found. In the Bochnia deposit bearing formation was deposited in a form of al- also other, thin WT2 and WT3 tuffite, layers ternating layers of claystones, siltstones and clay- were found. Several meter-thick tuffite package stone-anhydrite-halite interbeddings with a total is also found in series overlying the salt-bearing thickness of ca. 70 m. Above the salt formation, formation (Dudek et al. 2004). the Chodenice Beds of a thickness up to 300 m Tectonics of salt-bearing formation: During the and the upper Grabowiec Beds occur. orogenic phase in the Carpathians that occurred Quaternary sediments cover: Folded Miocene shortly after the deposition of rock salt, Carpathian sediments and Carpathian flysch are truncated flysch rocks shifted northward and thrust over the and covered by Quaternary sediments, which salt-bearing formation. Under the pressure of the consists of glacial and fluvioglacial formations Carpathian orogen, Badenian rocks situated close of the Pleistocene South-Polish glaciations and to the orogenic front, including the salt-bear- eolian loess and loess-like silts and sands as well ing formation, were folded, moved northward, as Pleistocene and Holocene fluvial sediments. thrust over undisturbed sediments and uplifted. Quaternary formations hide and level an uneven Consequently, due to so-called tectonic enrich- relief of older rocks. Among the Quaternary ment, the salt layers of original uniform thickness, sediments are silt-sand formations called quick- underwent local accumulation forming rich salt sands, which, watered, undergo semi-liquid de- deposits. As a result of such processes, two prin- formations and, therefore, have posed a techni- cipal folds composed of flysch rocks in axial parts cal problem in the construction and maintenance and Badenian salt-bearing formation in limbs de- of shafts since the beginning of salt mining veloped in the Bochnia area. The main fold, in the (Poborski 1952; Poborski, Skoczylas-Ciszewska northern limb of which the Bochnia deposits are 1963; Wiewiórka et al. 2007, 2009; Garlicki located, is named the Bochnia Anticline. To the 2008; Wiewiórka et al. 2016; Flasza 2016). south of this structure a second fold, called the Uzbornia Anticline, is located. Within Uzbornia Highlights of Bochnia Salt Mine: Apart from Hill, sulphate rocks of the evaporite formation, the depositional and tectonic structures of the including alabaster and fibrous gypsum, are out- original sediments in the Bochnia Salt Mine gal- cropped. The tectonically uplifted Bochnia salt leries several very interesting secondary phenom- deposit underwent destructive corrosion pro- ena have been observed. One of them are halite cesses before the Pleistocene South-Polish gla- stalactites oblique to the horizontal (roof) or ver- ciations. The destruction of salt layers was also tical (wall) surfaces that grow against the air flow slowed down when the salt-bearing formation owing to the aggradation of micro-crystals from was covered by loess cover formed during the the sodium chloride aerosol in the air. The other Pleistocene (Wiewiórka et al. 2016). very specific forms of salt crystallization are fi- Dimensions and thickness of salt deposits: The brous halite crystals called ‘Hairs of Saint Kinga’ Bochnia salt deposit extends over a length of 3.6 (the Princess who was a legendary founder of the kilometres from west to east and is limited by the Mine). The aggregates of large cubic halite crys- northern limb of the Bochnia Anticline. It is rela- tals growing in brine pools due to the slow pre- tively narrow, reaching a maximum width of 200 cipitation and crystallization of sodium chloride m. The maximum depth of the deposit, at the 16th are the most typical secondary salt forms. In turn, level of the mine, is 468 m, however, drilling con- the uniqueness of the Bochnia Salt Mine is proved firmed a deposit depth of over 520 m. Folded salt by a mirabilite (hydrous sodium sulphate), a very layer stretch eastward to the village of Łazy, and rare mineral that occurs (as a natural formation) to the west are extended by the available deposits only in a few places in the world. In the Bochnia

16 FIELD TRIP: Geological framework of the Kraków Region

Salt Mine it forms incrustations and flower-like into the register of historic monuments. The low- formations (Wiewiórka et al. 2016). ermost levels of the mine (from the 10th to the 16th Unique environment of the Bochnia Salt one, situated below a depth of 289 m) have been Mine is also a reason of the occurrence of flu- successively backfilled with sand and/or barren orescent secondary halite crystals. In 2014 in rocks. On 26th September 2000, the President of partly filled with brine and not accessible for the Republic of Poland signed a decree officially public mine gallery the cubic halite crystals were recognizing ‘the Bochnia Salt Mine as a mon- found which emit orange or pink-red light when ument of historical heritage’. Legal protection were radiated with UV rays. Such phenomenon encompasses ca. 60 km of mining galleries and is extremely rare. In the Bochnia Salt Mine it was chambers situated on nine exploitation levels, at observed only at two sites. The study performed depths from 70 m to 289 m. The protected area by Professor M. Manecki and his collaborators stretches 3.5 km along the WE axis, with a max- (University of Science and Technology AGH in imum width (NS) of 250 m, which is exactly a Kraków) indicated that this phenomenon in the width of the deposit. Since 5th December 2005, Bochnia Salt Mine is caused by the occurrence 27 documentation sites that document the geol- of small admixture of manganese and lead in the ogy of the Bochnia salt deposit have been under crystal structure (Waluś et al. 2016). legal protection (Wiewiórka et al. 2009). On 23th June 2013 the centuries-old mine in Bochnia Mining history: Archaeological artefacts indi- entered the World Heritage UNESCO List, cate the extraction of brine springs and salt pro- named together with the Wieliczka Salt Mine duction in the vicinities of Bochnia has existed as ‘Wieliczka and Bochnia Royal Salt Mines’. since the Middle Neolithic Period. As surface Currently, the key issue consists in protecting brine sources became exhausted, in the Middle and preserving for future generations as much Ages brine wells were dug, which facilitated as possible of the Earth history pages written the discovery of rock salt. In Bochnia the mine in the dark chambers and galleries of the mine. was founded in 1248. The oldest shafts: Sutoris, Regis, Gazaris and Floris, reached a depths of References about 60 m. Greater depths (about 300 m) were Bąbel, M. 2004. Badenian evaporite basin of the north- reached by means of a complex system of in- ern Carpathian Foredeep as a drawndown salina clined galleries, small underground shaft and basin. Acta Geologica Polonica, 54 (3), 313–338. crosscuts. In the 16th century the Campi shaft Dudek, K., Bukowski, K., Wiewiórka, J. 2006. Radio- was dug in the western part of the deposit. In metric dating of Badenian pyroclastic sediments 18th century the digging of the first straight hori- from the Wieliczka-Bochnia area. In: Materiały 8. zontal gallery, called August and connecting the Ogólnopolskiej Sesji Naukowej ‘Datowanie Min- Campi shaft and the Floris shaft at a depth of erałów i Skał’, Kraków 18–19.11.2006, p. 19–26. 212 m, brought a kind of order in the mine devel- Instytut Nauk Geologicznych Polskiej Akademii Nauk w Krakowie; Kraków. (In Polish with En- opment. The 19th and 20th centuries were marked glish summary). up by the mechanisation of mining works, indus- Flasza, M. 2016. A description of the geological struc- trial exploitation from increasingly lower levels ture of the Bochnia salt deposit. In: J. Flasza, M. of the mine. Extraction continued in the mine Flasza, T. Migdas, S. Mróz, A. Puławska, K. Zięba until 1990. Since the early 1980’s, a change in the (Eds), History caved in salt. Bochnia, p. 33–53. mine functions and activity from industrial to Kopalnia Soli Bochnia; Bochnia. touristic, recreational and even medical one (as a Garlicki, A. 2008. Salt Mines at Bochnia and Wieli- spa) has been made. Nowadays, these functions czka. Przegląd Geologiczny, 56 (8/1), 663–669 . comprise the essence of mine operations which Poborski, J. 1952. The Bochnia Salt Deposit on the continue to grow (Wiewiórka et al. 2009). geological background of region. Biuletyn Państ- wowego Instytutu Geologicznego, 78, 1–160. (In Protection and conservation: As early as in Polish with English summary). 1981 the historic parts of the Bochnia Salt Mine, Poborski, J., Skoczylas-Ciszewska, K. 1963. Miocene i.e. the six oldest levels, were officially inscribed in the zone of the Carpathian overthrust in the area

17 9th ProGEO Symposium, Chęciny, Poland, 2018

of Wieliczka and Bochnia. Rocznik Polskiego To- i historii górnictwa w Kopalni Soli Bochnia. Gos- warzystwa Geologicznego, 33 (3), 339–346. (In podarka Surowcami Mineralnymi, 23, 157–161. Polish with English sumary). Wiewiórka, J., Dudek, K., Charkot, J., Gonera, M. Waluś, E., Głąbińska, D., Puławska, A., Flasza, M., 2009. Natural and historic heritage of the Boch- Manecki, M. 2016. Fluorescent halite from Boch- nia salt mine (South Poland). Studia Universitatis nia salt mine, Poland, European Geosciences Babeş-Bolyai, Geologia, 54 (1), 43–47. Union General Assembly 2016, 18, Geophysical Research Abstracts, p. 8505. http://adsabs.har- Wiewiórka, J., Poborska-Młynarska, K., Zięba, K., vard.edu/abs/2016EGUGA.18.8505W Flasza, M. 2016. W głąb soli i czasu, w Kopalni Wiewiórka, J., Charkot, J., Dudek, K., Gonera, M. Soli Bochnia, pp. 1– 64. Wydawnictwo Akademii 2007. Nowe dane do budowy geologicznej złoża Górniczo-Hutniczej; Kraków.

KRAKÓW CITY

Stop 1.2. Krakus Mound Leader: Jan Urban

Keywords: structural morphology, geological constraints of human history, Carpathian Foredeep, Kraków Old City GPS coordinates: 50°02’17.1” N; 19°57’30.2” E Location: 3 km south of the the Kraków City Centre, in the Krzemionki Podgórskie Hills (Podgórze quarter, Lasota Hill, Bonarka Horst).

Lithostratigraphy and tectonics as a factor controlling geomorphology of the Kraków area Jan Urban Introduction: Krakus Mound is an artificial pre- plateau slope of the Silesian‒Kraków Homocline historic mound, which is considered to be a grave (Kraków‒Częstochowa Upland), to the north- of the legendary King Krakus (Krak) a founder north-east – plateau slope of the Miechów Syn- of Kraków. Krakus Mound is one of the best view cli norium (Małopolska Upland). Between these point on a landscape of the Kraków area, where regions distinctly deepened area of the Kraków morphological consequences of tectonic struc- city within the Carpathian Foredeep is located, ture and lithology can be shown. however, this area is spotted with numerous hills. Lithostratigraphy and tectonics: From Krakus This area is generally situated within the Mound almost whole area of Kraków urban ag- uplifted and marginal part of Precambrian and glomeration can be observed. The city is situ- Palaeozoic units, the Hamburg-Kraków Tectonic ated within the narrowest part of the Carpathian Zone and the Rzeszotary Horst, therefore the trun- Foredeep, which is 10–15 km wide here, there- cated surface of the Variscan succession, mainly fore the neighbouring geological units (and ade- Devonian rocks, occur as shallow as ca. 300 m be- quate geographical regions, cf. Kondracki 2000) low ground surface in some places. The Variscan are well visible from the mound: to the south unit is overlain by the Alpine succession which is – hills and mountains of the Outer Carpathians generally composed of three principal lithostrati- (Carpathian Foothills and Beskidy Mountains graphic complexes: the Upper Jurassic limestone in geographical terms), to the north-northwest – complex, the Upper Cretaceous marl complex and

18 FIELD TRIP: Geological framework of the Kraków Region

Fig. 3. Geological cross-section of the area between the Kraków Old City and Krzemionki Podgórskie Hills, i.e. just between our viewpoint and the city centre visible from this point (after Rutkowski 1994a, simplified). Symbol explanations: 1 – Upper Jurassic, 2 – Cretaceous, 3 – Neogene–Miocene, 4 – Quaternary, 5 – faults. the Middle Neogene siliciclastic clay complex, they were eroded during the Palaeogene and which were covered by sheets of Quaternary sed- younger Neogene–Quaternary time (Rutkowski iments (Fig. 3). The Upper Jurassic and Upper 1986, 1994a, b, c; Pilecka, Szczepańska 2004; Cretaceous complexes represent the older Alpine Gradziński M., Gradziński R. 2013). units that were weakly modified (inclined to the The Middle Neogene, strictly Middle Mio- north-east or south-east) due to the Laramide tec- cene, sequence is usually up to 200 m thick in tonic movements, whereas the Middle Neogene the Kraków area and formed predominantly of complex is a typical element of the Carpathian siliciclastic-clayey rocks, which are occasion- Foredeep tectonically shaped only during the ally underlain with thin sheets (lobes) of coquina younger Alpine, Neogene movements. Upper (Ostrea) limestones (of earlier Miocene marine Jurassic, mainly Oxfordian complex is ca. 200 m ingression) and terrestrial (also karst) sediments: thick and composed of three limestone lithotypes caliche, clays, sands. Within this sequence the fol- (facies): (1) Massive buildups (bioherms) that form lowing lihostratigraphic units are distinguished more or less isolated bodies within the bedded (from the bottom): Skawina Beds, Wieliczka Beds, rocks; (2) Thick-bedded limestones (biostromes) Chodenice Beds and Bogucice Sands (these last bearing numerous cherts and (3) Thin-bedded, occur only in the southern part of the area). The ‘platy’, occasionally marly or chalky, limestones. Wieliczka Beds are characterised be the occur- This series is underlain by a thin, ranging several rence of evaporate series, which is formed of gyp- meters layer of Callovian sandstones and sandy sum and anhydrite in the Kraków area and grades limestones (Rutkowski 1986, 1994a; Pilecka, toward south-southeast to halite of the Wieliczka Szczepa ńska 2004; Matyszkiewicz et al. 2006, salt deposit (Rutkowski 1986, 1994a; Michalik Matyszkiewicz 2008; Gradziński M., Gradziń- et al. 1989; Felisiak 1992; Pilecka, Szczepańska ski R. 2013). The thick-bedded limestones grad- 2004; Gradziński M., Gradziński R. 2013). ing to massive ones are very well visible in the Neogene series, together with the older se- abandoned Liban Quarry situated just next to the quence sections were significantly modified by Lasota Hill and Krakus Mound. We can also ob- the Neogene disjunctive tectonic movements: serve the Palaeogene–Neogene karst palaeo-do- they were dissected into the tectonic blocks – lines filled with sediments in this quarry faces horsts and grabens – by numerous dip-sleep (Gradziński R. 1962, 1972) . faults (Fig. 4) (Dżułyński 1953; Rutkowski 1986, The Upper Cretaceous complex mainly con- 1994a, b; Pilecka, Szczepańska 2004; Gradziński sists of Santonian–Maastrichtian marls, sandy M., Gradziński R. 2013). marls and siliceous marls bearing cherts. Upper Cretaceous rocks occur principally in the Mie- Structural geomorphology: This Cenozoic tec- chów Synclinorium, northeast of Kraków, where tonics, together with the lithological differences they reach a thickness ranging up to several of the complexes described above, is strictly hundred meters, while within the Kraków area responsible for the specific morphology of the

19 9th ProGEO Symposium, Chęciny, Poland, 2018

Fig. 4. Geological map of Kraków area (after Gradziński R. 1993, simplified). Symbol explanation: 1 – Upper Jurassic, 2 – Upper Cretaceous, 3 – Cretaceous and Palaeogene of the Carpathian flysch, 4 – Neogene, 5 – faults; 6 – Carpathian overthrust; 7 – sites visited and a route of field trip; 8 – historical centre of Kraków, route; 9 – cross-section shown on Fig. 3. Kraków area. The Kraków area is characterised with the Neogene depositional complex, which, by the occurrence of numerous hills (groups and in turn, is covered by the Quaternary, fluvial ranges of hills) that stand up to 150 m above and fluvioglacial sediments: gravels and sands the lowland of the Wisła (Vistula) River Valley, overlain by clays and silts. Within these low- which are horsts built of Jurassic limestones (in ered areas two principal fluvial levels are dis- some places covered with ‘caps’ of Cretaceous tinguished: (1) Holocene floodplain, originally rocks) framed with normal, (sub)vertical faults marshy and covered by overbank muds as well as or, more frequently, bundles/clusters of faults. numerous palaeo-channels (cut-off channels, ox- The hilltops (ridges, plateaus) can be identified bow lakes) of the Vistula River and its tributaries with the remnants of the Palaeogene denuda- and (2) The upper, Vistulian (Würm) terrace that tion palaeo-surface, while the hillslopes mark stands from several meters to more than 10 m the courses and locations of zones of step faults above the Vistula River channel (Rutkowski framing the horsts (Dżułyński 1953; Gradziński 1989; Kalicki 1991; Gradziński M., Gradziński M., Gradziński R. 2013; Izmaiłow 2013). The de- R. 2013; Izmaiłow 2013). struction of the Gothic Saint Catherina Church Nowadays, most of this area is occupied by the situated in the marginal zone of the Skałka Hill urban agglomeration and definitely changed by horst in Kraków Old City during the earthquakes human activity, however some hills (horsts) dis- in 1443 and 1786 (Guterch 2009) suggests that tinctly stand out in the Kraków area landscape. some of these faults are still active. Some of them are still not covered by buildings, The hills (horsts) are surrounded by the low- such as the Lasota Hill (Bonarka Horst), on a top ered areas of grabens, which started to form of which we are now, and forested Sowiniec-Las in the Early–Middle Miocene and were filled Wolski Hill Range very well visible to the north-

20 FIELD TRIP: Geological framework of the Kraków Region west, as well as closer Krzemionki Podgórskie ki Przestrzennej Uniwersytetu Jagiellońskiego; Hills being a city park in this part. Lower horst Kraków. of Wawel Hill is completely covered by buildings Kalicki, T. 1991. The evolution of the Vistula river of the Royal Castle, similarly to Skałka Hill, valley between Kraków and Niepołomice in Late with two Medieval churches, situated next to Vistulian and Holocene times. In: L. Starkel (Ed.), Evolution of the Vistula river valley during the last Wawel Hill and the Old City, which is the low- 15 000 years, 6, Geographical Studies Special Is- ermost horst in this group, mostly covered by sue, 6, 11–37. the Quaternary sediments of the upper, Vistulian Kondracki, J. 2000. Geografia regionalna Polski (2nd terrace (Rutkowski 1989). edition), pp. 1–440. Państwowe Wydawnictwo Geoheritage value: Looking at the landscape Naukowe; Warszawa. of the Kraków area from the Krakus Mound, we Matyszkiewicz, J. 2008. The Kraków-Częstochowa Upland (Southern Poland) – the land of white can simply appreciate the role of the morphology cliffs and caves. Przegląd Geologiczny, 56 (8/1), that is strictly controlled by the geological struc- 647–652. ture, in the urban landscape and human activity Matyszkiewicz, J., Krajewski, M., Żaba, J. 2006. Struc- in this area during several centuries of Kraków tural control on the distribution of Upper Jurassic agglomeration development. carbonate buildups in the Kraków-Wieluń Upland (south Poland). Neues Jahrbuch für Paläontologie References und Geologie, 3, 182–192. Dżułyński, S. 1953. Tektonika południowej części Michalik, M., Paszkowski, M., Szulc, J. 1989. Węgla- Wyżyny Krakowskiej. Acta Geologica Polonica, 3 nowe utwory pedopdogeniczne miocenu okolic (3), 325–440. (In Polish). Krakowa. In: J. Rutkowski (Ed.), Przewodnik LX Felisiak, I. 1992. Oligocene–Early Miocene karst Zjazdu Polskiego Towarzystwa Geologicznego, deposits and their importance for recognition of Kraków, 14–16.09.1989, p. 190–195. Wydawnic- the development of tectonics and relief in the Car- two Akademii Górniczo-Hutniczej w Krakowie; pathian foreland, Kraków region, southern Po- Kraków. land. Annales Societatis Geologorum Poloniae, Pilecka, E., Szczepańska, M. 2004. Geological struc- 62, 173–207. (In Polish with English summary). ture of Kraków – general characteristics. Technika Gradziński, M., Gradziński, R. 2013. Budowa geo- Poszukiwań Geologicznych, Geosynoptyka i Geo- logiczna. In: B. Degórska, M. Baścik, (Eds), Śro- termia, 56, 59–65. (In Polish with English abstract). dowisko geologiczne Krakowa, p. 13–20. Instytut Rutkowski, J. 1986. On Tertiary fault tectonics in the Geografii i Gospodarki Przestrzennej Uniwer- vicinities of Kraków. Przegląd Geologiczny, 36 sytetu Jagiellońskiego; Kraków. (10), 587–590. (In Polish with English abstract). Gradziński, R. 1962. Origin and development of sub- Rutkowski, J. 1989. Osady czwartorzędowe centrum terranean karst in the southern part of the Cracow Krakowa. In: J. Rutkowski (Ed.), Przewodnik LX Upland. Rocznik Polskiego Towarzystwa Geolo- Zjazdu Polskiego Towarzystwa Geologicznego, gicznego, 32 (4), 429–492. (In Polish with English Kraków 14–16.09.1989, p. 196–200. Wydawnic- summary). two Akademii Górniczo-Hutniczej w Krakowie; Gradziński, R. 1972. Przewodnik geologiczny po oko- Kraków. licach Krakowa, pp. 1–335. Wydawnictwa Geolo- Rutkowski, J. 1994a. Introduction to the geological giczne; Warszawa. structure of the Kraków Region. Tectonics. In: Z. Gradziński, R. 1993. Geological Map of Kraków Re- Kotański (Ed.), Excursion guidebook, 3rd Interna- gion without Quaternary and terrestrial Tertiary tional Meeting of Peri-Tethyan Epicratonic Ba- deposits, Scale 1:10.000. Geological Museum, In- sins, Kraków (Poland), 29 August – 3 September stitute of Geological Sciences of Polish Academy 1994, p. 1–10. Polish Geological Institute; War- of Sciences; Kraków. szawa. Guterch, B. 2009. Seismicity in Poland in the light of Rutkowski, J. 1994b. Excursion 1. Geology of historical records. Przegląd Geologiczny, 57 (6), Kraków Region. Tectonics. In: Kotański Z. (Ed.), 513–520. (In Polish with English abstract). Excursion guidebook. 3rd International Meeting Izmaiłow, B. 2013. Rzeźba terenu. In: B. Degórska, of Peri-Tethyan Epicratonic Basins, Kraków (Po- M. Baścik (Eds), Środowisko geologiczne Kra- land), 29 August – 3 September 1994, p. 10–11. kowa, p. 22–31. Instytut Geografii i Gospodar- Polish Geological Institute; Warszawa.

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Rutkowski, J. 1994c. Excursion 2, Cretaceous of the Tethyan Epicratonic Basins, Kraków (Poland), Kraków Region. In: Kotański Z. (Ed.), Excursion 29 August – 3 September 1994, p. 12–19. Polish guidebook. 3rd International Meeting of Peri- Geological Institute; Warszawa.

Stop 1.3. Bonarka Nature Reserve Leader: Jan Urban

Keywords: tectonics, geological history, Jurassic, Cretaceous, sedimentology, palaeogeography, ichnofauna, geoheritage protection GPS coordinates: 50°01’45.2” N; 19°57’33.1” E Location: Southern part of Kraków, Krzemionki Podgórskie Hills, Bonarka Horst.

Mesozoic history of the Kraków area Jan Urban Introduction: The Bonarka Nature Reserve the Cretaceous marls during the Early–Middle protects the abandoned quarry in which Upper Miocene, which was overlain by Middle Miocene Cretaceous marls were excavated for a concrete clay-siliciclastic rocks, however, this sequence is production in the first half of 20th century. The also not outcropped, now (Gradziński R. 1961, quarry was a site of many geological studies, in 1972, 1978; Rutkowski 1994; Słomka 2012). particular, tectonic, paleontological and miner- The abrasion platform of the Jurassic lime- alogical investigations since the beginning of the stone gently dips by the angle up to 12° to the 20th century. The nature reserve was established south and is cut by three small dip-slip normal in 1961 due to the high scientific and educational faults of a WNW-ESE direction (110–135°) and values of the geological outcrops in the quarry vertical displacement ranging 2–3 m. The fault (Gradziński R. 1961, 1978; Alexandrowicz 1967; surfaces are currently irregular, because they Rutkowski 1986; Alexandrowicz and Alexan- are associated with tectonic breccias, which are drowicz 1999; Słomka 2012). partly destroyed during the quarrying and sub- Lithostratigraphy and tectonics: A principal sequent weathering. Apart from this bundle of part of the quarry bottom is occupied by a flat, faults, diagonal hinge faults of smaller displace- truncated due to the erosion surface of thick-bed- ments (up to 0.5 m) can be observed. The faults ded Jurassic limestones – a palaeo-abrasion cutting Jurassic limestone gradually disappear platform. This surface, gently tilted, is cov- within the lower section of Upper Cretaceous ered by Upper Cretaceous, strictly Santonian– marls grading into flexures that diminish up- Campanian marls, which are outcropped in the ward (Gradziński R. 1961, 1972; Rutkowski eastern face of the quarry. Moreover, thin sheets 1994; Bromley et al. 2009; Słomka 2012). of Cenomanian conglomerate as well as Lower Upper Cretaceous marl sequence is currently Turonian conglomerate and limestone and Upper only partly outcropped in the quarry face due Turonian conglomeratic limestone separated by to the weathering-erosion process destroying unconformity surfaces (with angle discordances densely cracked and soft rocks and consequen- ranging several degrees) were visible in the past tial formation of scree in the slope foot. The low- in the marginal part of the quarry and its vicinity. ermost part of this sequence is represented by a The youngest depositional evidences of geologi- layer of grey-green glauconitic marls up to 0.5 cal history identified in the vicinity of the quarry m thick, which can be also found in thin crev- were remnants of the caliche zone developed in ices within underlying Jurassic limestones. Gray

22 FIELD TRIP: Geological framework of the Kraków Region marls 2–3 m thick that overly glauconitic marls, ing within the detrital sediment covering lime- grade up to the white marls bearing cherts, stone ground) is also considered. The exact time which are now outcropped and visible in the up- of these trace fossils and, consequently, abrasion per parts of the quarry face (Gradziński 1961, platform formation, has not been defined and 1972; Rutkowski 1994; Wieczorek, Olszewska two possible ages, Late Turonian and Santonian, 2001; Bromley et al. 2009). are taken into account (Bromley et al. 2009). Apart from these trace fossils, the echino- Specific geological phenomena: Apart from the derms, ammonites, belemnites, bivalves as well general features briefly described above, many as fish fossils were collected and studied at this other interesting phenomena were observed at site (Gradziński R. 1961). this site and discussed since the beginning of the The occurrence of silica concentrations of 20th century. A matter of such discussion was, very various oval and lenticular shapes (flints) as for example, the nature and age of the faults and well as siliceous (sub)vertical thin veins within widened crevices filled with Cretaceous rocks. Jurassic limestones is the other specific petro- According to one of the hypothesis the faults graphic feature of the Bonarka Nature Reserve. cutting Jurassic limestones are of Cenozoic, Such character of these concentration suggests most likely Neogene age and their disappearance that apart from diagenetic cherts, epigenetic sil- within Upper Cretaceous marls is caused by plas- ica concentrations occur in the rocks. Moreover, tic deformation of these soft and flexible rocks the occurrence of small aggregates of hatchet- (Gradziński R. 1961; Dżułyński 1995; Felisiak tine, a very rare mineral of hydrocarbon group, 1995), whereas other geologists argues the syn- which was identified within the marls of the depositional development of these faults and lowermost part of the Cretaceous sequence at also crevices in limestones (as neptunian dykes) the beginning of the 20th century, is considered during the Late Cretaceous (Santonian) period to be another evidence of advanced hydrother- (Wieczorek et al. 1995; Wieczorek, Olszewska mal process developed within the zone of the 2001). The Subhercynian tectonic movements in Upper Jurassic–Upper Cretaceous unconfor- the Kraków area are proved at least by irregu- mity (Gradziński R. 1961; Matyszkiewicz 1987; lar occurrence of sheets/lobes of Cenomanian, Rutkowski 1994). Lower Turonian and Upper Turonian sediments separated with angle unconformities. Geoheritage value and geoconservation: The The most impressive paleontological feature geological studies at the Bonarka site make of the site is agglomeration of very numerous possible to reconstruct significant events of the sponge borings that cover the abrasion platform Mesozoic and Cenozoic geological history of of the Upper Jurassic limestones (Rutkowski the Kraków area. Apart from general geological 1994). They are ovoid depressions 1–4 cm in features, several very specific and unique phe- diameter from which numerous usually straight nomena were documented here, such as tectonic canals (several centimetres long) radiate. New features, new species of ichnotaxa, hydrother- species of ichnotaxa (trace fossils), called mal silification and other mineralisation. Some Entobia cracoviensis, has been described from of them are still accessible and very illustrative here (Bromley et al. 2009). This ichnospecies is (described on panels), e.g. faults and tectonic attributed to the endolithic, living (partly) em- breccias, abrasion platform with sponge borings, bedded into the lithified rocks, sponge possibly cherts and other silica formations. However, of the genus Aka. This was a single chambered some valuable features, as outcrops of Turonian organism, supposedly half boring, which is sug- and Neogene sediments as well as the lowermost gested by the fact that all found specimens are part of the Santonian sequence were lost just af- lacking of roofs. Therefore, the hypothesis that ter the closing of quarrying. The legal protection the roof was removed by organism itself during of the Bonarka Nature Reserve has protected this its live seems to be most probable, however the site against the total destruction (Alexandrowicz psammobiontic character of this species (its liv- 1967), and works performed by the environmen-

23 9th ProGEO Symposium, Chęciny, Poland, 2018 tal protection administration have kept the site Gradziński, R. 1972. Przewodnik geologiczny po in proper state. However, the geotechnical works okolicach Krakowa, pp. 1–335. Wydawnictwa that will recover some former features should be Geologiczne; Warszawa. considered. Gradziński, R. 1978. Protection of geological object in the environs of Kraków. Prace Muzeum Ziemi, References 25, 101–117. (In Polish with English sumary). Alexandrowicz, Z. 1967. A plan for the management Rutkowski, J. 1994. Excursion 2, site 2-1. Bonarka: of the ‘Bonarka’ reserve of inanimate nature near Cretaceous deposits and tectonics in Bonarka. In: rd Kraków. Chrońmy Przyrodę Ojczystą, 23 (3), Kotański, Z. (Ed.), Excursion guidebook. 3 In- 52–56. ternational Meeting of Peri-Tethyan Epicratonic Alexandrowicz, S.W., Alexandrowicz, Z. 1999. Se- Basins, Kraków (Poland), 29 August – 3 Septem- ber 1994, p. 19‒21. Polish Geological Institute; lected geosites of the Kraków Upland. Polish Geo- Warszawa. logical Institute Special Papers, 2, 53–60. Słomka, T. 2012. The Bonarka. In: T. Słomka (Ed.), Bromley, R.G., Kędzierski, M., Kołodziej, B., Uch- The catalogue of geotourist sites in nature reserves man, A. 2009. Large chambered sponge borings and monuments, p. 233–236. AGH University of on a Late Cretaceous abrasion platform at Kraków, Science and Technology; Kraków. Poland. Cretaceous Research, 30, 149–160. Wieczorek, J., Dumont, T., Bouilin, J.-P., Olszewska, Dżułyński, S. 1995. Neptunian dykes of Bonarka – a B. 1995a. Neptunian dykes of Bonarka – a testimo- testimony of the Late Cretaceous tectonic move- ny of the Late Cretaceous tectonic movements in ments in the Kraków Upland – discussion. Prze- the Kraków Upland – reply. Przegląd Geologiczny, gląd Geologiczny, 43 (8), 689–690. (In Polish 43 (8), 690–692. (In Polish with English abstract). with English abstract). Wieczorek, J., Dumont, T., Bouilin, J.-P., Olszewska, Felisiak, I. 1995. Neptunian dykes of Bonarka – a B. 1995b. Neptunian dykes of Bonarka – a testi- testimony of the Late Cretaceous tectonic move- mony of the Late Cretaceous tectonic movements ments in the Kraków Upland – discussion. Prze- in the Kraków Upland – reply. Przegląd Geolog- gląd Geologiczny, 43 (10), p. 863. (In Polish with iczny, 43 (10), p. 872. (In Polish with English ab- English abstract). stract). Gradziński, R. 1961. The project of the reserve at Wieczorek, J., Olszewska, B. 2001. Cretaceous nep- Bonarka. Ochrona Przyrody, 27, 239–251. (In Pol- tunian dykes of the Kraków Upland. Geologica ish with English sumary). Saxonica, 46‒47, p. 139–147.

Stop 1.4. Wawel Hill and Royal Castle Leader: Jan Urban

Keywords: structural morphology, geological constraints of human history, Carpathian Foredeep, Kraków Old City GPS coordinates: 50°03’15.3” N; 19°56’08.4” E Location: Wawel is the Royal Castle Complex perched on the Wawel Hill, located at the southern part of the Kraków Old City, at the Wisła (Vistula) River bank.

Kraków Old City and Wawel Royal Castle as an illustration of geological constraints of human history Jan Urban Tectonics, lithostratigraphy and their geomor- Wawel Hill is a typical tectonic horst within phological consequences: In geological terms the narrowest part of the Carpathian Foredeep

24 FIELD TRIP: Geological framework of the Kraków Region

(Rutkowski 1986, 1994a), whose occurrence Square in Europe with the Renaissance ‘super- is probably related to the structures of a deep, market’, one of the oldest universities in Europe Palaeozoic and Precambrian substrate (Buła et al. founded in 1364 (Jagiellonian University), rem- 2008; Pilecka, Szczepańska 2004). This horst is nants of the historic Jewish city with several syn- built of the Upper Jurassic massive limestones and agogues, and others. The first and most principal surrounded by grabens filled with siliciclastic- centre of this administration and urban agglom- clayey Neogene and Quaternary sediments as eration since its beginning in the Early Middle well as – just from the northeast, i.e. from the Old Ages was obviously the Wawel Hill that is cur- City side – by less uplifted horst built of Upper rently occupied by the Renaissance Royal Castle. Jurassic limestone and Upper Cretaceous marls The preferable colonisation of the Wawel Hill and partly covered by Quaternary sediments was fully justified by the environmental con- (Figs. 3, 4) (Gradziński R. 1972; Rutkowski 1986, straints of this area which are, in turn, closely 1989, 1994 a, b). The lithological differences controlled by geological history and structure and, most of all, the results of the Neogene tec- of this area (as it was argued above). The first tonic movement are perfectly reflected in relief evident reason for the colonisation of the Wawel and landscape of this area: the highest horst of Hill was its shape (steep slopes) and location Wawel Hill distinctly (ca. 20 m) stands above amid the marshy plain dissected by water chan- the surrounding areas as hill with steep, locally nels and lakes, which provided natural defence rocky slopes and relatively flat summit. Some of the settlement. Concurrently, there was a per- small karst dolines formed on the top of the hill manent source of water and food, because water were found during the archaeological excavations and fish were in the river, whereas plants, e.g. (Sawicki 1955; Kowalski et al. 1970). cereals could be cultivated both on wet ground The lower horst of the Old City comprises (at marshy floodplain) and arid ground (on hill- much lower but still elevated middle terrace cov- top), so profitably harvested alternatively in wet ered with clayey-sandy Quaternary sediments, or dry years. Furthermore, this environment fa- whereas the area of grabens in Wawel Hill vi- cilitated the development of trading links and cinity represents flat and marshy floodplain dis- commercial relations, since the Vistula River sected by active or abandoned (cut off) chan- was navigable and river ports and ferry jetties nels, e.g. oxbow lakes, of the Vistula River and were situated along its bank (Alexandrowicz et its tributaries (Gradziński R. 1972; Rutkowski al. 2009; Urban 2017). The developed urban ag- 1989; Kalicki 1991). Such landscape have been glomeration was also easily supplied with con- definitely changed due to human activity that struction stone resources, which occur at the site have lasted for about ten centuries (formation of (Upper Jurassic limestones) and in its vicinity anthropogenic sediments, building construction, (Carpathian sandstones, Palaeozoic limestones geotechnical regulation of river channels and – ‛marbles’) (Rajchel 2005, 2008; Bromowicz, others), nevertheless still two hundred years ago Magiera 2015). Even the oldest settlements on the oxbow lakes and riverbeds separating parts the Wawel Hill, falling on the Palaeolithic Period of the Old City were situated next to the Wawel (Firlet 1996), met favourable conditions provided Hill (Alexandrowicz et al. 2009). by caves as dwelling places. These factors of natural character and evident geological foun- Geological constraints of human activeness dation significantly stimulated location and then and history: Kraków is one of the most important development of human settlement firstly at a tec- historic sites in Poland as a capital of Kingdom tonic horst of the high Wawel Hill and then on of Poland from the 11th through 16th century. It the lower but still elevated horst of the Old City has a long range of historical monuments such as (Alexandrowicz et al. 2009; Urban 2017). Medieval arrangement of the Old City that is sur- rounded by fragments of the Medieval ramparts, Geological foundation of human history and several tens of churches built in Romanesque, culture as a geoheritage: In the light of ar- Gothic and Baroque styles, the largest Central gumentation presented above, the Kraków Old

25 9th ProGEO Symposium, Chęciny, Poland, 2018

City and, in particular, the Royal Castle crown- Gradziński, R. 1972. Przewodnik geologiczny po oko- ing Wawel Hill are very evident examples of licach Krakowa, pp. 1–335. Wydawnictwa Geo- casual relationships between the geological logiczne; Warszawa. structure that controls the morphological and Kalicki, T. 1991. The evolution of the Vistula river environmental conditions and human history valley between Kraków and Niepołomice in Late and culture. Taking into account the definition Vistulian and Holocene times. In: L. Starkel (Ed.), Evolution of the Vistula River valley during the proposed by Dixon (1996) that the geoheritage last 15 000 years, 6, Geographical Studies Special comprises those components of natural geodi- Issue, 6, 11–37. versity of significant value to humans, includ- Kowalski, S., Kozłowski, J. K., Ginter, B. 1970. Le ing scientific research, education, aesthetics and gisement du Paléolitique moyen et supérieur à la inspiration, cultural development, and a sense colline du Wawel à Cracovie. Materiały Archeo- of place experienced by communities (similar logiczne, 11, 47–70. (In Polish with French sum- definitions were proposed and quoted by Brocx, mary). Semeniuk 2007) one can, consequently, define Pilecka, E., Szczepańska, M. 2004. Geological struc- Wawel Hill and Kraków Old City as elements of ture of Kraków – general characteristics. Tech- geoheritage, i.e. geosites, because they are very nika Poszukiwań Geologicznych, Geosynoptyka accurate elements illustrating that geology is a i Geotermia, 5-6, 59–65. (In Polish with English proper tool for the interpretation of important summary). Rajchel, J. 2005. Kamienny Kraków, pp. 1–235. Uczel- aspects of human history and culture, in other niane Wydawnictwa Naukowo-Dydaktyczne; Kra- words: the geological structure was a foundation ków. of human history (Alexandrowicz et al. 2009; Rajchel, J. 2008. The stony Cracow: geological valors Urban 2017). of its architecture. Przegląd Geologiczny, 56 (8/1), The Royal Castle and Kraków Old City 653–662. were entered into the UNESCO World Heritage Rutkowski, J. 1986. On Tertiary fault tectonics in the List in 1978 as cultural elements, however, vicinities of Kraków. Przegląd Geologiczny, 36 Alexandrowicz et al. (2009) postulated to ac- (10), 587–590. (In Polish with English abstract). commodate the geological values and geological Rutkowski, J. 1989. Osady czwartorzędowe centrum heritage to the evaluation process of these sites. Krakowa. In: J. Rutkowski (Ed.), Przewodnik LX Zjazdu Polskiego Towarzystwa Geologicznego, References Kraków, 14‒16.09.1989, p. 196–200. Wydawnic- Alexandrowicz, Z., Urban, J., Miśkiewicz, K. 2009. twa Akademii Górniczo-Hutniczej w Krakowie; Geological values of selected Polish properties of Kraków. the UNESCO World Heritage List. Geoheritage, 1 Rutkowski, J. 1994a. Introduction to the geological (1), 43–52. structure of the Kraków Region. Tectonics. In: Brocx, M., Semeniuk, V. 2007. Geoheritage and geo- Kotański, Z. (Ed.), Excursion guidebook. 3rd In- conservation – history, definition, scope and scale. ternational Meeting of Peri-Tethyan Epicratonic Journal of the Royal Society of Western Australia, Basins, Kraków (Poland), 29 August – 3 Septem- 90, 53–87. ber 1994, p. 1–10. Polish Geological Institute; Bromowicz, J., Magiera, J. 2015. Building stones used Warszawa. in early medieval edifices of Kraków; their origin Rutkowski, J. 1994b. Excursion 1. Geology of and geology of the area, pp. 1–171. Wydawnic- Kraków Region. Tectonics. In. Kotański Z. (Ed.), two Akademii Górniczo-Hutniczej w Krakowie; Excursion guidebook. 3rd International Meeting Kraków. (In Polish with English summary). of Peri-Tethyan Epicratonic Basins, Kraków (Po- Dixon, G. 1996. Geoconservation: an internation- land), 29 August – 3 September 1994, p. 10–11. al review and strategy for Tasmania, pp. 1–101. Polish Geological Institute; Warszawa. Miscellaneous Report, Parks and Wildlife Service; Sawicki, L. 1955. Le gisement Paléolitique inférieur Tasmania. de Wawel à Cracovie. Studia do Dziejów Wawelu, Firlet, E.M. 1996. The Dragons Den in Wawel Hill; 1, 1–70. (In Polish with French summary). history, legends, dragons, pp. 1–154. Universitas; Urban, J. 2017. Urban geoheritage; the Old City of Kraków. (In Polish with English summary). Kraków as a case. ProGEO News, 3, 2–3.

26 FIELD TRIP: Geological framework of the Kraków Region

Stop 1.5. Wawel Hill and Smocza Jama (Dragon’s Den) Cave Leaders: Michał Gradziński and Jan Urban

Keywords: karst, cave, geological constraints of culture, Kraków Old City GPS coordinates: 50°03’11.7” N; 19°56’01.2” E Location: Smocza Jama Cave is located within Wawel Hill, near its western slope.

Smocza Jama Cave ‒ its origin, scientific potential and cultural importance Michał Gradziński and Jan Urban Introduction: Smocza Jama (Dragon’s Den) and 25 m. They maximal height exceeds 10 m, Cave is a typical geological element of the Wawel however the original height is bigger because Hill of important scientific and potential educa- the rocky bottom is covered with clastic deposits tional value. around 1.5 m in thickness (Kleczkowski 1976). The chambers originated along joints and bed- Geomorphology, hydrology and genesis: The ding planes, which is especially visible in the origin of Smocza Jama Cave and the chemistry northernmost chamber, named Alth’s chamber. of cave waters have been discussed in detail by The chamber ceiling is extensively rugged. It Gradziński M. et al. (2009) and Motyka et al. is featured by rounded hierarchically arranged (2005), respectively. The description of this stop solution cavities. Several smaller forms occur is based on the above mentioned papers. within one big form. The biggest of them fall Smocza Jama is a 276 m long cave which into a definition of cupola. The smaller solution includes two parts primarily separated; they cavities may be called solution pockets. Some were linked by an artificial shaft mined in 1974 neighbouring cupolas integrate owing to breach- during the works aimed at stabilization of the ing of intervening limestone walls. Most pockets hill (Fig. 5) (Szelerewicz, Górny 1986). The old are rounded in shape, and their height equals or series of the cave is spacious and acts as a show exceeds their diameter. Only the minority of the cave. Conversely, the new series is narrow; it cupolas and pockets is guided by joints. A big includes some small chambers separated by in- solution cavity in the ceiling of Grabowski’s tervening thin walls (locally less than 10 cm chamber led to the surface and acted as a cave in thickness) with extremely narrow squeezes. entrance in 19th century. At present it is blocked The pools are present in fissures formed at the with a brick construction. bottom of some chambers. The water table of The cave almost lacks of speleothems. The the pools is located at the altitude of about 199 bottom of the old series is filled with fine- m, that is at the similar level as the Vistula grained clastics; however, the majority of cave (Wisła in Polish) River which flows in the deposits in the old series most probably have proximity of about 50 m from the cave pools. been destroyed during the long lasting use of Some small water insects migrate through the the cave since the Middle Ages (see Firlet 1996). water filled fissures from the Vistula River The vermiculation structures preserved in some (Dumnicka 2000). places on cave walls suggest that the clastics The old series displays a suite of specific fea- also covered the cave walls. The cave clastics are tures which testify the artesian origin of the cave. composed predominantly of clay minerals and They can be observed during a tour through the autochthonous limestone debris. Surprisingly, cave. The old series comprises three rounded they lack any admixtures of the Vistula River de- spatial chambers which form NNW–SSE trend- posits, such as quartz sand (Alth 1877). It proves ing passage. The chambers are up to 8 m in that the cave was completely isolated from the width whereas their length varies between 10 inflow of river waters.

27 9th ProGEO Symposium, Chęciny, Poland, 2018

The pool water is of Ca–Na–HCO3–SO4– Cl type, whereas the drip water represents SO4–Ca–Na type. High concentrations of NO3, SO4, Cl, Na, K, and P suggest that the wa- ter is considerably affected by pollution. The chemical composition of the studied pool water can be the effect of mixing of, at least, two of the components mentioned above. The wa- ter can: (1) Filtrate from the Vistula River; (2) Percolate down from the surface of Wawel Hill; (3) Migrate from the nearby area, where the city centre is located; and (4) Ascend as arte- sian water from deeper confined aquifer. The first three of the four mentioned water sources may be strongly degraded due to long lasting human occupation of both Wawel Hill and the city centre, as well as pollution of the Vistula River. The high amount of SO4 ions reaching 1439 mg/l in drip water results probably from leaching of litter and rubble poured over the cave in the 19th century. Cultural and historical aspects: Smocza Jama is the most famous Polish cave being the im- portant natural attribute of the legendary his- tory of Poland. According to very popular and commonly known tale, the cave was a dwelling place of a dragon – monster that threatened the Fig. 5. Map of the Smocza Jama Cave (after Gradziński M. et al. 2009). human settlement recently founded by legend- ary Krakus (Krak) King on Wawel Hill. The The cave rocky relief, chiefly extensive ceil- dragon was killed using an artifice, namely it ing solution cavities, shows that Smocza Jama swallowed an animal filled with burning sul- cave developed in the phreatic conditions by phur and left by devious men in front of the slow and long lasting circulation of water of cave entrance. And, consequently, the dragon elevated temperature. Cave fine-grained de- perished in flames (Firlet 1996; some other ver- posits represent residuum after dissolution of sions of this legend are also known). The main Jurassic limestone. The lack of quartz sand, part of the cave, easily accessible for people, has Pleistocene mammal bones and Palaeolithic ar- been known at least since the Middle Ages, the tefacts, proves that the cave was isolated since legend was recorded first time by the histori- its inception till Holocene time. The cave origi- cal source from the 13th century. Subsequently, nated due to the basal input of ascending water. Smocza Jama Cave and tales connected with it The Wawel horst composed of Oxfordian lime- have been popular matter of notices in chron- stone was at that time confined by overlying icles, other descriptions and pictures of the Miocene clays. The artesian circulation within Royal Castle during the 15–18th centuries. In Oxfordian limestone was possible owing to a the 17th and 18th centuries even a tavern exi- topographic gradient between the recharge zone sted in the cave entrance. Since the first half of located northward of Kraków and the potential the 19th century the main part of the cave was discharge zone in the former Vistula River val- periodically accessible for public. The geologi- ley over the cave. cal and archaeological studies in the cave were

28 FIELD TRIP: Geological framework of the Kraków Region conducted in 1874, whereas geotechnical and References construction works preparing the cave for pub- Alth, A. 1877. Sprawozdanie z badań geologiczno-an- lic access were performed in 1917‒1919, 1945 tropologicznych przedsięwziętych w tak zwanéj and 1966‒1976. Since 1919 the cave has been ‘Smoczéj Jamie’ na Wawelu w Krakowie. Zbiór almost permanently accessible for public as Wiadomości do Antropologii Krajowej, 1, 2–7. show cave (excluding the winter time and with Komisja Antropologiczna Akademii Umiejętnoś- breaks during the 2nd World War and conserva- ci; Kraków. tion works). New, hardly accessible (narrow and Brocx, M., Semeniuk, V. 2007. Geoheritage and geo- conservation – history, definition, scope and scale. partly filled with water) part of the cave was ex- Journal of the Royal Society of Western Australia, plored in 1974‒1995 (Szelerewicz, Górny 1986; 90, 53–87. Firlet 1996). As a consequence, Smocza Jama Dixon, G. 1996. Geoconservation: an internation- th Cave, described since the 19 century up to now al review and strategy for Tasmania, pp. 1–101. in numerous guidebooks, fables, poems, nov- Miscellaneous Report, Parks and Wildlife Service; els, handbooks and even political dissertations, Tasmania. has become one of the most popular inanimate Dumnicka, E. 2000. Studies on Oligochaeta taxons in natural element of Polish tradition and culture. streams, interstitial and cave waters of southern Currently, the cave, which is a part of the Wawel Poland with remarks on Aphanoneura and Poly- Royal Castle Complex, is the most popular cave chaeta distribution. Acta Zoologica Cracoviensia, in Poland visited by ca. 300 thousand people per 43, 339–392. year (the statistics comes from the beginning of Firlet, E.M. 1996. The Dragon’s Den in Wawel Hill; history, legends, dragons, pp. 1–154. Universitas; the 21st century, see Urban 2011). Kraków. (In Polish with English summary). Geoheritage values and their usage: Smocza Gradziński, M., Motyka, J., Górny, A. 2009. Artesian Jama Cave is the site of two specific values. The origin of a cave developed in an isolated horst: a first is its meaning in a cultural, even national case of Smocza Jama (Kraków Upland, Poland). tradition as a significant element of Polish leg- Annales Societatis Geologorum Poloniae, 79, 159– endary and real history, while the second is its 168. obvious scientific-educational importance as an Kleczkowski, A. S. 1976. Hydrogeological conditions of the Wawel Hill in Cracow. Biuletyn Geologi- example of specific karst developed in isolated czny, 21, 153–175. (In Polish with English sum- horst massif, which is perfectly illustrated by mary). morphology of the cave walls. Both values con- Motyka, J., Gradziński, M., Różkowski, K., Górny, stitute the geological heritage of this site: this A. 2005. Chemistry of cave water in Smocza first one due to the cultural inspiration provided Jama, city of Kraków, Poland. Annales Societatis by this strictly geological object, according to Geologorum Poloniae, 75, 189–198. the geoheritage definitions proposed by Dixon Szelerewicz, M., Górny, A. 1986. Jaskinie Wyżyny (1996), as well as Brocx and Semeniuk (2007), Krakowsko‒Wieluńskiej, pp. 1–200. PTTK Kraj; while this second value is strictly of geological Kraków. nature. The most amazing (shocking) is the fact Urban, J. 2006. Legal and practical protection of that the whole public awareness is currently fo- caves in Poland. Chrońmy Przyrodę Ojczystą, 62, cused on the cultural aspect of Smocza Jama 1, 53–72. (In Polish with English summary). Urban, J. 2011. Tourist accessibility of caves in Po- Cave, whereas an information about the natural land – description of the problems. In: T. Słomka character of this object is completely lacking: (Ed.), Geotourism; a cariety of aspects, p. 55–70. there is no information about the cave origin, AGH University of Sciences and Technology; features and even that this is a cave! Kraków.

29 9th ProGEO Symposium, Chęciny, Poland, 2018

OJCÓW NATIONAL PARK

Stop 2.1. The Kraków Gate rock Leaders: Piotr Ziółkowski and Józef Partyka

Keywords: Upper Jurassic, carbonates, facial development, palaeoenvironment, fossils, Ojców National Park GPS coordinates: 50°11’45.4” N; 19°49’44.8” E Location: The Kraków Gate rock is situated in the central part of the Ojców National Park, at the mouth of the Ciasne Skałki Gorge to the Prądnik Valley.

Highlights of the Ojców National Park Józef Partyka The route of the trip within a field session leads In front of Kraków Gate, on the other side of from the King’s Łokietek Cave through Ciasne the Prądnik Valley, one can see a large rock mas- Skałki Gorge to the spectacular erosional rock sif of Koronna Mountain with Ciemna (Dark) form called Kraków Gate (in Polish ‒ Brama Cave. A large part of the massif is under active Krakowska) ‒ one of the Park’s classics. On the protection. Trees are removed and sheep graze way, one can observe forest communities which are naturally restructured. The place of formerly in that part. In the proximity to this massif, there planted pines is gradually taken by beech and fir. is a pictoresque view to the Panieńskie (Maiden) The walls of the bottom part of the Ciasne Skałki Rocks and a solitary rock of Igła Deotymy (Dio- Gorge are under strict protection. tima’s Needle).

Origin of the Upper Jurassic limestone Piotr Ziółkowski Geological settings: Ojców National Park stones (Trammer 1989). In places where the (ONP) owes its unique character and beauty to sponges grew massively, dome-like forms called the Upper Jurassic limestones that build numer- bioherms grew on the sea bottom. In addition to ous picturesque rocks the park is famous for. sponges, a variety of bacterial (microbial) struc- This rock formation outcrops along valleys of tures played a significant role in the construc- the two streams, Prądnik and Sąspówka, at the tion of bioherms, forming coatings and mats distance of 11 km. The limestones were formed on the sediment surface. Thus, they stabilized during Oxfordian and Kimmeridgian time (ca. the sediment, helping to create a rigid bioher- 160‒154 million years ago) on the bottom of a mal framework (Trammer 1989). Other benthic warm, epicontinental sea that covered the area organisms also dwelled in such marine envi- from today’s Portugal, France, Germany, and ronments. These included brachiopods, sea ur- Poland, to Romania and the Caucasus (Matyja, chins, mussels, bryozoans, foraminifers, small crabs and serpulids. Ammonites and belemnites Wierzbowski 1995). The Tethys Ocean stretched predominated among the floating organisms in out to the south of this zone (Fig. 6). the sea. Palaeoenvironment and biotas: Lithistid and Between areas of intense growth of sponge hexactinellid sponges played an important role bioherms, deeper zones (inter-biohermal basins) in the formation of the Upper Jurassic lime- developed. Organisms characteristic of bio-

30 FIELD TRIP: Geological framework of the Kraków Region

Fig. 6. Palaeogeography of Europe in Late Jurassic time (after Matyja, Wierzbowski 1995, modified) herm areas may also be found in these depres- picturesque rock forms (cliffs, spurs, pinnacles) sions, but generally they were the places where from which their name was taken. They form for lime mud accumulated. In some inter-bioher- example Maczuga Herkulesa (Herkules’ Club) mal basins, deposits formed due to underwater rock in the Pieskowa Skała Hill, The Kraków mass movements and density currents can be Gate rock in the Prądnik Valley, the rocks of found (Matyszkiewicz 1989; Ziółkowski 2007). Igła Deotymy (Diotima’s Needle) and Rękawica Submarine avalanches developed on the mar- (Glove) in the Koronna Mountain. Rocky lime- gins of the bioherms and sediments transported stones developed from sediment accumulated by gravity were accumulated in adjacent basins. in the sponge bioherms. They are light-cream The triggering factor of the slides could be the or light-yellow rocks when freshly fractured, sea bottom palaeorelief and earthquakes. and light-grey and white when weathered. The Lithology and geomorphology: Several vari- rocky limestones are mostly massive and more eties of Upper Jurassic limestones can be dis- resistant to weathering than the other varieties tinguished in the Ojców National Park and its of limestones in the area. No flints occur in this vicinity. These include: (1) Rocky limestone; (2) lithological variety, as opposed to its common Bedded limestone; (3) Pelitic limestone; and (4) occurrence in the bedded limestones. Numerous Detritic limestone (Matyja, Wierzbowski 2004; fossils of siliceous sponges preserved as cal- Ziółkowski 2007). careous mummies (in which the soft body of (1) Rocky limestone: The most prominent in the sponge was replaced by dark calcite) can be the landscape is the rocky limestone building noticed on the weathered surfaces of the rock.

31 9th ProGEO Symposium, Chęciny, Poland, 2018

These sponges attaining different shapes belong (4) Detritic limestone: It is composed of lime- to the Hexactinellida and Lithistida (Trammer stone grains of different sizes. These limestones 1989). Their common feature is a skeleton com- were created as a result of submarine slides posed of siliceous spicules. In the early stage that moved the detritic material from the bio- of diagenesis these siliceous spicules were dis- herm margin to adjacent basins. Fine- and me- solved and replaced by calcite, and the silica was dium-grained limestones can be found among removed from the biohermal limestone. the detritic limestones; they also include vari- (2) Bedded limestone: It is a dominant litho- eties that contain fragments of previously con- logical variety of limestone in the ONP area. It solidated layers and blocks of rocky limestone forms thick layers within the rocky limestones. reaching up to several metres in diameter. These limestones are strongly eroded and karst- ified due to their lower resistance to weathering References and karst corrosion. In the present-day landscape Matyja, B.A., Wierzbowski, A. 1995. Biogeographic they form depressions between the rocks. They differentiation of the Oxfordian and Early Kim- do not differ much from the rocky limestones, meridgian ammonite faunas of Europe, and its being characterized by bedding and a higher po- stratigraphic consequences. Acta Geologica Po- rosity. The thickness of individual layers varies lonica, 45 (1-2), 1–8. Matyja, B.A., Wierzbowski, A. 2004. Stratigraphy from 0.6 m up to 3 m. In these limestones nu- and facies development in the Upper Jurassic merous dark-grey or brown oval siliceous con- of the Kraków-Częstochowa Upland and the cretions occur flints, with a diameter of up to 30 Wieluń Upland. In: J. Partyka (Ed.), Zróżnicow- cm. They occur in prominent horizons empha- anie i prze miany środowiska przyrodniczo-kul- sizing the bedding or, less commonly, randomly turowego Wyż yny Krakowsko-Częstochowskiej distributed within the layers. Silica building the (Diversification and transformation of natural flints was derived from dissolved sponge spic- and cultural environment of the Kraków-Często- ules. chowa Upland), Przyroda, 1, 13–18. Ojcowski (3) Pelitic limestone: It contains a variety of Park Narodowy; Ojców. (In Polish with English limestones that originated beyond the areas of summary). bioherm development, in the basins between Matyszkiewicz, J. 1989. Utwory osuwiskowe w wapie- them. Pelitic limestones are light-grey, grey or niach górnego oksfordu w Ujeździe. Przewodnik 40. Zjazdu Polskiego Towarzystwa Geologicznego, grey-yellow in colour with layers from a few 83‒88. Wydawnictwo Akademii Górniczo-Hut- to several dozen centimetres thick, sometimes niczej w Krakowie; Kraków. showing cube separation when weathered. The Trammer, J. 1989. Middle to Upper Oxfordian spong- limestone layers are interbedded with marly es of the Polish Jura. Acta Geologica Polonica, 39 layers from 1 cm to several centimetres thick. (1-4), 49–91. Fossils are rare and poorly preserved in the pel- Ziółkowski, P. 2007. Stratygrafia i zróżnicowanie fac- itic limestones. They are represented e.g. by am- jalne górnej jury wschodniej części Wyżyny Kra- monites, belemnites and trace fossils. kowskiej. Tomy Jurajskie, 4, 25–38.

32 FIELD TRIP: Geological framework of the Kraków Region

Stop 2.2. Ciemna Cave Leader: Michał Gradziński

Keywords: karst cave, Upper Jurassic limestone, Neogene, archaeological site, Kraków Upland, Ojców National Park GPS coordinates: 50°11’49.8” N; 19°49’52.1 E” Location: Ciemna Cave is located 62 m over the bottom of the Prądnik Valley at the altitude of 372 m in the central part of the Ojców National Park.

Geomorphology and genesis of Ciemna Cave Michał Gradziński Geomorphology and genesis: Ciemna Cave (in subsequently remodeled in a vadoze zone. The Polish – Jaskinia Ciemna) is one of the most fa- caves were filled with clastic deposits and con- mous caves located in the Ojców National Park. tain some speleothems; the most common being There are 742 caves registered in the Prądnik moonmilk flowstones and cave coralloids. Cave catchment; the majority are located in the na- clastics contain remnants of Pleistocene animals. tional park area (Gradziński M. et al. 2008). The caves were settled by prehistoric human in They are formed in Oxfordian limestones along the Pleistocene and Holocene time. vertical joints. The majority of the caves are hor- Ciemna Cave is a 209 m long horizontal cave izontal and relatively short; they do not exceed (Gradziński M. et al. 2007) (Fig. 7). It is open a length of a few hundred meters. The caves for tourists, but not equipped with electricity. It were formed in phreatic conditions and were comprises a large chamber which is 88 m long

Fig. 7. Map and cross-sections of Ciemna Cave in the Prądnik Valley (after Gradziński M. et al. 2007, simplified)

33 9th ProGEO Symposium, Chęciny, Poland, 2018 and 23 m wide. The narrow passage is an ex- cave clastic series. They are Holocene in age and tension leading from the chamber to the east. contain dark-coloured laminae associated with A small rocky-tunnel is an independent part of activity of human within the cave (Gradziński the cave. The cave is formed in Oxfordian lime- M. et al. 2003). stone, partly along joints. References Ciemna Cave is famous for ceiling cupolas, up to 3.5 m in diameter, which are common Alex, B., Valde-Nowak, P., Regev, L., Boaretto, E. 2017. Late Middle Paleolithic of Southern Poland: in the chamber and the deeper series of the Radiocarbon dates from Ciemna and Obłazowa cave. They testify that the cave was formed Caves. Journal of Archaeological Sciences: Re- in phreatic conditions (Gradziński R. 1962). ports, 11, 370–380. However, neither the origin of the cave nor its Gradziński, M., Górny, A., Pazdur, A., Pazdur, M. F. age have been studied in detail, so far. The cave 2003. Origin of black coloured laminae in spele- is the relict of a bigger cave, most probably of othems from the Kraków-Wieluń Upland. Boreas, Neogene age, dissected by erosion. The other 32, 532–542. cave, called Oborzysko Wielkie, also used to Gradziński, M., Michalska, B., Wawryka, M., Szel- belong to this system. One of the possible hy- erewicz, M. 2007. Jaskinie Ojcowskiego Parku potheses concerns the importance of hypogean Narodowego, Dolina Prądnika, Góra Koronna, circulation of water of elevated temperature for Góra Okopy, pp. 1‒122. Ojcowski Park Naro- the origin of the cave. However, the formation dowy, Muzeum im. Prof. Władysława Szafera; Ojców. of the cave by floodwater must be also taken Gradziński, M., Gradziński, R., Jach, R. 2008. Geolo- into consideration. gy, morphology and karst of the Ojców area. In: A. The cave comprises a series of clastic de- Klasa, J. Partyka (Eds), Monografia Ojcowskiego posits, which is up to 7 m thick. It is composed Parku Narodowego, Przyroda, p. 31–95. Wydawn- of loam or silt mixed with autochthonous lime- ictwo Ojcowskiego Parku Narodowego; Ojców. stone debris (Madeyska 1982). At present the (In Polish with English summary). series is well-exposed in an archaeological Madeyska, T. 1982. The stratigraphy of palaeolithic trench. The cave clastics host a rich assem- sites of the Cracow Upland. Acta Geologia Polon- blage of Palaeolithic flint-tools which represent ica, 32, 227–242. Micoquian, Mouste rian and Taubachian (Valde- Valde-Nowak, P., Alex, B., Ginter, B., Krajcarz, M. T., Nowak et al. 2014). Animal bones, including Madeyska, T., Miekina, B., Sobczyk, K., Stefańs- Ursus spelaeus, are also present. Radiocarbon ki, D., Wojtal, P., Zając, M., Zarzecka-Szubińs- ka, K. 2014. Middle Paleolithic sequences of the dates reveal that bones associated with Ciemna Cave (Prądnik valley, Poland): the prob- Micoquian levels are older than 50 ka (Alex et lem of synchronization. Quaternary International, al. 2017). Some stalagmites occur on the top of 326‒327, p. 125–145.

34 FIELD TRIP: Geological framework of the Kraków Region

Stop 2.3. Władysław Szafer Natural History Museum Leader: Józef Partyka

Keywords: nature protection, geoconservation, biotic and abiotic values, Kraków Upland, Ojców National Park GPS coordinates: 50°12’35.9” N; 19°49’45.6” E Location: Władysław Szafer Natural History Museum of the Ojców National Park is situated in the Prądnik Valley, nearby the Zamkowa (Castle) Hill in Ojców, in the central and most visited by tourists place of the Park. The administration centre of the Park is located at the distance of 300 m to the north. Bio- and cultural heritage of the Ojców National Park and its protection and conservation Józef Partyka Nature protection: The Ojców National Park blue aconite (Aconitum variegatum), Moldova was established on 14 January 1956. Its area aconite (A. moldavicum), Carpathian cardamine ranges 2145.62 ha. It is located in the southern (Dentaria glandulosa), and others. Among the part of the Kraków‒Częstochowa Upland and xerothermic species growing on the rocks there includes the valleys of two streams: Prądnik and is e.g. European feather grass (Stipa joannis). Sąspówka. The geological substratum is com- The Park’s fauna includes over 6 000 species. posed of Jurassic limestones. Karst groundwater However, the expected number is estimated at activity and other denudational processes led to about 12000 species. One of the most characteris- the creation of a unique landscape with deep tic mammals of the Park are the bats (17 species), gorges, various rock formations and caves. There a lot of which hibernate in the Park’s caves (there are over 700 caves discovered within the Park are 25 species of bats in Poland), and the most and two the longest are: King’s Łokietek Cave common are a greater mouse-eared bat (Myotis (320 m long) and Ciemna Cave (230 m long). myotis) and lesser horseshoe bat (Rhinolophus The most valuable forest compositions, mainly hipposideros). Carpathian beech, covering the surface of 251 ha Within the frames of the Park one can find (12% of the Park’s area) are under strict protec- numerous monuments of architecture. Amongst tion. The remaining part of the Park is under ac- them there are e.g.: the well preserved Renaissance tive and landscape protection. Forest ecosystems Pieskowa Skała Castle; the remnants of the Gothic cover the largest area of the Park (71%). These are Ojców Castle; sacral hermitage of Blessed Salo- mixed forests, Carpathian beech and oak-horn- mea in Grodzisko; old milling settlement Boro- beam forests, and spots of sycamore and ther- niówka and some examples of 19th /20th century mophilic beech. Agricultural area covers 464 ha spa architecture. (22%) including 81 ha of meadows (4%). These areas are gradually turning into forests owing to Risk and protection: The Park is surrounded the sub-optimal agricultural use of the grounds, by large and populous villages, Krakow and whereas the meadows need mowing which is Upper Silesian Industrial Region are located in done as part of active protection. The landscape close proximity. The neighborhood of the Park protection generally covers private property. is an attractive settlement area which results in There are about 950 species of vascular a large investment pressure and development of plants in the Park. They are mainly the species construction and infrastructure. It constitutes a of Central Europe (the most numerous), North great external threat to the nature of the Park, Europe and Asia (i.a. beech, hornbeam, common whose source is its buffer zone, which is the oak). Amongst about 50 species one can find: part that is supposed to protect it from threats. hornbeam (Carpinus betulus), fir (Abies alba), Meanwhile, the pressure on building and con-

35 9th ProGEO Symposium, Chęciny, Poland, 2018 flicts with local communities arising from that protection, negative changes in flora communi- lead to serious problems with keeping ecological ties and depletion of rock flora were recorded. balance and ensuring sustainability of natural Consequently, the area of strict protection was processes. Other threats for the Park include the reduced by the main landmark rock complexes in negative impact of tourism on the Park’s nature, the Prądnik Valley. Currently there are effective extinction of rare and endangered species of protection activities regularly conducted in the plants, including encroachment of the habitats of Park, including mowing the meadows on the bot- local flora by alien species, unfavorable owner- toms of the valleys (about 60 ha) and exposing ship structure (30% of the Park is owned by third the rocks (about 18 ha – 22 surfaces) to enhance parties, mostly private owners). growing of the rock flora. They have been more Protective activities in the Park include tree- widely applied and monitored by the Park since stands reconstruction by adjusting their species 1990s. As the results of monitoring show, this composition to the habitat conditions, mowing form of protection secures the diversity of xe- the meadows followed by collecting and trans- rothermic grassland communities and valuable portation of biomass, removal of undesired plant populations of flora species growing there. species from rare and endangered stands, protec- tion of landscape values, organization of tourist Natural and cultural heritage: Moving along movement. the Prądnik Valley towards Pieskowa Skała in The 1950s (when the Ojców National Park Sułoszowice Village, one can touch the cultural was established) was the time when the con- landscape of the valley with preserved architec- cept of nature conservation in Poland began to ture of the former Ojców spa (preserved villas, shape. At that time a lot of attention was paid wooden Chapel on the Water, and some exam- to the protection and reconstruction of forests, ples of lesser architecture). One permanent ele- and, as a matter of fact, the value of non-forest ment of this landscape seen on the way are the compositions – meadows and xerothermic grass- mowed meadows and rock forms under active lands identified back then as wastelands – was protection, including the Zamkowa (Castle) Hill completely not appreciated. Large part of them in Ojców with remnants of the Gothic Castle on was afforested or left for secondary succession. the top of the hill, and some eye-catching eros- The result of such activities was the reduction inal rock forms as for example Wdowie (Widow) of grassland area by about 70% till the 1990s crags or Maczuga Herkulesa (Hercules’ Club) and significant loss of landscape value of the crag, with the Pieskowa Skała Castle next to it. Park. In order to conserve the grasslands and This castle is best-preserved in the Kraków‒ unique landscape of the Valley of Prądnik in Częstochowa Upland, housing a permanent ex- the 1980s the idea of active protection evolved. hibition of the European painting art from the It was supposed to conserve the bottoms of the 14th century up to the interwar period. valleys covered with meadows and larger com- In less than 60 years of the Ojców National plexes covered with non-forest flora – rock and Park, despite many problems, including finan- xerothermic species. Formerly, the meadows on cial restrictions, the protection and conservation the bottoms of the valleys had used to be inten- of the area allowed preservation of the natural sively used by the local farmers, and farm ani- wealth and natural and traditional cultural land- mals (sheep, goats) had used to be grazed on the scape of the Prądnik Valley, which is also at- rocks that had used to be regularly deforested. tractive for tourists. About 350–400 thousands of As a result of traditional land use on the tourists visit the Park yearly. The objects available territory of the Park, interesting meadow com- for tourists in the Park are: King’s Łokietek Cave, munities and rock flora appeared that mark the Ciemna (Dark) Cave, the Pieskowa Skała Castle, landscape unique. Owing to the cessation of Natural History Museum of Prof. Władysław grazing because of disappearance of the tradi- Szafer, remnants of the Gothic Ojców Castle and tional land use around 1990, and due to the fact the Regional Museum of the Polish Tourist and that many rock communities were granted strict Sightseeing Society.

36 FIELD TRIP: Geological framework of the Kraków Region

Stop 2.4. The Maczuga Herkulesa (Hercules’ Club) crag and Pieskowa Skała Castle Leader: Piotr Ziółkowski

Keywords: Ojców Plateau, Prądnik Valley, Neogene, geomorphology, morphogenesis, rock terraces, Kraków Upland, Ojcowski National Park GPS coordinates: 50°14’34.0”N; 19°46’58.8”E Location: Sułoszowa Village in the northern part of the Ojców National Park.

Neogene morphogenesis of the Ojców Plateau Piotr Ziółkowski Ojców Plateau in Pliocene time: In that time (5.3−2.6 million years ago) the Ojców Plateau was incised and carved with deep ravines of me- ridionally flowing rivers. It was in that time, when the Prądnik Valley began to form (Fig. 8). The development of the valley went through sev- eral stages during Pliocene and Pleistocene time. Four levels of rock terraces are clearly visible on the slopes of the valley, being remnants of subse- quent stages of cutting of the river valley into the ground (Dżułyński et al. 1966). Neogene rock tarraces and kars processes in the Prądnik Valley: The oldest rock terrace (I) is located at the highest position above the pres- ent-day river (i.e. at the level of the summit of the Hercules’ Club). The upper middle terrace (II) is located approximately 25−30 m below the highest terrace. An old road from Ojców to Murownia Village passes through this terrace. The lower middle terrace (III) marks the top of the rock with the ruins of the Ojców Castle, the basis of the Maczuga Herkulesa (Hercules’ Club) crag, and the topmost part of the Kraków Gate rock. This terrace is located about 10−20 m below the previous terrace. The low terrace (IV) is situated a few metres above present-day bottom of the Prądnik Valley (Fig. 8). There, at this level occurs (among others) the window of the Dziurawiec Cave in Ojców (Dżułyński et al. 1966). The development of the Prądnik Valley in the Pliocene was associated with the intensive devel- Fig. 8. Development of the tarraces in the Prądnik opment of karst processes and caves formation. Valley in the Pliocene (after Dżułyński et al. 1966; It has been estimated that the caves were formed Płonczyński 2000).

37 9th ProGEO Symposium, Chęciny, Poland, 2018 in the Miocene, or even earlier, in the Palaeogene warzystwa Geologicznego, 36, 329–343. (In Pol- (Gradziński M. et al. 2007). ish with English abstract). Gradziński, M., Michalska, B., Wawryka, M., Szel- References erewicz, M. 2007. Jaskinie Ojcowskiego Parku Dżułyński, S., Henkiel, A., Klimek, K., Pokorny, J. Narodowego, Dolina Prądnika, Góra Koronna, 1966. The development of valleys in the southern Góra Okopy, pp. 1–122. Wydawnictwo Ojcows- part of the Cracow Upland. Rocznik Polskiego To- kiego Parku Narodowego; Ojców.

PONIDZIE REGION

Stop 2.5. Chotel Czerwony Leaders: Maciej Bąbel, Jan Urban and Anna Chwalik-Borowiec

Keywords: Badenian evaporites, Badenian salinity crises, Carpathian Foredeep, gypsum facies, selenites, giant gypsum intergrowths, largest gypsum crystals, gypsum karst, structural morphology, Nida Basin GPS coordinates: 50°22’47.0”; 20°42’26.7” Location: Escarpment near the road west of the church in Chotel Czerwony.

The Badenian Nida Gypsum deposits and their unique giant crystal facies Maciej Bąbel Introduction: The Badenian (=Wielician) salin- into the uncommon ancient sedimentary facies ity crisis in the Central Paratethys, ca. 13.6 Ma and environments of the giant evaporite basin. BP, in the Serravallian (Middle Miocene), The sequence of the Nida Gypsum depos- leads to widespread evaporite deposition in the its is up to ca. 50 m thick and is bipartite. The Carpathian Foredeep Basin. Gypsum deposits, upper part is mostly clastic and composed of known as the Krzyżanowice Formation, were microcrystalline and fine-grained gypsum. This formed mainly on the northern platformal mar- part of the sequence, called allochthonous, clas- gin of the basin, and the halite deposits crys- tic or microcrystalline unit, is mostly eroded, tallized in the more central areas. Now these mainly in the Quaternary. The lower part of the evaporites are mostly hidden in the subsurface. sequence which is nearly entirely composed In Poland the largest area of outcrops of the of coarse-crystalline gypsum is called autoch- Badenian gypsum deposits occurs at the vicin- thonous or selenite unit. It is up to 16 m thick ity of towns Busko-Zdrój, Wiślica and Pińczów. and is better exposed. This selenite unit will The gypsum deposits of this area are known be presented during the trip. Special attention as the Nida Gypsum deposits (named after the will be paid to the unique mineralogical, crys- Nida river, a left tributary of the Vistula river). th tallographic and sedimentological phenomena Studied since the 18 century they are the best revealed by these deposits, starting with the recognized part of the Badenian evaporites in the lowermost giant-crystalline layer seen in Chotel Carpathian Foredeep Basin (Bąbel et al. 2015). Czerwony outcrop. The outcrop was investigated The Nida Gypsum deposits were not dehy- and described by Pitera (2001) and Chwalik- drated and transformed into anhydrite during Borowiec et al. (2013). diagenesis and burial, and hence their primary sedimentary structures are very well preserved. Selenite facies and the giant gypsum crystals: Therefore these deposits offer an excellent insight Gypsum is a mineral which forms one of the

38 FIELD TRIP: Geological framework of the Kraków Region largest crystals on Earth (Rickwood 1981) and some evaporite deposits contain such crystals. They occur just in the primary evaporite facies known as selenites or selenite deposits. The term selenite has several meanings in geology, but in sedimentology it is used for large (>2 mm) gypsum crystals grown on the bottom of evap- orite basins directly from the overlying brine (Bąbel 2004). There are many varieties or facies of selenites, most of them are well bedded and composed of crystals no more than several cm in size. But there are also some coarse- or gi- ant-crystalline poorly to non-bedded selenite fa- cies composed of very large vertically elongated crystals arranged in a palisade-like manner, forming spectacular rows of ‘standing’ crystal- line prisms. The formation mechanism of these selenites is analogue to the growth of crystals on the walls of druses or mineral veins. Such crystals grew upward on the floor of the basin (like on the druse wall), being covered with Ca- sulphate supersaturated brine. Their growth was almost exclusively syntaxial and not accompa- nying by a creation of new crystal seeds (pre- Fig. 9. The giant gypsum intergrowths exposed west sumably due to a low degree of supersaturation, of church in Chotel Czerwony. Shining 010 perfect Bąbel 2007), and this permitted them to reach cleavage surfaces and composition surfaces (cs) are a very large sizes controlled merely by depth of marked. Note porous skeletal structure of the crystals. brine and available accommodation space. The Photograph by Maciej Bąbel. gypsum deposits seen in Chotel Czerwony out- crop represent just such a selenite facies. – described here since the 19th century (Zejszner 1861; Kontkiewicz 1884). The giant intergrowths The giant gypsum intergrowths: The spec- represent one of the most peculiar selenite facies tacular selenite facies exposed in the outcrop is considering not only the sizes of crystals but called the giant gypsum intergrowths (called in their specific crystallographic, textural, and sed- Polish ‘szklica’; Kwiatkowski 1972, p. 87; Bąbel imentological features. 1987). It is built of crystals from a few deci- metres to over 1.5 m in length. The crystals, Size of crystals: The giant intergrowths facies, arranged in a palisade-like manner, form the pe- exposed best between towns Pińczów, Busko- culiar intergrowths (Wala 1979) resembling the Zdrój and Wiślica on the Nida river, contains gypsum twins called the swallow tails. These the largest natural crystals (individual miner- giant intergrowths build a layer, up to a few als) in Poland. Older Polish reports mentioned metres thick (3.5 m on average), occurring at gypsum crystals reaching length of 4 m here the base of the gypsum section and widespread (e.g. Kontkiewicz 1907), or even more, but these on a very large area of the northern margin of findings remain unauthenticated (Bąbel 2002). the Carpathian Foredeep Basin (from the Czech At present, the largest gypsum crystals are seen Republic, through Poland to the environs of in two outcrops: at Bogucice-Skałki and at Gacki Horodenka in Ukraine). The giant intergrowths villages – 12–14 km NE of Chotel Czerwony exposed in the Nida Gypsum deposits contain (Bąbel 2002, Bąbel et al. 2010). In both sites the the largest recorded Badenian gypsum crystals length of the crystals is estimated as ca. 3.5 m.

39 9th ProGEO Symposium, Chęciny, Poland, 2018

Such a size (3.5 m) is a documented maximum length of the discussed gypsum crystals. In the visited Chotel Czerwony outcrop the crystals at- tain 2.7 m in length (Fig. 9; Kasprzyk 1993). The described giant crystals are compara- ble to the largest existing (i.e. documented and preserved) natural crystals in the world. In the evaporite facies the largest gypsum crystals are known from the Messinian of the Mediterranean Fig. 10. Orientation of the crystallographic axes (a, where some specimens have been reported to c; b is normal to a–c plane) and the 010 perfect cleav- attain 6 m (at Buraitotto, SE Favara in Sicily) or age planes of gypsum in the exemplary 101 twin (left), even 7.5 m in length (a few km N-NE Paphos, and in the typical giant intergrowths (right), hachure on Cyprus; see references in Bąbel 2002). marks the position of 010 planes. Unfortunately, these evaporite crystals remain unauthenticated. The largest documented gyp- dubious exceptions recorded in some older publi- sum crystal (a 100 twin) is a 11.4 m long speci- cations (see references in Bąbel 1991). men originating from hypogenic caves at Naica More detailed crystallographic measure- in Mexico (Badino et al. 2009). ments reveal that the pair of crystals forming the intergrowth, i.e. the component crystals, are not Crystallographic peculiarities: The Badenian symmetrical to each other in the crystallographic intergrown giant crystals break most easily sense (Fig. 10, left; Bąbel 1987). Furthermore, along the flat boundaries of contact between orientation of crystallographic axes a, b and c of them, called the composition surfaces, or along the component crystals in every particular inter- the planes of the perfect gypsum cleavage 010. growths is always slightly different than in the Just these surfaces, usually oriented vertically other ones (Bąbel 1991). Thus any strict twin law or subvertically to the depositional surface, are cannot be determined. However, statistically, the visible in the walls of outcrops (Fig. 9). The glow crystals fall into certain range of orientations of sunlight reflected from the large 010 surfaces similar to the present in the 101 gypsum twin gives an unforgettable impression, unknown in (Fig. 10). The intergrowths thus differ not only the other types of rocks. The Polish regional from the gypsum twins but from any twins, be- name of the discussed rocks (szklica from szklić cause such features do not fit to definitions of się – in Polish – to glisten, to shine like glass) the twins. The Badenian forms appear to be dif- refers to this feature. The intergrown crystals ferent from any so far recorded oriented inter- observed from the side of the 010 cleavage sur- growths of the same crystal species. faces reveal striking similarity to the contact 101 The intergrowths show also striking asym- swallow-tail gypsum twins (Fig. 10). metry in frequency distribution of some mor- It can be seen that the crystals are composed phological features. For example the faces con- of elongated blocks forming re-entrant angle tacting along the composition surface (irrational near the composition surface (Fig. 9) – an an- faces placed between 101, 302, and 111, 111) gle typical of the swallow tail twin morphology show dominance of the ‘left’ hkl forms (54.4%) (Fig. 10, right). Closer investigation, however, re- over the ‘right’ hkl forms (37.6%), (frequency veals a peculiar feature – the surfaces of the 010 of the intermediate h0l forms is equal 8%). The cleavage of the two component crystals are not other peculiar asymmetric morphological fea- parallel, and traces of them do not coincide on tures are described in Bąbel (1991). the composition surface (Fig. 10, right; Kreutz To explain the peculiar nature of these inter- 1925), as it should be in any known type of gyp- growths a hypothesis was proposed that biologi- sum twins (Fig. 10, left; Bartels, Follner 1989; cally produced organic compounds present in the Rubbo et al. 2012; and references in Bąbel 1991), basinal brine influenced both the nucleation and except of a few rare, poorly documented and the growth of the crystals (Bąbel 1991, 2000).

40 FIELD TRIP: Geological framework of the Kraków Region

result of the competitive growth of the crystals (Fig. 11; Bąbel 1987). The morphological obser- vation indicate that the highest rate of crystal growth was in the zone of the re-entrant angle in the upper part of the composition surface. This zone formed a base from which lenticular sub- crystals and their aggregates (crystalline blocks) started to grow up in direction oblique to the composition surface. Growth structures of the giant crystals: History of crystal growth can be reconstructed from the internal growth zoning, usually marked by inclusions incorporated during the growth, which permits to recognize the habit changes of the developing crystal. The upper growth sur- face of the giant intergrowths was uneven and toothed – the flat crystal faces did not appear on that surface (Fig. 11; Bąbel 1987). Therefore the internal growth zoning of these giant crystals is complicated and unclear. The clay particles and some microorganic remnants falling out from the brine column accumulated on the upper sur- faces of the subcrystals and in hollows between them. Consequently, they were incorporated along boundaries between subcrystals and their aggregates, forming streaks oriented obliquely Fig. 11. Mode of crystal growth in the skeletal sub- to the upper growth surface of the crystals (i.e. facies of the giant intergrowths facies (at the top) (see to the depositional surface; Fig. 11, at the top). Fig. 12), and exemplary skeletal intergrowths from The true horizontally oriented growth zones are Leszcze quarry (at the bottom); after Bąbel 1987, very difficult to recognize. Only several such modified. Photograph by Maciej Bąbel. growth zones was documented in the upper part Internal structure and morphology of crys- of the giant intergrowths layer permitting the tals: The giant crystals show a macroscopically isochronous correlation of these selenites in the visible block (mosaic) structure. They are com- Nida Gypsum deposits (Bąbel 2005, Appendix). posed of sub-parallel slightly misoriented indi- Sedimentary environment: It is interpreted that vidual parts or blocks – which can be called sub- the giant intergrowths facies crystallized at the crystals. The subcrystals are easily seen on the bottom of evaporite basin at depths from a few 010 cleavage surfaces as a network of rhomboidal metres up to maximum 10–20 m, under perma- or lenticular fields by their slightly different light nent or nearly permanent cover of Ca-sulphate reflection. Between larger aggregates of such saturated to supersaturated brine (Fig. 12; Bąbel lenticular subcrystals large primary pore spaces 1999, 2004, 2007). commonly occur, which in outcrops are usually The coarsest crystals, particularly those lack- enlarged by karst dissolution. The intergrowths ing synsedimentary dissolution features, grew in display thus spectacular skeletal structure rarely the deepest zones, below an average pycnocline observed in selenite deposits (Figs. 9, 11). Like (i.e. a boundary zone separating water bodies in crystal druses the boundaries between the gi- of significantly different density), at a depth not ant gypsum crystals show the features of the accessible to meteoric water. Presumably, be- compromise (induction) boundaries created as a cause of the low degree of supersaturation, and/

41 9th ProGEO Symposium, Chęciny, Poland, 2018

Fig. 12. Idealised reconstruction of the sedimentary environment of the giant gypsum intergrowths facies (showing palisade structure) and of its skeletal and massive subfacies (after Bąbel 1987, modified). or some organic compounds inhibiting gypsum Bąbel, M. 2002. The largest natural crystal in Poland. crystallization present in the brine, gypsum nu- Acta Geologica Polonica, 52, 251–267. cleation was sparse and the crystal growth was Bąbel, M. 2004. Models for evaporite, selenite and mostly syntaxial. The protracted period of up- gypsum microbialite deposition in ancient saline ward growth led to formation of extraordinarily basins. Acta Geologica Polonica, 54, 219–249. large crystals on the whole marginal area of the Bąbel, M. 2005. Event stratigraphy of the Badenian basin. The skeletal crystals (forming the skeletal selenite evaporites (Middle Miocene) of the north- ern Carpathian Foredeep. Acta Geologica Poloni- subfacies; Fig. 12) were deposited in a relatively ca, 55, 9–29 (with On-Line Appendix). deeper and less oxygenated brine, whereas the Bąbel, M. 2007. Depositional environments of a sali- massive crystals (of the massive subfacies) were na-type evaporite basin recorded in the Badenian crystallised in the shallower brine. gypsum facies in the northern Carpathian Foredeep. References In: B.C. Schreiber, S. Lugli, M. Bąbel (Eds), Evap- orites Through Space and Time. Geological Soci- Bartels H., Follner, H. 1989. Crystal growth and twin formation of gypsum. Crystal Research and Tech- ety, London, Special Publications, 285, 107–142. nology, 24, 1191–1196. Bąbel, M., Olszewska-Nejbert, D., Nejbert, K. 2010. Bąbel, M. 1987. Giant gypsum intergrowths from the The largest giant gypsum intergrowths from the Middle Miocene evaporites of southern Poland. Badenian (Middle Miocene) evaporites of the Acta Geologica Polonica, 37, 1–20. Carpathian Foredeep. Geological Quarterly, 54, Bąbel, M. 1991. Crystallography and genesis of the 477–486. giant intergrowths of gypsum from the Miocene Bąbel, M., Olszewska-Nejbert, D., Nejbert, K., Łu- evaporites of Poland. Archiwum Mineralogiczne, gowski, D. 2015. Guide to field trip A2 (21–22 44 (volume for 1990), 103–135. June 2015). The Badenian evaporative stage of Bąbel, M. 1999. Facies and depositional environments the Polish Carpathian Foredeep: sedimentary fa- of the Nida Gypsum deposits (Middle Miocene, cies and depositional environment of the selenitic Carpathian Foredeep, southern Poland). Geologi- Nida Gypsum succession. In: G. Haczewski (Ed.), cal Quarterly, 43, 405–428. Guidebook for field trips accompanying IAS 31st Bąbel, M. 2000. Giant organic-gypsum intergrowths Meeting of Sedimentologyheld in Kraków on from the Miocene evaporites of Carpathian Fore- 22nd–25th of June 2015, p. 25–50. Polskie Towa- deep Basin. In: N.P. Yushkin, V.P. Lutoev, M.F. rzystwo Geologiczne; Kraków. Samotolkova, M.V. Gavriliuk, G.V. Ponomareva Badino, G., Ferreira, A., Forti, P., Giovine, G., Giuli- (Eds), Mineralogy and life: biomineral homolo- vo, I., Infante, G., Lo Mastro, F., Sanna, L., Te- gies. Abstracts of 3th International Seminar ‛Min- deschi, R. 2009. The Naica caves survey. In: W.B. eralogy and life‛, p. 16–18. Geoprint; Syktyvkar. White (Ed.), Proceedings of 15th International

42 FIELD TRIP: Geological framework of the Kraków Region

Congress of Speleology ‛Karst Horizons’, 3, p. the Miocene of southern Poland. Prace Muzeum 1764–1769. Kerrville, Texas, USA. Ziemi, 19, 3–94. (In Polish with English summary). Chwalik-Borowiec, A., Urban, J., Bąbel, M. 2013. Sta- Pitera, H. 2001. Gips wielkokrystaliczny z Chotla nowisko 10. Chotel Czerwony: odsłonięcie gipsów, Czerwonego. Wiadomości Naftowe i Gazownicze, depresja krasowo-denudacyjna. In: A. Łajczak, A. 4, 10–14. Fijałkowska-Mader, J. Urban, A. Zieliński (Eds), Rickwood, P.C. 1981. The largest crystals. American Georóżnorodność Ponidzia, p. 79‒83. Instytut Geo- Mineralogist, 66, 885–907. grafii Uniwersytetu Jana Kochanowskiego w Kiel- Rubbo, M., Bruno, M., Massaro, F.M., Aquilano, D. cach; Kielce. 2012. The five twin laws of gypsum (CaSO4•2H2O): Kasprzyk, A. 1993. Gypsum facies in the Badenian A theoretical comparison of the interfaces of the (Middle Miocene) of southern Poland. Canadian penetration twins. Crystal Growth and Design, 12, Journal of Earth Sciences, 30, 1799–1814. 3018−3024. Kontkiewicz, S. [Kontkewitsch, S.] 1884. Geolo- Wala, A. 1979. Badania litologiczne mioceńskich war- gische Untersuchen im südwestlichen Theile von Russisch-Polen. Verhandlungen der Russisch-Kai- stw gipsowych i ilastych z wierceń na obszarze serlichen Mineralogischen Gesellschaft zu St. Pe- Niecki Nidy. In: Sprawozdanie z prac badawczych tersburg, 2, 19, 43–84. mioceńskiej serii gipsowej w obszarze Niecki Nidy, Kontkiewicz, S. 1907. Krótki podręcznik mineralogii Zał. 4, pp. 1–31. Unpublished materials. Archiwum (1st edition), pp. 1–226. Księgarnia E. Wende i Przedsiębiorstwa Geologicznego (Kombinat Geo- Spółka (T. Hirż i A Turkut), Rubieszewski i Wrot- logiczny ‘Południe’), Kraków. kowski; Warszawa. Zejszner, L. 1861. O mijocenicznych gipsach i marg- Kreutz, S. 1925. W sprawie ochrony przyrody nieoży- lach w południowo-zachodnich stronach Króle- wionej. Ochrona Przyrody, 5, 58–68. stwa Polskiego. Biblioteka Warszawska, 4 (10), Kwiatkowski, S., 1972. Sedimentation of gypsum in 230–245; (11), 472–487; (12), 715–733.

Structural morphology and karst developed in various rocks e.g. gypsum and marl Jan Urban and Anna Chwalik-Borowiec Geological settings: In geological terms the stop – a graben of WNW-ESE elongation, framed is situated within the northern marginal part of by faults from both (N and S) sides. Within this the Neogene basin of the Carpathian Foredeep structure secondary shallow and wide (usually (Fig. 1), where various lithostratigraphical units gently dipping) folds occur. In the area of Chotel of different lithology of Miocene marine succes- Czerwony and its vicinity several shallow brachy- sion and its substrate crop out and control the folds formed of Miocene–Upper Cretaceous structural relief. The hills in Chotel Czerwony rocks occur. They are genetically connected with are built of the Miocene gypsum deposits and the the transversal tectonic discontinuity: Wiślica– underlying gypsum series, i.e. Upper Cretaceous Busko–Chmielnik zone identified within a deep or Miocene marls. This geographical mesore- substrate (Flis 1954; Łyczewska 1975; Krysiak gion, characterised with significant importance 2000; Urban 2012). of gypsum in structural morphology, is called Geomorphology: The hill crowned with a the Niecka Solecka (Solec Basin), and is a part Gothic church is a monadnock that comprises the Niecka Nidziańska (Nida Basin) macroregion component of greater morphological structure or – according to other geographical division – – frame of large karst-denudational depression Ponidzie. The specific, structural, denudation- 1.5–1.6 km long, 0.7–0.8 km wide and some al-karst landscape of this area is a matter of pro- 20 m deep (Chwalik 2002; Urban et al. 2009, tection in the Nadnidziański Landscape Park that 2015), which is well visible from the hill. The covers this area (Urban 2012; Urban et al. 2012). marginal morphological structure that surrounds Tectonics: The Niecka Solecka geographic re- the depression is composed of the hill with the gion is the Solec Depression in tectonic terms church, the neighbouring monadnock – a char-

43 9th ProGEO Symposium, Chęciny, Poland, 2018

Fig. 13. Denudational karst depression in Chotel Czerwony: a – morphological map (digital terrain model) and b – geological map (after Łyczewska 1972, simplified). Symbol explanations: 1 – Quaternary alluvial overbank sed- iments, 2 – Quaternary fluvial-periglacial sands of the middle terrace, 3 – Miocene clays of the Krakowiec Beds, 4 – Miocene gypsum, 5 – Miocene sands of the Baranów Beds; 6 – Upper Cretaceous marls; 7 – caves in gypsum; 8 – hill range; 9 – nature reserve legally protected. The LiDAR-derived topographical map made under the licence dio.dft.7211.1018.2015_pl_n given to the Institute of Nature Conservation, Polish Academy of Science in Kraków. acteristic table-like Przęślin Hill, as well as the brachy-anticlines in this region. They belong to Góry Wschodnie hill range, which are all built of the older stages of gypsum karst, i.e. subjacent Miocene gypsum series (Fig. 13). This depression and entrenched karst stages, which started to de- is a morphological element similar to ‛polje’ – a velop when meteoric waters reached the gypsum depression typical for carbonate karst, however, it strata in the uppermost parts of brachy-anticlines is formed due to karstifying of gypsum, as well as (Table 1), although nowadays all morphological weathering, karstifying and mechanic erosion of karst elements represent stage of the denuded underlying Upper Cretaceous marls and Miocene karst (Urban et al. 2015). According to the calcu- sands. Moreover, the depression is formed within lation of Chwalik (2002) and Urban et al. (2015), a brachy-anticline, that has constrained the struc- who estimated a rate of mechanical and chemical tural relief – an oval pattern of gypsum hills (karst) denudation, the beginning of the develop- surrounding the depression. This is one of five ment of these large depressions falls on the Early similar inversion depressions formed within the Pleistocene or even Pliocene.

44 FIELD TRIP: Geological framework of the Kraków Region

Table 1. Stages of gypsum karst development in the Solec Basin, Ponidzie (after Urban et al. 2009, 2015).

Conditions, Chronostratigraphy Karst stage Development of karst forms Environment meteoric, infiltration water circula- chemical denudation (karstification) and mechanic Holocene, denuded tion in gypsum series that is widely denudation: formation of karst channels (numer- Late Pleistocene karst outcropped ous caves) at the water-table zone chemical and mechanic denudation: formation of gypsum series entrenched by karst Late and Middle entrenched karst channels (caves) at the water-table zone but valleys, in the entrenched areas mete- Pleistocene karst in spatially upper positions, development of karst oritic water circulation valleys and larger depressions development of karst in the uppermost parts of Middle and Early subjacent denudational entrenchment of the (brachy)anticlines, i.e. currently not existed central Pleistocene karst uppermost parts of (brachy)anticlines parts of large depressions local deep water circulation (e.g. in Pleistocene, Intrastratal fault zones), under the cover of Neo- formation of rare and small cave systems Pliocene (deep) karst gene impermeable rocks

In the structurally controlled relief of the a wide scope of their biotic, landscape, geolog- Niecka Solecka, the gypsum series and, espe- ical and historical values and motivations. The cially, the glassy gypsum layer is the strongest Gothic Saint Bartholomew Church that crowns rock unit that forms upper parts of hills (mo- the hill is obviously the historical monument, nadnocks), hill ranges as well as slope edges which is often visited by touristic groups trav- (cuesta rims). This is inconsistent with theoret- elling from or to the neighbouring Busko Zdrój ical scheme of mineral hardness according to resort. On the occasion these groups visit the which carbonates are harder than gypsum and glassy gypsum outcrop under the church, which is caused by rock fabric: large crystalline gyp- is protected as nature monument. Both gypsum sum is, in fact, stronger than fine-grained and hills forming the frames of the depression are cracked marls with argillaceous admixture. The protected as ‛Przęślin’ and ‛Góry Wschodnie’ large depressions, such as the one observed in nature reserves (Fig. 13). Although in both re- Chotel Czerwony, are very good examples of serves biotic, floristic elements are the princi- this principle because their elevated marginal pal matter of protection, the abiotic, landscape zones are everywhere formed of gypsum unit and geomorphological values of the Przęślin while deepened central parts in almost all of Hill are perfectly discernible from the church them represent (sub-Quaternary) outcrops of vicinity, while the gypsum outcrops in the marls (Urban 2012). At the Chotel Czerwony site Góry Wschodnie Hill Range are hardly acces- this morphological regularity is confirmed by sible and then rarely used as educational site. spectacular relief/landscape element, namely the Nevertheless, despite the publication of pop- Przęślin Hill. This monadnock comprises typical ular materials (Urban 2008, 2012), as well as table-like hill with slopes formed of soft marls activity of landscape park service that have and crowned with almost horizontally oriented promoted the geological heritage of this area, ‛plate’ of glassy gypsum layer with rocky, (sub) the geological heritage of the Chotel Czerwony vertical slopes. This ‛cap’ of strong gypsum layer site seems to be not sufficiently distinguished (partly covered by lobe of upper sabre-like gyp- among other touristic attractions of this region, sum) forms horizontal upper surface (plateau) of which is principally known for its historical this monadnock (Urban 2012). monuments. Geoheritage value and geoconservation: The References whole area of Chotel Czerwony village is lo- Chwalik, A. 2002. Morphometrical characterisation cated within the Nadnidziański Landscape Park, of karstic forms in Wiślica region. In: Materiały whereas its particular elements are protected by XXI Szkoły Speleologicznej. Cieszyn–Morawski various categories of legal protection, regarding Kras, February 7–13, 2002, p. 39‒41. Sosnowiec.

45 9th ProGEO Symposium, Chęciny, Poland, 2018

Flis, J. 1954. Gypsum karst of the Nida Trough. Prace Ponidzie area (Niecka Nidziańska region), Poland. Geograficzne, Instytut Geografii PAN, 1, 1‒73. In: A.B. Klimchouk, D. Ford (Eds), Hypogene (In Polish with English Abstract) . speleogenesis and karst hydrology of artesian ba- Krysiak, Z. 2000. Tectonic evolution of the Carpathian sins, p. 223‒232. Ukrainian Insitute of Speleology Foredeep and its influence on Miocene sedimenta- and Karstology; Simferopol. tion. Geological Quarterly, 44 (2), 137–156. Urban, J., Chwalik-Borowiec, A., Kasza, A. 2015. Łyczewska, J. 1972. Szczegółowa mapa geologiczna The development and age of the karst in gypsum Polski 1:50 000. Arkusz Busko Zdrój. Wydawnic- deposits of the Niecka Solecka (Solec basin) area. two Geologiczne; Warszawa. Biuletyn Państwowego Instytutu Geologicznego, Łyczewska, J. 1975. An outline of the geological struc- 462, 125‒152. (In Polish with English Summary). ture of the Wójcza‒Pińczów Range. Biuletyn Insty- Urban, J., Chwalik-Borowiec, A., Kasza, A., Gubała, J. tutu Geologicznego, 283, 151–189. (In Polish with 2012. Jaskinie i stanowiska krasowe. In: A. Świercz English Abstract). (Ed.), Monografia Nadnidziańskiego Parku Krajo- Urban, J., Andreychouk, V., Kasza, A. 2009. Epigene brazowego, p. 82‒121. Uniwersytet Jana Kochano- and hypogene caves in the Neogene gypsum of the wskiego w Kielcach; Kielce.

Stop 2.6. Skorocice and Skorocicka Valley Leaders: Jan Urban, Maciej Bąbel and Anna Chwalik-Borowiec

Keywords: gypsum facies, selenite deposits, selenite domes, gypsum karst, karst valley, caves, Carpathian Foredeep, Nida Basin GPS coordinates: 50°25’08.5”; 20°40’16.8” Location: Situated within the tectonic Solec Depression, which represents in geographic terms the Niecka Solecka (Solec Basin) region.

The facies of the lower selenite unit of the Nida Gypsum deposits at Skorocice Maciej Bąbel Introduction – selenite facies at Skorocice: The in the previous stop. It is composed of crys- Skorocicka Valley is a karst valley formed within tals more than 1 m in length and forms a layer Miocene gypsum rocks of marginal, northern part about 2.8 m thick. It displays massive structure. of the Neogene basin of the Carpathian Foredeep. Synsedimentary dissolution surfaces are visible The geology of the Skorocicka Valley was de- in the upper part of this layer in the transition scribed by many authors including Flis (1954), zone to the overlying grass-like facies. Turchinov (1997), Bąbel (1999a) and Urban et al. The grass-like facies and its subfacies: The (2013, 2015). grass-like facies is composed of the more or less In the karst valley almost a complete section of continuous rows of crystals (usually a few cen- the lower selenite unit of the Nida Gypsum depos- timetres thick) intercalated with fine-grained its is exposed. The section is here ca. 11 m thick gypsum and/or clay. Fine-grained gypsum com- and comprises three facies (from the bottom to the monly shows wavy lamination and creates small top): the giant gypsum intergrowths, the grass-like domal structures. It is interpreted that this gyp- gypsum and the sabre gypsum (Fig. 14). These fa- sum represents a kind of microbialite deposits cies are particularly well seen on the uncovered and was deposited in the presence of microbial with speleothems walls of Skorocicka Cave. mats covering the basin floor. The giant gypsum intergrowths: The giant Two subfacies of the grass-like gypsum are intergrowths facies is similar to the observed exposed: the subfacies with alabaster beds (in the

46 FIELD TRIP: Geological framework of the Kraków Region

the valley). The subfacies with alabaster beds is characterized by thick (up to 40 cm) intercala- tions of white fine-grained gypsum (alabaster) and scarcity of clay. The selenite crystals in this subfacies form not only rows but also isolated ra- dial aggregates or domal structures. The crystals are from a few millimetres to more than several centimetres long. Within some domal structures they are up to 1 m in length. The grass-like subfacies with clay intercala- tions occurs in the layer ca. 0.8 m thick. Small laminated domal forms composed of fine-grained gypsum and tiny selenite crystals, commonly twinned according to 100, are observed here. The sabre gypsum subfacies and their sedi- mentary structures: The sabre gypsum facies is characterized by occurrence of long (from a few centimetres to over 0.5 m) curved crystals resembling sabres – and called the sabre crystals. Two subfacies are present separated by a thin clastic clay-gypsum layer forming a character- istic marker bed designated by letter h (Fig. 14). The flat bedded subfacies occurs below that layer and is nearly entirely composed of selenite crys- tals forming continuous beds 0.2 to 0.8 m thick (Fig. 15). In the overlying wavy bedded subfacies selenite crystals and their aggregates are placed within the laminated fine-grained gypsum. The aggregates show the features of the so-called selenite nucleation cones (Dronkert 1985). They

Fig. 14. The gypsum sections at the Skorocice and Siesławice sites (hachure reflects mainly the arrange- ment of selenite crystals); 1-6 – gypsum facies and subfacies; 1 – the giant gypsum intergrowths, 2 – the grass-like gypsum with alabaster beds, 3 – the grass- like gypsum with clay intercalations, 4 – the flat bed- ded sabre gypsum, 5 – the wavy bedded sabre gypsum, 6 – the microcrystalline gypsum (after Wala 1963; Bąbel 1999b). southern part of the valley, directly overlying the Fig. 15. Natural bridge at Skorocice. Note concordant giant gypsum intergrowths), and the subfacies orientation of sabre gypsum crystals with apices di- with clay intercalations (in the northern part of rected to the east. Photograph by Maciej Bąbel.

47 9th ProGEO Symposium, Chęciny, Poland, 2018

Depositional environments: The described selenite facies represent various environments (from subaqueous and more or less shallow-brine to subaerial) of a giant salina-type evaporite ba- sin (Kasprzyk 1999; Bąbel 2007a). The gypsum layers originated in a vast flat-bottom marginal zone of the basin. This area was occupied by a system of variable perennial saline pans (<5‒20 m deep, dominated by selenite giant intergrowths and sabre gypsum deposition) and evaporite shoals (dominated by grass-like and fine-grained

Fig. 16. Giant selenite dome exposed in the Pieczara Dzwonów Cave in the Skorocicka Valley. Photograph by Maciej Bąbel, taken in 1999. resemble inverted cones in shape and the lami- nation of the fine-grained gypsum below them is thinned and bent downward presumably due to sinking of the crystals in the soft substrate during their growth. Deformation around the selenite aggregates are also the result of differ- ential compaction, creep or, in places, slumping. Compactional breaks and fractures of the sabre crystals are very common in this subfacies. Orientation of sabre crystals: The majority of the sabre crystals visible in the outcrop is con- formably oriented with apices directed in similar horizontal direction, mostly to the east (Fig. 15). This is a regional feature observed in the sabre facies in the whole margin of basin and it will be discussed in detail in the next stop. Giant selenite domes: In the southern part of the valley the giant domal structures several me- tres in diameter and height appear within the grass-like and sabre facies (Bąbel 2007b). They are primary structures accreted at the bottom Fig. 17. Development of giant selenite domes during of evaporite basin. The domes are visible in drowning of elevated area of evaporitic shoal at cross-sections on the walls of Skorocicka Cave Skorocice, hachure reflects the arrangement of sele- and as hillocks – forms exhumed by weather- nite crystals. Note that giant domes were accreted on ing – at the surface above this cave. The domes the small domal structures scattered on the shoal el- started to grow on the convexities of the bottom evation (after Bąbel 1999a). A – deposition of grass- like gypsum (subfacies with alabaster beds and sub- created by the selenite crystal aggregates within facies with clay intercalations) on a slope of evaporitic the grass-like subfacies with alabaster beds. The shoal. B – sabre gypsum deposition and accretion of most spectacular dome is visible in the cave giant domes, arrow indicates brine current; 1-4 – fa- called Pieczara Dzwonów (Bells’ Cave) which is cies and subfacies; 1 – giant gypsum intergrowths, 2 – formed within the giant selenite dome and shows grass-like gypsum with clay intercalations, 3 – grass- the ceiling resembling a bell owing to the convex like gypsum with alabaster beds, 4 – sabre gypsum; shape of the selenite beds (Fig. 16). 5 – pycnocline.

48 FIELD TRIP: Geological framework of the Kraków Region microbialitic gypsum deposition). The various gypsum facies in the northern Carpathian Fore- morphologies and fabric of the bottom-grown deep. In: B.C. Schreiber, S. Lugli, M. Bąbel (Eds), crystals in the giant intergrowths, the grass-like, Evaporites Through Space and Time. Geological and sabre gypsum facies, reflect different com- Society, London, Special Publications, 285, 107– positions and properties of the brine in the sepa- 142. rate saline pans evolving in time. The sequence Bąbel, M., 2007b. Gypsum domes in the karst relief of Ponidzie region, southern Poland. Prace Instytutu of facies: the giant intergrowths → grass-like Geografii Akademii Świętokrzyskiej w Kielcach, gypsum → sabre gypsum (Fig. 14), is interpreted 16, 71–89. (In Polish with English Summary). as a result of shallowing followed by deepening Dronkert, H. 1985. Evaporite models and sedimen- accompanying with salinity rise (Bąbel 1999b). tology of Messinian and Recent evaporites. GUA The growth of giant selenite domes was re- Papers of Geology, Ser. 1, 24, 1–283. lated to drowning of evaporite shoal and rise of Flis, J. 1954. Gypsum karst of the Nida Trough. Prace salinity (Figs. 16, 17; Bąbel 1999a). The subfacies Geograficzne, Instytut Geografii PAN, 1, 1–73. with alabaster beds represents former shoal el- (In Polish with English Summary). evations overgrown with small domes built Kasprzyk, A. 1999. Sedimentary evolution of Bad- of aggregates of gypsum crystals. During the enian (Middle Miocene) gypsum deposits in the drowning of the shoal these small domes devel- northern Carpathian Foredeep. Geological Quar- oped into larger forms due to syntaxial growth terly, 43, 449–465. Turchinov, I.I. 1997. Lithological controls on devel- of crystals taking place below a pycnocline, in opment of karst processes in the Badenian gypsum a more saline, deeper brine. The domes were of the Carpathian Foredeep (southern Poland and overgrown with successive layers of sabre gyp- West Ukraine). Przegląd Geologiczny, 45, 803– sum which accreted concordantly with the initial 802. (In Polish). bottom convexities. The giant domes occur in Urban, J., Chwalik-Borowiec, A., Bąbel, M. 2013. clusters, one near the other, passing laterally into Stanowisko 9. Skorocice, Dolina Skorocicka: a flat or wavy bedded sabre gypsum deposited in dolina krasowa w gipsach. In: A. Łajczak, A. Fi- nearby depressions. jałkowska-Mader, J. Urban, A. Zieliński (Eds), Georóżnorodność Ponidzia, p. 69–79. Instytut References Geografii Uniwersytetu Jana Kochanowskiego w Bąbel, M. 1999a. Facies and depositional environ- Kielcach; Kielce. ments of the Nida Gypsum deposits (Middle Urban, J., Chwalik-Borowiec, A., Kasza, A. 2015. Miocene, Carpathian Foredeep, southern Poland). The development and age of the karst in gypsum Geological Quarterly, 43, 405–428. deposits of the Niecka Solecka (Solec Basin) area. Bąbel, M. 1999b. History of sedimentation of the Biuletyn Państwowego Instytutu Geologicznego, Nida Gypsum deposits (Middle Miocene, Car- 462, 125–152. (In Polish with English Summary). pathian Foredeep, southern Poland). Geological Wala, A. 1963 (printed for 1962). Korelacja litostraty- Quarterly, 43, 429–447. graficzna serii gipsowej obszaru nad ni dziańskiego. Bąbel, M. 2007a. Depositional environments of a sa- Sprawozdania z Posiedzeń Komisji, Polska Aka- lina-type evaporite basin recorded in the Badenian demia Nauk, Oddział w Krakowie, 7/12, 530–532.

Blind karst valley with numerous associated caves (karst conduits) as a unique example of active karst Jan Urban and Anna Chwalik-Borowiec Tectonics: The gypsum strata gently dip to- Geomorphology: The Skorocicka Valley in the wards east (thus are stretched parallel to the val- most typical example of active, currently de- ley elongation) in the upper and middle sections veloping karst valley in the Polish territory. Its of the valley (Fig. 18) and are approximately hor- karstic origin and nature is perfectly reflected by izontal in its lower part of the section (Flis 1954; its topographic division into the upper–middle Urban et al. 2015). section and the lower section, which are sepa-

49 9th ProGEO Symposium, Chęciny, Poland, 2018

Fig. 18. Skorocicka Valley: A – map (after Urban et al. 2015; simplified), B – fragment of rocky wall and cave in 2012 (photograph by J. Urban); C – fragment of the same view and the Wielki Schron Cave in 1951 (photo J. Fijałkowski). Symbol explanations: 1 – plateau and its relict elements within valley; 2 – valley (gorge); 3 – rock wall; 4 – escarpment; 5 – extent and dip of rock strata; 6 – perennial (solid line) and seasonal (dashed line) super- ficial stream (Potok Skorocicki); 7 – cave without water-pool or stream; 8 – cave of size too small to the map scale, without water-pool or stream; 9 – cave with water-pool or stream; 10 – cave of size too small to the map scale, with water-pool or stream, 11 – spring; 12 – swallow hole; 13 – arrow pointing the place presented on photographs B and C as well as Fig. 16. Caves mentioned in the text: a – Tunel (in Skorocice), b – Jaskinia z Potokiem, c – Wielki Schron, d – Jaskinia Stara, e – Pieczara Dzwonów, f – Jaskinia Górna, g – Jaskinia Skorocicka, h – Schronisko pod Drogą Zachodnie, i – Schronisko pod Drogą Wschodnie, j – Jaskinia u Ujścia Doliny. rated by transversal rock bar – a natural bridge Skorocicki (Fig. 18). The other evidences of karst called in Polish Wysoka Droga, and hydrologi- origin of this valley are: (1) Lack of apparent cally connected with underground conduit of the streambed on the valley bottom; (2) The occur- Skorocicka Cave with the stream called Potok rence of numerous irregular hills (karst hums)

50 FIELD TRIP: Geological framework of the Kraków Region

Fig. 19. Broad and very uneven bottom of Skorocicka Valley with numerous hums; at the background a bar of Wysoka Droga which closes the upper section of the valley, with the entrances of two small caves. Photograph by Jan Urban. and some depressions (dolines) within the bottom small karst-weathering forms or cavities devel- of wider parts of the valley; (3) Numerous caves oped due to gravitational collapses of karst forms. which are relicts or active fragments of an un- All these features indicate that the valley was derground stream channel (Figs. 18, 19). Totally formed due to the gravitational destruction of 33 caves were recorded in the Skorocicka Valley underground stream channels and lake chambers and its close vicinity, the longest of which is that developed in the water table zone owing to Skorocicka Cave (232 m long), which represents the karst process. Consequently, the Skorocicka in main part an active underground streambed of Valley represents a mature karst valley. Such or- the Potok Skorocicki stream (Urban 2008; Urban igin of the valley is additionally confirmed by its et al. 2008, 2009, 2012, 2015). Numerous other direction (elongation) parallel to the stretching caves are also located within the water table zone of gypsum strata, which indicates that the karst and comprise fragments of stream channel, as for development was driven by the direction of the example Stara Cave (86 m long), and two other underground flow in the water table zone, along ones called in Polish Jaskinia z Potokiem (46 m) the bedding plain (Flis 1954; Urban 2008; Urban and Pieczara Dzwonów (91 m) caves. Some of et al. 2008, 2009, 2015). High water mineralisa- the caves, e.g. Jaskinia u Ujścia Doliny (122 m), tion in the gypsum aquifer suggests active con- contain lake chambers. Some other caves, e.g. temporary karstification processes (Dumnicka, Jaskinia Górna (61 m), are situated above the wa- Wojtan 1993; Różkowski et al. 2015). ter table and thus represent the preserved frag- The Skorocicka Valley and its caves represent ments of relict underground streambeds. Some the youngest stage of gypsum karst in the Niecka of them are tunnels that transpierce hums, e.g. Solecka region – a denuded karst (Table 1). Tunnel Cave in Skorocice (18 m) (Figs. 18, 20). They have been developed during last several Other caves of the Skorocicka Valley represent to several ten thousands years (Late Pleistocene

51 9th ProGEO Symposium, Chęciny, Poland, 2018

Fig. 20. Cave conduits formed as underground stream channels and abandoned by water due to water table lowering: A – Pieczara Dzwonów Cave (two level of channels are visible), B –Skorocicka Cave. Photograph by Jan Urban. and Holocene), however, the beginning of the was published in German in the first scientific Skorocicka Valley formation (the oldest and up- geological monograph of Polish territory, and permost karst conduits in this place) could reach seventy years later, in Polish, by Pusch (1903). back the older stage of the entrenched karst Since that time numerous scientific and popu- (Urban et al. 2008; 2015). lar descriptions of karst forms in the Skorocicka Invertebrate fauna and bats were stud- Valley were issued (Kontkiewicz 1882; Sawicki ied in the Skorocicka Cave (Wołoszyn 1990; 1918‒1919; Malicki 1947; Nowak 1986; Wołoszyn Dumnicka, Wojtan 1993). Hibernating bats have 1990; Gubała et al. 1998; Urban, Gągol 1999; been monitored in this cave every winters. Urban et al. 2003, 2008, 2009, 2012, 2015). Cultural and scientific context: The relief and Geoheritage value and geoconservation: The landscape of the Skorocicka Valley, in particular Niecka Solecka (Solec Basin) is the only region its caves, rocky sides (scarps) and uneven bottom in Poland, in which active karst processes and its with hums, attracted people since the first mani- effects are fully accessible for scientific-educa- festations of tourism in the region in the first half tional observations and the Skorocicka Valley is of the 19th century, when Busko Zdrój resort was famous karst valley in which a continuous and founded. In the publications propagating this re- unchangeable evolution of such valley can be sorts (first such book was issued in 1834) the accurately described and demonstrated for edu- Skorocicka Valley was described as picturesque cational purpose. The karst forms of this valley and mysterious place of recreation and cultural have been known for their aesthetic and land- activity for people cured and relaxing in this scape values as well as scientific importance for resort (Urban, Gągol 1999). In that time visits last two hundred years (see above). Therefore, of ‛bathers’ from Busko Zdrój were such pop- although the principal objective of the establish- ular that even short story describing such visit ing, in 1960, the Skorocice Nature Reserve was a that included a music concert in the cave was unique steppe, xerothermic and rocky flora, the written by Dziekoński (1983) and published by educational-scientific values of karst forms also Wiśniewski (2002). were a matter of human interest and protection In the same period (1836‒1837) the detailed since the beginning of its conservation. Several description of gypsum karst, based – among oth- guidebooks concerning the biotic and abiotic or ers – on the observations in the Skorocicka Valley, only karst values of this nature reserve were pub-

52 FIELD TRIP: Geological framework of the Kraków Region lished (Urban 2008, 2012) and several times the Sawicki, L. 1918–1919. O krasie gipsowym pod Bus- educational trail was traced in the valley. kiem. Przegląd Geograficzny, 1 (1–2), 306–310. Unfortunately, fast overgrowing of grassy, Turchinov, I.I. 1997. Lithological controls on develop- steppe meadows of the reserve area with synan- ment of karst processes in the Badenian gypsum of thropic plant species and then shrubs and trees the Carpathian Foredeep (southern Poland and West Ukraine). Przegląd Geologiczny, 45, 803–802. has been the most dangerous process that has Urban, J. 2008. Kras gipsowy w Nadnidziańskim i Sza- threatened natural and landscape values of the nieckim Parku Krajobrazowym, pp. 1–87. Zespół Skorocicka Valley (Fig. 18 B and C). After the Nadnidziańskich i Świętokrzyskich Parków Krajo- ending of pasturing and then grassland moving, brazowych; Kielce. large part of the area has been covered by such Urban, J. 2012. Dziedzictwo geologiczne. In: A. vegetation. Although this vegetation does not di- Świercz (Ed.), Monografia Nadnidziańskiego Par- rectly threaten the caves, it significantly masks ku Krajobrazowego, p. 35–81. Uniwersytet Jana the valley relief, diminishes its landscape val- Ko cha nowskiego w Kielcach; Kielce. ues and ousts unique steppe plant communities. Urban, J., Andreychouk, V., Gubała, J., Kasza, A. 2008. Occasional removing of this vegetation has not Caves in gypsum of the Southern Poland and the Western Ukraine – a comparison. Kras i Speleolo- been effective, because the shrub and tree com- gia, 12 (21), 15–38. munity has been easily renewed. Urban, J., Andreychouk, V., Kasza, A. 2009. Epigene References and hypogene caves in the Neogene gypsum of the Ponidzie area (Niecka Nidziańska region), Dumnicka, E., Wojtan, K. 1993. Invertebrates (with Poland. In: A.B. Klimchouk, D. Ford (Eds), Hy- special regard to Oligochaeta) of the semi-un- pogene speleogenesis and karst hydrology of ar- derground water bodies in the gypsum caves. tesian basins, p. 223–232. Ukrainian Institute of Mémoíres de Biospéleologie, 20, 63–67. Speleology and Karstology; Simferopol. Dziekoński, J.B. 1983. Duch jaskini. In: J. Tuwim Urban, J., Chwalik-Borowiec, A., Kasza A. 2015. The (Ed.), Polska nowela fantastyczna, 2. Władca cza- development and age of the karst in gypsum de- su, p. 5–17. Wydawnictwo Alfa; Warszawa. posits of the Niecka Solecka (Solec Basin) area. Flis, J. 1954. Gypsum karst of the Nida Trough. Prace Biuletyn Państwowego Instytutu Geologicznego, Geograficzne, Instytut Geografii Polskiej Akademii 462, 125–152. (In Polish with Eglish Summary). Nauk, 1, 1–73. (In Polish with English Abstract). Urban, J., Chwalik-Borowiec, A., Kasza, A., Gu- Gubała, J., Kasza, A., Urban, J. 1998. Jaskinie Niec- bała, J. 2012. Jaskinie i stanowiska krasowe. In ki Nidziańskiej, pp. 1‒173. Polskie Towarzystwo A. Świercz (Ed.), Monografia Nadnidziańskiego Przyjaciół Nauk o Ziemi; Warszawa. Parku Krajobrazowego, p. 82–121. Uniwersytet Kontkiewicz, S. 1882. Sprawozdanie z badań geologic- Jana Kochanowskiego w Kielcach; Kielce. znych dokonanych w 1880 r. w południowej częś- Urban, J., Gągol, J. 1999. When were the caves near ci guberni kieleckiej. Pamiętnik Fizjograficzny, 2, Skorocice visited. Jaskinie, 1 (14), 1–31. (In Polish 175–202. with English Abstract). Malicki, A. 1947. Zabytki przyrody nieożywionej na Urban, J., Gubała, J., Kasza, A. 2003. Caves in gyp- obszarach gipsowych dorzecza Nidy. Chrońmy sum of the Nida basin, Southern Poland. Przegląd Przyrodę Ojczystą, 1–2, p. 31–38. Geologiczny, 51, 1, 79–86. (In Polish with English Nowak, W. 1986. Karst phenomena of the Nida Basin. Abstract). Studia Ośrodka Dokumentacji Fizjograficznej, 14, Wiśniewski, W.W. 2002. Wycieczka do jaskini w 87–117. Skorocicach w noweli fantastycznej z I połowy Pusch, J.B. 1903. Geologiczny opis Polski oraz XIX wieku. In: M. Gradziński, M. Szelerewicz, innych krajów na północ od Karpat położonych, J. Urban (Eds.), Materiały 36. Sympozjum Spe- pp. 1–216. Druk S. Święckiego; Dąbrowa. leologicznego, Pińczów, 25–27.10.2002, p. 5–19. Różkowski, J., Jóźwiak, K., Chwalik-Borowiec, A. Sekcja Speleologiczna Polskiego Towarzystwa 2015. Water chemistry in the Neogene and Cre- Przyrodników im. Kopernika; Kraków. taceous sulphate and carbonate rocks of the Nida Wołoszyn, B.W. 1990. Caves of Ponidzie Landscape Basin area. Biuletyn Państwowego Instytutu Geo- Park Complex. Studia Ośrodka Dokumentacji Fiz- logicznego, 462, 163–170. (In Polish with English jograficznej, 18, 275–341. (In Polish with English Abstract). Abstract).

53 9th ProGEO Symposium, Chęciny, Poland, 2018

Stop 2.7. Siesławice Leaders: Maciej Bąbel and Jan Urban

Keywords: selenite facies, curved gypsum crystals, oriented crystal growth, brine paleocurrents, gypsum karst, caves, Carpathian Foredeep, Nida Basin GPS coordinates: 50°26’59.0”; 20°41’29.1” Location: Situated within the tectonic Solec Depression, which represents in geographic terms the Niecka Solecka (Solec Basin) region.

The Badenian sabre gypsum facies and oriented growth of selenite crystals Maciej Bąbel Introduction: In the abandoned gypsum quar- the flat bedded subfacies of the sabre gypsum ries the upper part of the selenite unit and the occurs composed of continuous selenite layers overlying microcrystalline (clastic) unit crop out in which the crystals grew evenly over the en- (Fig. 14). The sabre facies is best exposed in tire surface of the basin floor (Figs. 21A, 22). this outcrop, described previously by Niemczyk The bedding planes are mostly represented by (1997), Bąbel (2015) and Bąbel et al. (2015). synsedimentary dissolution and/or erosion sur- faces, which are commonly covered with gyp- Sabre gypsum subfacies: The sabre facies is sum sand showing normal graded bedding. separated by the thin clastic clayey-marly-gyp- The wavy bedded subfacies of sabre gypsum sum marker bed h into two parts. Below bed h appearing above the bed h is built of separate

Fig. 21. Sabre gypsum facies and sabre crystals. A – Flat bedded sabre gypsum with concordant orientation of sabre crystals at Siesławice site, compactional breaks of crystals are arrowed; photograph by M. Bąbel. B – Morphology of sabre crystals; a – sabre crystal growing by advance of the prism faces 120; b – crystal growing by advance of lens-shaped subcrystals; note zoning related to growth of the 120 faces on the 010 surface (after Bąbel 1996). C – Initial forms of sabre crystals; a – 100 gypsum twin as a nucleus of sabre crystals, b-d – twinned nuclei growing on the substrate with low chance (b), higher chance (c) and the highest chance (d) to survive in the competitive growth; the fastest growth direction related to accretion of the apical 120 faces is shown by red arrows, the length of arrows corresponds to chance of survive (after Bąbel et al. 2015).

54 FIELD TRIP: Geological framework of the Kraków Region

Fig. 22. Tree trunk trace in sabre gypsum, Siesławice site. A – Mould of tree trunk overgrown by selenite crystals; note conformable orientation of sabre crystals. B – Mould of tree trunk (and of its side branch?); detail of A. C – Mode of deposition of the drifting tree on basin bottom. D – Way of incrustation of the tree by the growing selenite crystals. Photographs by Maciej Bąbel. aggregates of the sabre crystals (locally form- velopment of side faces was extremely inhibited ing the so-called selenite nucleation cones; Bąbel (Fig. 21B, a). The interior of such crystals is al- 1986) lying within the fine-grained gypsum. most entirely composed of two contacting growth In this subfacies the crystals grew as isolated sectors of the 120 and the 120 faces. The apices of groups, more or less simultaneously with depo- the other sabre crystals were not terminated by the sition of fine-grained gypsum. Compactional flat 120 prism faces but by many parallel lenticu- deformation of the soft sediments surrounding lar forms or subcrystals (Fig. 21B, b). The inter- the crystal aggregates are well developed. In the mediate forms with apices being partly 120 prism whole outcrop the compactional fractures and faces and partly lenticular forms are common. breaks of the sabre crystals are very common. The sabre crystals represent the so-called Broken and fractured crystals are also observed twisted crystals. Their curved shape is a primary near fault surfaces (Fig. 21A). feature and is a result of the deformation of the Morphology and growth zoning of sabre crys- crystal lattice during the crystal growth. Some tals: The morphology and internal structure of sabre crystals are split into a bunch of subparallel the sabre crystals is excellently visible in the out- aggregates of sabre crystals (Fig. 21B, b; 23, at crop. The crystals are usually seen split along the the top). 010 cleavage surfaces which ran from the base The crystals with apices terminated by 120 to the apex of the crystals (Fig. 21A, B). Internal faces show pronounced growth zoning. The zon- growth structures are well seen of these surfaces ing is related to development and advance of the and in thin plates split along the 010 cleavage 120 faces and is seen as set of parallel dark and planes observed in transparent light (Fig. 23). light streaks of a fraction of millimetre thick It can be easily reconstructed that most com- forming traces of these faces (Fig. 21B, a; 23). monly the crystals grew by advance of the flat The darker streaks are enriched with inclusions 120 prism faces in the apical zone whereas the de- of organic material, mostly tube-like remnants

55 9th ProGEO Symposium, Chęciny, Poland, 2018

the water column were deposited on the faces of the crystals as organic detritus which was then incorporated into the crystal bodies during the accelerated growth in the dry season. Moulds of trees in sabre gypsum: In the south part of the outcrop, at the base of the wavy subfacies (directly above the bed h), a unique structure is visible. Two horizontal elongated tube-like empty holes form giant pore spaces which are surrounded by a radially grown gyp- sum crystals (Fig. 22). The sabre crystals form a domal structure above these holes. These empty spaces are moulds of the tree trunk (larger hole) and probably its branch (smaller hole). The tree was carried from the land by flood water. Then it floated in basinal water as drift wood and when ‘anchored’ at the bottom it became a substrate for the gypsum crystal growth. The wood was later degraded during diagenesis. The tree trunk was probably surrounded by a crown of branches that rested on the substrate and lifted the trunk above the bottom. Therefore the crystals could grow on the trunk and the branch centrifugally in every direction, both up, down and horizontally. Fig. 23. Growth zoning in sabre gypsum crystals seen on the 010 perfect cleavage surfaces (at top) and in Concordant orientation of sabre crystals and plates split along the 010 cleavage observed in trans- its significance: The other unique structure seen parent light (at bottom), Siesławice site. Direction of in this outcrop is ordered and concordant orien- crystal growth is marked by arrows. Photographs by tation of sabre crystals. The predominant orien- Maciej Bąbel. tation of the largest sabre crystals is perfectly of some microorganic debris, 300–500 μm long visible in one long wall of the outcrop which and 50–90 μm in diameter. coincides with direction of this orientation. It is This very regular mm-scale growth zoning seen that the majority of the apices of sabre crys- suggests monomictic hydrographic regime of the tals are turned horizontally towards NE (Figs. evaporite basin, i.e. regular mixing of the strati- 21A, 22A, 25A). This orientation is interpreted fied brine once a year (Fig. 24). In the wet season as a result of the competitive growth of the crys- of the year the brine was density stratified and tals ‘fighting’ for free space, modified by the then the growth of crystals was inhibited. In the accelerated growth upstream of the Ca-sulphate supersaturated brine flowing over the bottom. dry season mixing of the basinal brine took place and then the crystal growth was accelerated due Depositional environment: The environment to intensive evaporation (Bąbel, Becker 2006). of crystal growth was similar to this in which The microorganic remnants represent seasonal the giant gypsum intergrowths were crystallised blooms of some planktonic micoorganisms dif- (Fig. 25). Nevertheless, the morphology of crys- ficult to univocal taxonomic determination (cy- tals was different because they grew in brines of anobacteria?, chlorophytes?, colorless sulphur different composition and properties (probably bacteria?) possibly associated with eutrofication more saline in case of sabre gypsum). The basic of the basinal brine (Cackowska et al. 2016). The difference was that the crystals of sabre gypsum dead microorganic remnants falling down from grew syntaxially, in combination with seeding

56 FIELD TRIP: Geological framework of the Kraków Region

Fig. 24. Interpreted depositional environment and structure of brine column during the growth of oriented sabre crystals (after Bąbel, Becker 2006, modified). (nucleation) of new crystals on the surfaces of one component crystal of the twin. During fur- the pre-existing crystals. ther growth the component crystals unfavourable The crystals started to grow from the tiny 100 oriented, i.e. with the direction of fastest growth twins attached to the substrate and usually invis- not vertical or subvertical (Fig. 21C, b), were ible with naked eye (Fig. 21C, a). At this stage eliminated from the further growth because they the earliest selection took place. The twins grew did not have enough space for the development. with the re-entrant angle directed upwards to the Such crystals did not attain large sizes. The long substrate or the depositional surface, which is sabre crystals with a typical curved shape devel- known as the so-called Mottura’s rule (Ogniben oped from the favourably oriented twin seeds, 1954). This rule determined the initial orientation with the direction of fastest growth of one com- of the sabre crystals, which developed from the ponent crystal vertical or nearly vertical (Fig.

57 9th ProGEO Symposium, Chęciny, Poland, 2018

Fig. 25. Brine palaeocurrents reconstruction. A – Rose diagram showing orientation of apices of sabre crystals at Siesławice; n – number of measurements, cr – consistency ratio, mean vector is coloured in purple (after Bąbel, Becker 2006). B – Scheme showing method of brine current vector determination, mean vector is interpreted as parallel to the brine current. C – Scheme showing competitive growth of sabre gypsum crystals in calm and flowing brine (after Bąbel 2002). 21C, c, d). Such crystals have the highest chance bottom was flowing predominantly in the same to win in the competitive growth. However, be- or similar direction it was able to influence the cause of the crystal twisting during the growth, growth competition. The crystals with 120 api- the 120 faces forming the crystal apex gradually ces pointed upstream grew with an accelerated changed the growth direction from vertical into rate (Fig. 25C, at the bottom). They easily attain more and more horizontal (Fig. 21B) and it was the position erected over the bottom surface and the cause that these long crystals also did not the larger sizes, winning the competition with survive the competition for space with the sur- the unfavourable oriented neighbours. The ac- rounding neighbours. Therefore, sooner or later celerated crystal growth presumably took place they were also eliminated from the competitive during mixing period in the dry season of the growth. year (Fig. 24). The resulted unique oriented tex- When the crystallisation took place in the ture is an excellent indicator of the brine flow di- calm water the sabre crystal apices were directed rection in selenite evaporite basins (Fig. 25B), so in every horizontal direction and the resulted far recorded only in the Badenian and Messinian texture of the selenite beds was like in Fig. 25C evaporites (e.g. Lugli et al. 2010). (at the top). However, when the brine over the Concordant orientation of sabre crystal apices

58 FIELD TRIP: Geological framework of the Kraków Region in similar horizontal direction is a feature (or sed- on oriented selenite crystals in the Nida Gypsum imentary structure) observed in the sabre gypsum deposits (Badenian, southern Poland). Geological facies in the whole Carpathian Foredeep Basin Quarterly, 46, 435–448. (in the Czech Republic, Poland and Ukraine). The Bąbel, M. 2004. Badenian evaporite basin of the measurements of this structure indicate that the northern Carpathian Foredeep as a drawdown sa- brine flow ‛en mass’ along the northern shores lina basin. Acta Geologica Polonica, 54, 313–337. Bąbel, M. 2015. Stanowisko 3. Siesławice. Gipsy of the basin, from the east to the west, in the szablaste. In: S. Skompski (Ed.), Ekstensja i in- counterclockwise direction. This flow pattern is wersja powaryscyjskich basenów sedymentacy- interpreted as the longshore cyclonic circulation jnych, 84 Zjazd Naukowy Polskiego Towarzystwa of water (typical of the northern hemisphere), Naukowego, Chęciny, 9–11 września 2015 r., p. similar to the recently observed cyclonic circula- 159–162. Państwowy Instytut Geologiczny – tion in the majority of large lakes and semi-closed Państwowy Instytut Badawczy; Warszawa. basins of the northern hemisphere (Bąbel, Becker Bąbel, M., Becker, A. 2006. Cyclonic brine-flow pat- 2006, with references; Bąbel, Bogucki 2007, with tern recorded by oriented gypsum crystals in the references). In the Nida Gypsum deposits, in the Badenian evaporite basin of the northern Carpath- visited Skorocice and Siesławice outcrops, only a ian Foredeep. Journal of Sedimentary Research, small fragment of this circumbasinal flow is seen 76, 996–1011. (Bąbel 1996, 2002). Bąbel, M., Bogucki, A. 2007. The Badenian evapo- rite basin of the northern Carpathian Foredeep as The sabre gypsum facies represents the sub- a model of a meromictic selenite basin. In: B.C. aqueous environment of the giant salina-type Schreiber, S. Lugli, M. Bąbel (Eds), Evaporites evaporite basin (Fig. 24; Bąbel 2004). The sele- Through Space and Time. Geological Society, nite beds accreted in a vast flat marginal zone of London, Special Publications, 285, 219–246. the basin (Bąbel, Bogucki 2007). The flat bed- Bąbel, M., Olszewska-Nejbert, D., Nejbert K., Łu- ded subfacies was deposited in a brine more than gowski, D. 2015. Guide to field trip A2 (21–22 ca. 1 m deep. The brine was density stratified June 2015). In: G. Haczewski (Ed), Guidebook and seasonally mixed down to the bottom (Fig. for field trips accompanying IAS 31st Meeting of 24, at top). The gypsum crystals and the domal Sedimentology held in Kraków on 22nd–25th of structures accreted under permanent or nearly June 2015, p. 25–50. Polskie Towarzystwo Geo- permanent cover of Ca-sulphate saturated to su- logiczne; Kraków. persaturated brine, i.e. below a pycnocline. Their Cackowska, M., Bąbel, M., Kremer, B. 2016. Inkluzje mikroorganiczne w gipsach szablastych Ponidzia. growth was disturbed by refreshments associ- In: D. Olszewska-Nejbert, A. Filipek, M. Bąbel, A. ated with the drop of the pycnocline, recorded Wysocka (Eds), Granice sedymentologii, 6 Polska by dissolution surfaces and fine-grained clastic Konferencja Sedymentologiczna POKOS 6, Mate- gypsum deposition. The wavy bedded subfacies riały konferencyjne: Przewodnik sesji terenowych, was deposited in a similar environment but as- Streszczenia referatów i posterów, Materiały do sociated with copious deposition of fine-grained warsztatów, 28.06–01.07.2016 Chęciny–Rzepka, p. gypsum. 156–157. Instytut Geologii Podstawowej Wydziału Geologii Uniwersytetu Warszawskiego; Warszawa. References Lugli, S., Manzi, V., Roveri, M., Schreiber, B.C. 2010. Bąbel, M. 1986. Growth of crystals and sedimenta- The Primary Lower Gypsum in the Mediterra- ry structures in the sabre-like gypsum (Miocene, nean: a new facies interpretation for the first stage southern Poland). Przegląd Geologiczny, 34, 204– of the Messinian salinity crisis. Palaeogeography, 208. Palaeoclimatology, Palaeoecology, 297, 83–99. Bąbel, M. 1996. Wykształcenie facjalne, stratygrafia Niemczyk, J. 1997. Osuwisko mioceńskie w serii oraz sedymentacja badeńskich gipsów Ponidzia. gipsowej z Siesławic na tle budowy geologicznej In: P. Karnkowski (Ed.), Analiza basenów sedy- okolic Buska Zdroju. Przegląd Geologiczny, 45, mentacyjnych a nowoczesna sedymentologia. 811–815. Materiały Konferencyjne V Krajowego Spotkania Ogniben, L. 1954. La ‛Regola di Mottura’ di orien- Sedymentologów, p. B1–B26. Warszawa. tazione del gesso. Periodico di Mineralogia, 23, Bąbel, M. 2002. Brine palaeocurrent analysis based 53–64.

59 9th ProGEO Symposium, Chęciny, Poland, 2018

Gypsum karst developed in stagnant underground water: underground chambers and lakes Jan Urban Geological settings: The site of Siesławice is differ in shape from the majority of caves at the located in the northern part of the Carpathian Skorocice site: they are usually wide and low Foredeep, within the outcrop of the Miocene chambers – underground lakes, lacking of con- gypsum rocks (Łyczewska 1975). The site com- duits with streambeds. Different nature of water prises the abandoned gypsum quarry and neigh- flow within the water table zone seems to be the bouring areas in which underground and surface principal reason of this difference: namely in the karst forms occur, that are partly modified by Skorocicka Valley the adequate hydrostatic gra- human impact. dient as well as the orientation of bedding planes (as a basic medium of water movement) force the Tectonics: Gypsum strata are approximately relatively fast water flow along the strata stretch- horizontal. ing, and this causes directional mechanic and Geomorphology: In the abandoned quarry as karst corrosion resulting in conduit formation. well as to the north of the quarry, within the area In turn, at the Siesławice site located within the of undulated morphology only partly changed extensive and low water divide, the hydrostatic due to the human activity, thirteen karst caves gradient is very small, and the horizontal strata have been recorded and documented. These orientation does not stimulate any flow direction. caves range in length from 2 m up to 48 m and As a consequence, the karst corrosion of stagnant represent mostly wide and low chambers (or com- water that fills karst cavities acts similarly in all binations of chambers), frequently partly or al- horizontal directions, which results in formation most totally filled with water, i.e. lakes (Fig. 26). of more or less regular chambers. Therefore, both The chambers are more or less opened to the the Skorocice and Siesławice sites are very good surface (Gubała et al. 1998; Urban et al. 2015). examples that illustrate the reasons of different The occurrence of water in karst forms indicates karst formation driven by only slightly distinct their location within the water table zone and, hydrogeological conditions (Urban et al. 2015). consequently, relatively recent development of The mineral composition of water suggests active these structures during the young stage of karst- contemporary karstification (Dumnicka, Wojtan ification – stage of the denuded karst (Table 1), 1993). similarly to the karst in the Skorocicka Valley. Cultural and scientific context: The tradition of However, the caves at the Siesławice site distinctly karst study at the Siesławice site is also relatively

Fig. 26. Karst lakes in Siesławice; at the right sides of both photographs an entrance of watered cave is visible. Photographs after Henryk Gąsiorowski (1925)

60 FIELD TRIP: Geological framework of the Kraków Region long, because it dates back to the first half of 20th which have visited and have been treated in the century, when the karst lakes in Siesławice were Busko Zdrój resort. described by Gąsiorowski (1925) (Fig. 26). This References author compared the karst forms and process as well as hydrological conditions at the Skorocice Dumnicka, E., Wojtan, K. 1993. Invertebrates (with special regard to Oligochaeta) of the semi-un- and Siesławice sites pointing to some differences derground water bodies in the gypsum caves. between them. He described the state of natural Mémoíres de Biospéleologie, 20, 63–67. elements and postulated protection of both these Gąsiorowski H. 1925. Podziemne jeziorko w krasie sites. The karst site in Siesławice was also de- gipsowym w Siesławicach. Ochrona Przyrody 5, scribed by Malicki (1997), whereas caves were 33–37. documented by Wołoszyn (1990) and Gubała et Gubała J., Kasza A., Urban J. 1998. Jaskinie Niecki al. (1998). Nidziańskiej, pp. 1–173. Polskie Towarzystwo Przyjaciół Nauk o Ziemi; Warszawa. Geoconservation and geoheritage value: Due Łyczewska, J. 1975. An outline of the geological to its high scientific-educational values, the structure of the Wójcza-Pińczów range. Biuletyn Siesławice site has been legally protected as na- Instytutu Geologicznego, 283, 151–189. (In Pol- ture monument since 1987. Moreover, the geo- ish with English Abstract). logical outcrop of gypsum sequence is protected Malicki, A. 1947. Zabytki przyrody nieożywionej na as documentary site (legal category typical for obszarach gipsowych dorzecza Nidy. Chrońmy protection of abiotic, geological elements) since Przyrodę Ojczystą, 1–2, p. 31–38. 2002. Situated very close to the crossroad, the Urban, J., Chwalik-Borowiec, A., Kasza, A. 2015. site has been often polluted (depressions were The development and age of the karst in gypsum filled by rubbish), however it has been regularly deposits of the Niecka Solecka (Solec Basin) area. cleaned. Nevertheless, this site, situated very Biuletyn Państwowego Instytutu Geologicznego, close to the Busko Zdrój resort needs better 462, 125–152. (In Polish with English Summary). Wołoszyn, B.W. 1990. Caves of Ponidzie Landscape protection and, most of all, better educational Park Complex. Studia Ośrodka Dokumentacji Fiz- (geotouristic) use, in particular, in a context of jograficznej, 18, 275–341. (In Polish with English numerous people and, especially, the young ones Abstract).

61 POST-SYMPOSIUM FIELD TRIP – TOP GEOSITES OF GÓRY ŚWIĘTOKRZYSKIE

Convener: Stanisław Skompski Faculty of Geology, University of Warsaw, Żwirki i Wigury 93, 02-089 Warsaw, Poland, e-mail: [email protected]

Leaders: Ewa Głowniak Faculty of Geology, University of Warsaw, Żwirki i Wigury 93, 02-089 Warsaw, Poland, e-mail: [email protected] Stanisław Skompski Faculty of Geology, University of Warsaw, Żwirki i Wigury 93, 02-089 Warsaw, Poland, e-mail: [email protected]

63 9th ProGEO Symposium, Chęciny, Poland, 2018

Itinerary of the Post-symposium Field Trip

Friday, 29th June 2018 9:00 Departure for Miedzianka (20 min, 12 km) 9:20 Stop 1. Miedzianka Hill (1h) 10:20 Departure for Gałęzice and Ostrówka (30 min, 8 km) 10:50 Stop 2. Northern wall of the Ostrówka Quarry (40 min) 11:30 Departure for Kielce ‒ Kadzielnia (30 min, 20 km) 12:00 Stop 3. Kadzielnia Quarry (1h) 13:00 Departure for lunch (50 min, 45 km) 13:50 Lunch in the ‛Świętokrzyski Dwór’ restaurant, in Nowa Słupia village (1h 10 min) 15:00 Departure for Krzemionki Opatowskie (1h, 45 km) (Note, Stop 4. Górno Quarry ‒ cancelled) 16:00 Stop 5. Krzemionki Opatowskie – prehistoric flint mines (2h 30 min) 18:45 Departure for the hotel (15 min, 5 km) 19:00 Arrival to the ‛Leśne Kąty’ Hotel near Ostrowiec Świętokrzyski 19:30 Dinner in the ‛Leśne Kąty’ Hotel Saturday, 30th June 2018 8:30 Departure for Łysa Góra (1h, 45 km) 9:30 Stop 1.6 Łysa Góra (1h) 10.30 Departure for Mogiłki (45 min, 40 km) 11:15 Stop 7. Mogiłki Quarry (45 min) 12:00 Departure for Zachełmie near Zagnańsk (45 min, 30 km) 12.45 Stop 8. Zachełmie Quarry near Zagnańsk (1h) 13:45 Departure for lunch (15 min, 15 km) 14:00 Lunch in the ‛Echa Leśne’ restaurant (1h) 15:00 Departure for Tumlin Gród (20 min, 20 km) 15.20 Stop 9. Tumlin Quarry (40 min) 16:00 Departure for Chęciny via Jaworznia (1h, 25 km) 17:00 Optional stop: Jaworznia Quarry (30 min) 17:30 Departure for Chęciny (20 min, 10 km) ~18.00 Arrival to Chęciny 18:30 Dinner in the symposium venue

64 GEOLOGY OF GÓRY ŚWIĘTOKRZYSKIE (HOLY CROSS MOUNTAINS) Stanisław Skompski

Introduction (description based on Skompski area and exposed the strongly folded Palaeozoic 2015): A brief look at the simplified geological rocks. As a result, the Palaeozoic core is an map of the Holy Cross Mountains (Fig. 1) allows erosional window, an inlier, which exposes us to identify the basic features of their struc- the rocks and structures that were buried be- ture: the central part composed of Palaeozoic neath younger strata, and the observations made rocks, usually referred to as the Palaeozoic core, here are often transposed to some other areas and its Mesozoic margin. Such a distribution where the Palaeozoic is not as well exposed. of stratigraphic units does not reflect the pa- This distinct regional disjunction, additionally laeogeographic relationships but is the effect emphasized by the Variscan angular unconfor- of the post-Laramide erosion that removed the mity, means that the history of the Holy Cross Mesozoic strata from the central part of the Mountains can be subdivided into two parts:

Pliocene Triassic Miocene: terrestrial Permian: Zechstein Pilica Miocene: marine Carboniferous: Lower Tomaszów Oligocene: Lower Devonian Cretaceous: Upper Devonian: Middle/Upper Inowłódz Cretaceous: Lower Devonian: Lower Przytyk Jurassic: Upper Ordovician/Silurian Jurassic: Middle Cambrian Gielniów Jurassic: Lower Precambrian Opoczno RADOM Magmatic veins Sulejów Faults

Szydłowiec

Końskie Iłża

Pilica Tychów Kamienna Skarżysko Radoszyce Przedbórz Suchedniów Starachowice Bałtów Kamienna Tarłów Kunów Bodzentyn Ostrowiec

Wisła

Ożarów Rachów Ćmielów Nowa Słupia KIELCE Daleszyce Opatów

NidaChęciny Łagów Opatówka Iwaniska San

Sandomierz Raków 0 10 20 km Klimontów Czarna

Koprzywianka Chmielnik Koprzywnica Staszów

Pińczów Wisła Nida

Fig. 1. Geological map of the Holy Cross Mountains (after Samsonowicz 1966 – appendix to the ‘Guide to Physical Geology labs’ edited by W. Jaroszewski, Wydawnictwa Geologiczne, slightly simplified).

65 9th ProGEO Symposium, Chęciny, Poland, 2018 the Palaeozoic (precisely: pre-Permian) and the the Permian and Mesozoic time the area of Holy Permian–Mesozoic–Cenozoic history. Cross Mountains has been included into the A significant feature of the Palaeozoic inlier, quickly subsided basin known as Mid-Polish (or which can be spotted already when analyzing Danish-Polish) Trough (Kutek, Głazek 1972). It the Cambrian history of the area, is its differ- originated in the post-Variscan time as eastern entiation into two parts: the southern Kielce part of the Central European Basin, and was in- Region and the northern Łysogóry Region. This filled by facially different deposits from Permian differentiation occurs at several levels; it refers to the Late Cretaceous. Finally trough has been to differences in lithologies and tectonic his- inverted into the Mid-Polish Anticlinorium tory (e.g. Czarnocki 1919, 1957; Samsonowicz during Late Cretaceous time (Krzywiec 2006). 1926; Szulczewski 1971, 1995). Tectonically, the The most uplifted, south-eastern part of this boundary between the regions is the Holy Cross Anticlinorium is referred to as the Holy Cross Fault. In terms of facies, the boundary separat- Mountains. ing areas of different sedimentation and distinct diastrophic rhythms (presence of unconformities References and stratigraphic gaps) is much more difficult to Bełka, Z., Valverde-Vaquero, P., Dörr, W., Ahrendt, determine, particularly due to the fact that its H., Wemmer, K., Franke, W., Schäfer, J. 2002. Ac- position varied in time and usually overstepped cretion of first Gondwana-derived terranes at the the tectonic boundary. In order to eradicate these margin of Baltica. In: J.A. Winchester, T.C. Pha- terminological discrepancies, in this book the raoh, J. Verniers (Eds), Palaeozoic Amalgamation term Łysogóry (or Kielce) Fold Belt will be used of Central Europe. Geological Society of London, for tectonic units, while the term Łysogóry (or Special Publications, 201, 19–36. Czarnocki, J. 1919. Stratygrafia i tektonika Gór Świę- Kielce) Region will refer to facies areas. A basic tokrzyskich. Prace Towarzystwa Naukowego War- problem that significantly influences the inter- szawskiego, 28, 1–172. pretation of the geological history of the Holy Czarnocki, J. 1957. Tektonika Gór Świętokrzyskich. Cross Mountains is the choice of an hypothesis Stratygrafia i tektonika Gór Świętokrzyskich. Prace regarding the palaeogeographic relationships of Instytutu Geologicznego, 18, 11–133. the two regions. An extreme older hypothesis Dadlez, R., Kowalczewski, Z., Znosko, J. 1994. Some suggested that both regions were located in close key problems of the pre-Permian tectonics of Po- vicinity to one another during Palaeozoic time, land. Geological Quarterly, 38, 169–190. and that the development of different facies was Jaworowski, K., Sikorska, M. 2006. Łysogóry Unit influenced by the rate and course of subsidence (Central Poland) versus East European Craton – ap- and by different source areas of the clastic ma- plication of sedimentological data from Cambrian terial (Dadlez et al. 1994; Żelaźniewicz 1998; siliciclastic association. Geological Quarterly, 50, Kowalczewski 2000; Jaworowski, Sikorska 77–88. 2006). This theory has been confirmed by deep Kowalczewski, Z. 2000. Litostratygrafia, paleogeo- seismic soundings, which have shown that in the grafia, facje i tektonika kambru świętokrzyskiego Łysogóry and Kielce regions (the latter lies in (zagadnienia podstawowe i stan ich znajomości). the northern part of the Małopolska Block), the Prace Instytutu Geografii Wyższej Szkoły Peda- gogicznej w Kielcach, 4, 7–66. structure of the deep basement is very similar Krzywiec, P. 2006. Triassic–Jurassic evolution of the to the crustal structure known from the East- Pomeranian segment of the Mid-Polish Trough – European Craton (Malinowski et al. 2005). The Basement tectonics and subsidence patterns (re- recent hypothesis assumes that the regions devel- ply). Geological Quarterly, 50, 491–496. oped independently of one another and merged Kutek, J., Głazek, J. 1972. The Holy Cross area, Cen- during the Variscan Epoch (Lewandowski 1993). tral Poland, in the Alpine cycle. Acta Geologica There are a number of intermediate hypothe- Polonica, 22 (4), 603–653. ses, presuming, for instance, earlier collision Lewandowski, M. 1993. Paleomagnetism of the Pa- times (see Pożaryski 1991; Bełka et al. 2002; leozoic rocks of the Holy Cross Mts (Central Po- Nawrocki 2008; Walczak, Bełka 2017). During land) and the origin of the Variscan orogen. Pub-

66 FIELD TRIP: Top Geosites of Góry Świętokrzyskie

lications of the Institute of Geophysics, Polish Skompski, S. 2015. Geological history of the Holy Academy of Sciences, 265, 1–84. Cross Mountains. In: S. Skompski, A. Żylińska Malinowski, M., Żelaźniewicz, A., Grad, M., Guterch, (Eds), The Holy Cross Mountains – 25 journeys A., Janik, T. 2005. Seismic and geological structure through Earth history, p. 7–18, University of War- of the crust in the transition from Baltica to Palae- saw, Faculty of Geology; Warsaw. ozoic Europe in SE Poland – ‘Celebration 2000’ Szulczewski, M. 1971. Upper Devonian conodonts, experiment, profile CEL02. Tectonophysics, 401, stratigraphy and facial development in the Holy 55–77. Cross Mts. Acta Geologica Polonica, 21, 1–129. Nawrocki, J. 2008. Paleomagnetism. In: T. McCann Szulczewski, M. 1995. Depositional evolution of the (Ed.) The Geology of Central Europe, 2, Mesozo- Holy Cross Mts. (Poland) in the Devonian and Car- ic and Cenozoic, p. 757–760. Geological Society, boniferous – a review. Geological Quarterly, 39, London. 471–488. Pożaryski, W. 1991. The strike-slip terrane model for Walczak, A., Bełka, Z. 2017. Fingerprinting Gondwa- the North German-Polish Caledonides. Publica- na versus Baltica provenance: Nd and Sr isotopes tions of the Institute of Geophysics, Polish Acade- in Lower Paleozoic clastic rocks of the Małopols- my of Sciences, 236, 3–15. ka and Łysogóry terranes, southern Poland. Gond- Samsonowicz, J. 1926. Uwagi nad tektoniką i paleo- wana Research, 45, 138–151. geografią wschodniej części masywu paleozo- Żelaźniewicz, A. 1998. Rodinian–Baltican link of the icznego Łysogór. Posiedzenia Naukowe Państwo- Neoproterozoic orogen in southern Poland. Acta wego Instytutu Geologicznego, 15, 44–46. Universitatis Carolinae, Geologica, 42, 509–511.

Stop 1. Miedzianka Hill Leader: Stanisław Skompski

Keywords: Palaeozoic anticline; Mesozoic margin; Devonian carbonate platform; hydrothermal mineralization GPS coordinates: 50°50’47.7”N, 20°21’36.63”E Location: Highest summit of Miedzianka Hill near Zajączków village.

Geological panorama of south-western corner of the Holy Cross Mountains Bogusław Waksmundzki (based on original description by Waksmundzki 2015) Geological structure and general succession: Miedzianka Hill is the last elevation of Miedzianka (Engl. ‘Copper’) Hill, a nature re- the Chęcińskie Range and in the view from serve since 1958, is a unique place in very many Zamkowa Hill its sharp outline encloses the aspects. Its attractiveness lies not only in the in- western perspective of the Chęcińska Valley. teresting morphology with three rocky summits The hill is also the furthest promontory of the (the highest middle summit at 354 m), but also in Palaeozoic inlier to the south-west, where expo- the magnificent view that it offers towards the sures of Devonian rocks building the limbs of the Chęcińska Valley and the enclosing hill ranges, Chęciny Anticline meet, being surrounded by with Chęciny castle to the south-east (Fig. 2). the Buntsandstein (Lower Triassic) deposits. The Moreover, this locality is worth visiting due to Devonian Miedzianka massif is a tectonic block, its interesting geological structure and the com- from the east and west bounded by faults trans- pelling history of the copper mining, traces of verse to the anticlinal axis, whereas along longi- which, in the form of old shafts and slag heaps, tudinal faults, the block is in a contact, from the are extremely common in the area. north with Cambrian rocks and from the south

67 9th ProGEO Symposium, Chęciny, Poland, 2018

Fig. 2. View from Miedzianka hill towards the east. Photograph by Stanisław Skompski. with the Buntsandstein deposits (Fig. 3). Despite ‘carbonate factory’, and its transformation into a the fact that the Upper Devonian strata com- pelagic platform was characterised by low sedi- posing the massif belong to the southern limb mentation rates (Szulczewski et al. 1996). of the anticline, they possess northerly dips, as On the northern slope, just a few metres be- do the deposits in the northern limb, exposed on low the summit, on a small flat surface occurs Kozi Grzbiet Hill, just opposite Miedzianka Hill. the weathering cover of the Buntsandstein rocks At this locality, the anticline has an asymmetric that probably infilled a karst depression and structure and rocks of the southern limb possess were not subjected to the post-Laramide erosion. overturned dips. Miedzianka Hill is almost entirely built of the History of copper mining and ore origin: The resistant Frasnian sedimentary rocks with a total beginnings of copper mining in the Miedzianka thickness of about 250 m, formed in the reef- area can probably be traced back to ancient lagoonal environments of the shallow marine times. In the middle ages, the ores were ex- th Central Carbonate Platform (Racki 1993). The ploited since the 14 century, whereas the first Frasnian/Famennian boundary is located within written records of copper mining and smelting a thin (about 2 m) package of stratigraphically are from 1478. Regular exploitation was termi- condensed crinoid limestones with cephalo- nated in 1919. The last prospecting was carried pods (Szulczewski 1989, 1995) that are exposed out in 1951–1953, after which the deposit was on the southern hill slope (location of outcrop considered completely exhausted and the lower and detailed stratigraphy in Dzik 2006). The mining pits were flooded. appearance of condensed facies resulted from The deposit originated as a result of two types the drowning of the shallow-water carbonate of processes: hydrothermal, related to primary platform, which till that time was an effective vein mineralization, and subsequent weathering,

68 FIELD TRIP: Top Geosites of Góry Świętokrzyskie

Fig. 3. Asymmetric structure of the western extremity of the Chęciny anticline with overturned Devonian strata in the southern limb visible on Miedzianka Hill (after Waksmundzki 2015).

Fig. 4. Cross-section through the main exploitation field in the Miedzianka Mine (after Rubinowski 1971, modified). whose products were subjected to later exploita- there were formed calcite veins (‘różanka’-type tion (Rubinowski 1958, 1971; Wojciechowski vein calcite). The subsequent veins contained cal- 1958; Balcerzak et al. 1992). cite and primary sulphides. Most common are The primary Variscan hydrothermal mineral- chalcopyrite veins, in which besides chalcopyrite ization developed along fractures parallel to the (CuFeS2) there are subordinate quantities of gers- anticlinal axis and occurred only within Devonian dorffite (NiAsS) and galena (PbS). rocks. In the first stage of the mineralization, Secondary, post-Triassic weathering (hyper-

69 9th ProGEO Symposium, Chęciny, Poland, 2018 genic) mineralization resulted in the formation in the Devonian of the Holy Cross Mountains. of chalcocite (Cu2S) and covellite (CuS), sec- Acta Palaeontologica Polonica, 37, 87–182. ondary copper sulphides, from chalcopyrite and Rubinowski, Z. 1958. Wyniki badań geologicznych tennantite, primary minerals of the hydrother- w okolicy Miedzianki Świętokrzyskiej. Biuletyn Instytutu Geologicznego, 126, 143–153. mal phase. Rubinowski, Z. 1971. Rudy metali nieżelaznych w The richest parts of the deposits occurred in Górach Świętokrzyskich i ich pozycja metalo- the south-western part of the Miedzianka block, geniczna. Biuletyn Instytutu Geologicznego, 247, at the contact of the Devonian limestones with 5–166. the Buntsandstein deposits (Fig. 4). Intense de- Szulczewski, M. 1989. Światowe i regionalne zdarze- velopment of karst processes in this zone resulted nia w zapisie stratygraficznym pogranicza franu z in the accumulation of clasts of the hydrothermal famenem Gór Świętokrzyskich. Przegląd Geologi- ore veins, often strongly altered by hypergenic czny, 37, 551–557. processes, in fractures and caves. Although the Szulczewski, M. 1995. Depositional evolution of the Holy Cross Mts. (Poland) in the Devonian and ore deposit has long been exhausted, mineral col- Carboniferous – a review. Geological Quarterly, lectors still eagerly visit Miedzianka Hill. With 39, 471–488. enough stamina, many attractive specimens can Szulczewski, M., Bełka, Z., Skompski, S. 1996. The be acquired from the old mine slag heaps. drowning of a carbonate platform: an example from the Devonian–Carboniferous of the south- References western Holy Cross Mountains, Poland. Sedimen- Balcerzak, E., Nejbert, K., Olszyński, W. 1992. Nowe tary Geology, 106, 21–49. dane o paragenezach kruszcowych w żyłach Waksmundzki, B. 2015. Chęciny anticline – from siarczków pierwotnych złoża Miedzianka (Góry Zamkowa hill to Miedzianka hill. In: S. Skomps- Święto krzyskie). Przegląd Geologiczny, 40, 659– ki, A. Żylińska (Eds), The Holy Cross Mountains 663. – 25 journeys through earth history, p. 87–97. Uni- Dzik, J. 2006. The Famennian ‘golden age’ of cono- versity of Warsaw, Faculty of Geology; Warsaw. donts and ammonoids in the Polish part of the Va- Wojciechowski, J. 1958. Minerały Miedzianki pod riscan sea. Palaeontologia Polonica, 63, 1–360. Chęcinami (pierwsze minerały niklu na Mie- Racki, G. 1993. Evolution of the bank to reef complex dziance). Prace Muzeum Ziemi, 1, 133‒156.

Stop 2. Northern wall of Ostrówka Quarry Leader: Stanisław Skompski

Keywords: Devonian carbonate platform, Mississippian Culm facies, Permian cover GPS coordinates: 50°50’37.55’’N, 20°24’3.71’’E Location: Large quarry situated near the south- western corner of the Holy Cross Mountains, at the western end of the Gałęzice hills; southern limb of the Gałęzice–Kowala syncline.

Frasnian (Upper Devonian) to Permian stratigraphic succession demonstrating depositional evolution from carbonate platform trough condensed pelagic limestones to basinal setting with sediment-gravity flows and finally epi-Variscan unconformity Stanisław Skompski (based on Skompski 2015) Lithological sequence and stratigraphy: The hillock known as Todowa Grząba, close to the point from which it is recommended to begin a quarry escarpment. The succession (Fig. 5) re- study of the upper Palaeozoic rocks, is a small cords the subsequent phases of development

70 FIELD TRIP: Top Geosites of Góry Świętokrzyskie

SKAŁKA HILL N S TODOWA GRZĄBA

Permian L. Vi s e a n n é a H Vis Tournaisian .-U. Famennian M U. Frasnian G D F E C B 0 10 20 m A

Fig. 5. Geological cross-section through the hills near the village of Gałęzice. For description of units A to H – see the text (after Szulczewski et al. 1996, supplemented with Permian strata). and drowning of the Devonian carbonate plat- carbonate platform that in the Late Devonian form in the south-western part of the Holy Cross spanned the area of the present-day Zgórskie Mountains. The Devonian to Carboniferous se- Range and referred in the geological literature quence, finally folded and uplifted during the as the Dyminy Reef or the Central Carbonate Variscan cycle, was unconformably overlain by Platform. Zechstein deposits in the Permian. B – Cephalopod limestones: Dark-grey Famen- A – Amphiporoid limestones: The thick-bed- nian limestones with abundant cephalopods and ded, light coloured, usually micritic and some- crinoid detritus, characterised by very small times fine-grained limestones, are characterised thicknesses, overlie the amphiporoid lime- by the presence of an impoverished fossil assem- stones with a distinct angular unconformity blage, comprising mainly amphipores, massive (Szulczewski 1978; Szulczewski et al. 1996). The stromatoporoids, and rare gastropods. The strati- Frasnian/Famennian boundary is recorded here graphic position of this complex is indicated by as an erosional surface that formed in conditions the foraminifers Tikhinella fringa, Eonodosaria of subaerial karst weathering (Fig. 7). Famennian stalinogorski, Eogeinizia rara, Eogeinizia alta, bioclastic limestones, characterised by variable Nanicella ex gr. galloway and (?) Multiseptida (up to max. 3 m in diameter) size, contain ex- sp. (Szulczewski et al. 1996). In the uppermost part of the succession, in tremely rich bioclastic material, including goni- the amphiporoid limestones, beds with microbial atites and clymenids, crinoids, trilo bites, some lamination and fenestral structures cyclically ap- corals, bivalves, gastropods, some brachiopods pear, as well as thin breccia beds in which the clasts are coated with characteristic vadose ce- ments. These specific breccia beds (Fig. 6) may be interpreted as incipient sub-paleosol rego- liths (Skompski, Szulczewski 2000). They are typically located in the top of the amphiporoid limestones, and are covered by the laminated beds, which show features typical of tidal flats (intertidal zone). Sedimentation of the amphiporoid limestones was probably related to an environment of iso- Fig. 6. Polished slab incipient of the Frasnian sub- lated lagoons, located in the marginal part of the paleosol regoliths.

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facies known as the Culm. In terms of litho- stratigraphy, these rocks belong to the Zaręby Formation. The age of this unit is roughly estimated from radiolarians as the lower–middle Visean (Żakowa, Paszkowski 1989). The Zaręby For- mation represents the deepest sedimentary en- vironment for the lithologies occurring in the Ostrówka succession, although the depth cannot be determined precisely. Fig. 7. Boundary of the Frasnian amphiporoid lime- E – Gałęzice Debrite Member: Rocks of this stone and Famennian crinoid/cephalopod limestone unit form the Todowa Grząba hillock and are ac- from the Todowa Grząba area (photograph of poli- shed slab). cessible in old research cross-cuts. The complex comprises mainly bioclastic limestones (Fig. 8) and fish remains. Specific bedding resulting with variable bed thicknesses (from several cen- from storm sedimentation, with crinoids in the timetres to 1 m), with extremely abundant fos- basal part and gonitatites in the micritic matrix, sils, which include crinoids, corals and brachio- has been observed in the Famennian deposits. pods (descriptions can be found in Fedorowski The Famennian strata represent a perfect ex- 1971; Żakowa 1974, 1988). The basal part of the ample of stratigraphically condensed deposits, complex is a breccia of variable thickness, con- evidence of which is the abundance of cono- donts. The succession generally commences from the upper Marginifera Zone and extends (with some stratigraphic gaps) to the end of the Famennian, and in some sections – even to the lower Tournaisian (Szulczewski et al. 1996). The bioclastic material deposited on submarine highs was probably washed out to local depressions during high-energy sedimentary events. C – Upper Tournaisian clay-marly succession: The overlying Carboniferous deposits represent a much deeper sedimentary setting. Tournaisian (lowermost Carboniferous) strata include ash- grey, rarely greenish clay shales with thin in- terbeds of pyroclastic material (particularly in the basal part), marls and limestones. The latter lithology sporadically contains abundant fossils: goniatites, trilobites, crinoids, brachiopods and corals (e.g. Czarniecki 1992). Rare grading in the limestones suggests redeposition of the bio- clastic material from the shallows to the deeper part of the basin, which was dominated by clay sedimentation. D – Siliceous shales of the Zaręby Formation: Clay-siliceous shales with radiolarians and numer- ous phosphate concretions are typical represen- Fig. 8. Upper Visean crinoidal marly limestone (Gałę- tatives of the deep-marine lower Carboniferous zice area). Photograph by Stanisław Skompski.

72 FIELD TRIP: Top Geosites of Góry Świętokrzyskie

Nida Platform

Gałęzice area

Fig. 9. Palaeogeographic scheme of the areas located to the south of the Gałęzice area in the late Visean (after Bełka et al. 1996). Drawing by B. Waksmundzki. taining huge blocks of colonial corals (up to 1 m part of the succession with mudstones and sand- in diameter), and limestone and clay lithoclasts stones, complete the Carboniferous succession in derived from Frasnian, Famennian, Tournaisian the Holy Cross Mountains. Sideritic concretions and Visean rocks. are common in these rocks, whereas pyroclastic The deposits, formally representing the admixtures play a significant role in the sand- Carboniferous Limestone facies, which is alien stone composition (Żakowa, Migaszewski 1995). to the Holy Cross Mountains, were formed Numerous, although poorly preserved, fos- within a deep basin from material redeposited by sils from this part of the succession indicate a gravity flows from shallower zones (Bełka et al. late Visean age of the deposits (Goniatites gra- 1996). The basis for such a conclusion include: nosus Zone after Żakowa 1971). Remains of the the position of the complex in the succession Carboniferous flora (mainly stems of club mosses) of deep-marine facies, lens-shaped beds, their are common in this part of the succession. lateral thinning-out and irregular bedding, sedi- G – Permian: Devonian and Carboniferous mentary features of the limestones, the presence rocks folded in the Variscan orogeny are cov- of allochthonous material from the basement, ered, with a distinct angular unconformity, by preferred bioclast orientation, mixing of fauna the Upper Permian strata of the Zechstein facies. from different ecological niches, and the geom- The Zechstein sea shoreline that surrounded the etry of the limestone bodies. The disappearance uplifted massif of the Holy Cross Mountains was of the limestone bodies to the north (drilling log very variable, with numerous narrow bays par- from Skałka Rykoszyńska) indicates that the allel to the Variscan fold axes. One of them was bioclastic material was redeposited from the the Gałęzice Bay. Permian strata exposed on the south (Nida Platform in Fig. 9), from an area slopes of Skałka Hill and further to the north to- that at present is devoid of Carboniferous rocks wards the vicinity of the village of Gałęzice (for (Bełka et al. 1996). detailed descriptions see Bełka 1978) are repre- F – Clay shales of the Lechówek Formation: sented here by very diverse lithologies, including Olive-green clay shales, interbedded in the upper (from the base):

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– fine-grained limestones and marls with for- Czarniecki, S. 1992. Warunki sedymentacji karbonu aminifers of the genera Agathammina and Gałęzic. Przegląd Geologiczny, 40, p. 604. Geinitzina (visible to the naked eye) and bra- Fedorowski, J. 1971. Aulophyllidae (Tetracoralla) from chiopods of the genus Horridonia (upper part the Upper Visean of Sudetes and Holy Cross Moun- of Skałka slopes); tains. Paleontologia Polonica, 24, 1–137. – laminated limestones with galena crystals and Skompski, S. 2015. Palaeozoic of the Gałęzice area. In: S. Skompski, A. Żylińska (Eds), The Holy calcite pseudomorphs after gypsum crystals, Cross Mountains – 25 journeys through Earth His- and with desiccation cracks (road dissecting tory, pp. 118–124. University of Warsaw, Faculty the upper margin of Skałka Hill); of Geo logy; Warsaw. –stromatolitic limestones with interbeds of Skompski, S., Szulczewski, M. 2000. Lofer-type cyclo- chalcedonites (road leading to the crossroads thems in the Upper Devonian of the Holy Cross in Gałęzice), passing upwards into red, calcar- Mts (central Poland). Acta Geologica Polonica, 50, eous quartz mudstones; 393–406. – coarse-grained conglomerates with clasts of Szulczewski, M. 1978. The nature of unconformi- Devonian, sporadically Carboniferous lime- ties in the Upper Devonian–Lower Carboniferous stones (escarpments of the road running condensed sequence in the Holy Cross Mts. Acta through Gałęzice). Geologica Polonica, 28, 283–298. All these sediments were deposited in the Szulczewski, M., Bełka, Z., Skompski, S. 1996. The drowning of a carbonate platform: an example marginal zone of a shallow, narrow and peri- from the Devonian–Carboniferous of the south- odically drying-up bay of the Zechstein sea. western Holy Cross Mountains, Poland. Sedimen- The succession from limestones with foramini- tary Geology, 106, 21–49. fers that were formed at some distance from the Żakowa, H. 1971. Poziom Goniatites granosus w syn- shore, to periodically emersed stromatolites of klinie gałęzickiej (Góry Świętokrzyskie). Prace the intertidal zone indicates a gradually shallow- Instytutu Geologicznego, 60, 1–137. ing sedimentary environment. Conglomerates at Żakowa, H. 1974. Goniatitina from the Upper Visean the top of this succession (also referred to as the (Galezice Syncline), Holy Cross Mts. Annales So- Upper Conglomerates) are probably related to cietatis Geologorum Poloniae, 44, 3–30. the local uplift of the basement blocks and re- Żakowa, H. 1988. Brachiopods of the family Dictyoc- juvenation of the mountainous relief around the lostidae Stehli, 1954 from the Upper Visean strata bay. An analysis of palaeogeographic maps on a of Gałęzice. Biuletyn Instytutu Geologicznego, 358, 45–71. wider regional scale allows us to assume that the Żakowa, H., Migaszewski, Z. 1995. Góry Święto- succession corresponds to the oldest Zechstein krzyskie Mts. In: A. Zdanowski, H. Żakowa cyclothem (Werra) recognized in Central Poland. (Eds), The Carboniferous system in Poland. Prace Państwowego Instytutu Geologicznego, References 148, 109–115. Bełka, Z. 1978. Gałęzice-Zechstein profile along Żakowa, H., Paszkowski, M. 1989. Pozycja stratygra- the road to Rykoszyn. In: T.S. Piątkowski and R. ficzna warstw zarębiańskich (karbon dolny) w Gó- Wagner (Eds), Symposium on the Central Europe- rach Świętokrzyskich. Kwartalnik Geologiczny, 33, an Permian, Guide of excursions, part 2, Zechstein 376–377. of the Holy Cross Mts, p. 49–55. Waksmundzki, B. 2015. Chęciny Anticline – from Bełka, Z., Skompski, S., Soboń-Podgórska, J. 1996. Zamkowa Hill to Miedzianka Hill. In: S. Skomps- Reconstruction of a lost carbonate platform on ki, A. Żylińska (Eds), The Holy Cross Mountains the shelf of Fennosarmatia: evidence from Viséan – 25 journeys through Earth History, p. 87–97. polymictic debrites, Holy Cross Mountains, Po- University of Warsaw, Faculty of Geology; War- land. In: P. Strogen, I.D. Somerville, G.L.I. Jones saw. (Eds), Recent advances in Lower Carboniferous Wojciechowski, J. 1958. Minerały Miedzianki pod Geology. Geological Society of London, Special Chęcinami (Pierwsze minerały niklu na Miedzian- Publications, 107, 315–329. ce). Prace Muzeum Ziemi, 1, 133–156.

74 FIELD TRIP: Top Geosites of Góry Świętokrzyskie

Stop 3. Kadzielnia Quarry Leader: Stanisław Skompski

Keywords: Devonian bioherms, neptunian dykes, stratigraphic condensation GPS coordinates: 50º51’35.05’’N, 20º37’6.78’’E Location: Old quarry in the centre of the city Kielce; A panorama from the summit offers a view towards Karczówka Hill, the Zgórskie and Posłowickie ranges and the Telegraf Hill massif. Devonian carbonate build-up covered by stratigraphically condensed Famennian section; neptunian dykes Stanisław Skompski (based on original description by Łuczyński 2015) Lithologic sequence and stratigraphy: During is largely based on the results of his research the Frasnian (Late Devonian), biohermal carbon- (Szulczewski 1971, 1981, 1995). ate build-ups developed along the margins of a Two basic Upper Devonian complexes are carbonate platform in the central part of the Holy visible in the quarry: Frasnian and Famennian. Cross Mountains. At the present, the quarry is The Frasnian complex (Fig. 10) comprises three the only well-preserved exposure of such car- main lithological units, visible in the eastern part bonate structures in the Holy Cross Mountains. of the quarry. From north to south they include For many years the Kadzielnia Quarry was the (Fig. 11): the massive stromatoporoid‒coral subject of intense geological investigations, lime stones (Kadzielnia limestone), the bioclas- conducted mainly by Michał Szulczewski, who tic limestones, and the Manticoceras lime stones. distinguished the various lithological units, de- The dip observed on the boundaries of certain termined their age relationships on the basis of Frasnian members exposed in the Kadzielnia conodont stratigraphy, and presented a general Quarry in relation to the base of the Famennian facies model. The description presented below is not tectonic but is the effect of sea bottom

Fig. 10. Massive stromatoporoid-coral limestones in the central part of the Kadzielnia quarry. Photograph by Andrzej Konon.

75 9th ProGEO Symposium, Chęciny, Poland, 2018

beds of intraformational breccias. The name com- monly used for this unit is rather inadequate be- cause the Manticoceras goniatites are quite rare in it. Pelagic fauna includes also fish remains, whereas there is a general lack of shallow-marine organisms such as corals or stromatoporoids. The sedimentary environment of the Manticoceras Limestones was therefore deeper in comparison to other Frasnian lithologies exposed in the quarry. The Famennian complex lies unconformably Fig. 11. The main lithological units exposed in the on the Frasnian with a stratigraphic gap (Fig. 11), Kadzielnia Quarry (after Szulczewski 1981, simplified). and has a generally horizontal dip on the scale of the exposure. The succession includes cephalo- morphology and lateral, basinward sediment ac- pod limestone (Cheiloceras Limestone), covered cumulation in the Frasnian (Szulczewski 1981). by a limestone-shale unit. Massive stromatoporoid-coral limestones (for- Cheiloceras Limestone: The Frasnian succes- mally Kadzielnia Massive Limestone Mem- sion in Kadzielnia is overlain by the Famennian ber according to Narkiewicz et al. 1990): They Cheiloceras Limestone. Strata of the two stages comprise biolithic limestones with abundant ben- are separated by a stratigraphic gap that encom- thic fauna preserved in growth positions in a mi- passes up to 8 conodont zones. They contain critic matrix. The most abundant fossils include fossils of pelagic fauna, such as goniatites, nauti- stromatoporoids, sometimes attaining large sizes loids and fish remains. (exceeding 1 m in diamater) and various shapes (from tabular through domical to bulbous). The The Limestone-Shale Complex: The youngest organisms are preserved in growth positions and rocks exposed in Kadzielnia form the Famennian not destroyed; moreover, analysis of their basal Limestone-Shale Complex. It comprises inter- surfaces and growth directions permitted an in- bedded shales and micritic limestones with pe- terpretation of the bioherm slope dip (Łuczyński lagic fauna similar to that in the Cheiloceras 2009). The stromatoporoids are accompanied by Limestones. tabulate corals and less frequent rugose corals, as The primary positive element on the sea well as by brachiopods, gastropods, nautiloids, floor was the Kadzielnia bioherm built of stro- bryozoans and echinoderms. Stromatactis struc- matoporoid-coral limestones. Despite their high tures of ambiguous origin are also common. abundance, the benthic fossils occurring in the Kadzielnia Limestone did not form a rigid struc- Bioclastic Limestones: Crinoids and brachiopods ture, but were loosely distributed in the micritic comprise the main clasts of the bioclastic lime- matrix. Their role, particularly in the case of stones developed as calcarenites and calcirudites. tabular stromatoporoids, was thus to stabilize Inorganic clasts include intraclasts, pellets and the sediment. Therefore, the Kadzielnia build-up relatively frequent ooids. Stromatoporoids and was not a reef in terms of ecology, which means corals, the main components of macrofaunal as- that it did not form a rigid structure withstanding semblages in the adjacent Kadzielnia Limestone, wave action, but was rather a reef mound (mud occur as accessory elements, which suggests that mound) developing in a calm environment. the neighbouring bioherm was not the source area Subsequent lithologies were accumulated of the bioclastic material. The bioclastic compo- basin wards on the build-up slopes. Bioclastic nents were probably derived from loose material Limestones were deposited in relatively shallow deposited on the bioherm after it ceased growing. water, which accumulated the material washed Manticoceras Limestones: This term refers to out from the build-up top. Sedimentation of the Frasnian, poorly bedded micritic limestones with Manticoceras Limestones took place after the

76 FIELD TRIP: Top Geosites of Góry Świętokrzyskie whole system was drowned and resulted in level- Limestone they form a dense network of mu- ling the sea bottom morphology. tually cross-cutting structures. Their sediments At the end of Frasnian time development of attain reddish or greenish colours that are clearly the carbonate platform was rapidly terminated visible in the complex of light coloured stro- by minor tectonic block movements that uplifted matoporoid-coral limestones. and sank the sea floor. Parts of the sea floor References with the most profound relief were often ele- vated above sea level, and their tops were sub- Łuczyński, P. 2009. Stromatoporoid growth orientation as a tool in palaeotopography: a case study from the ject to erosional shearing or even karstification Kadzielnia Quarry, Holy Cross Mountains, central (see Stop 2 – Ostrówka Quarry succession). An Poland. Acta Geologica Polonica, 59, 319–340. intensive development of neptunian dykes oc- Łuczyński, P. 2015. Kadzielnia – a Devonian carbon- curred with this time interval. The Famennian ate build-up. In: S. Skompski, A. Żylińska (Eds). succession, from the Cheiloceras Limestones to The Holy Cross Mountains– 25 journeys through the Limestone-Shale Complex, reflects a gradual earth history, p. 102‒106, University of Warsaw, deepening of the area. Faculty of Geology; Warsaw. The neptunian dykes and related structures Narkiewicz, M., Racki, G. and Wrzołek, T. 1990. Lito- (voids filled with internal sediments) occur along stratygrafia dewońskiej serii stromatoporoidowo- both margins of the Central Carbonate Platform. koralowcowej w Górach Świętokrzyskich. Kwar- Most dykes contain a rich conodont assemblage talnik Geologiczny, 34, 433–456. that allows precise dating and recognition of their Szulczewski, M. 1971. Upper Devonian conodonts, stratigraphy and facial development in the Holy multi-stage evolution, comprising subsequent ep- Cross Mts. Acta Geologica Polonica, 21, 1–129. isodes of opening and closing. The dykes were Szulczewski, M. 1981. Dewon środkowy i górny formed in several phases during the disintegration zachodniej części Gór Świętokrzyskich. In: H. and drowning of the Frasnian carbonate platform Żakowa, H. (Ed.) 1981. Przewodnik 53 Zjazdu and its transition into a Famennian–Tournaisian Polskiego Towarzystwa Geologicznego, Kielce, pelagic carbonate platform. 6–8 września 1981, p. 68–82. The Kadzielnia neptunian dykes penetrate Szulczewski, M. 1995. Depositional evolution of the downwards from the Manticoceras Limestones Holy Cross Mts. (Poland) in the Devonian and and the Famennian strata. In the Kadzielnia Carboniferous – a review. Geological Quarterly, 39, 471–488.

Stop 4. Górno Quarry Leader: Stanisław Skompski

Keywords: Frasnian allodapic limestones, carbonate platform slope GPS coordinates: 50°51’09.4”N, 20°49’13.2”E Location: Abandoned quarry in Górno village, NE of Kielce. Upper Devonian succession typical of Kostomłoty facies: transition from deep basin to slope allochthonous deposits, redeposited from the Central Carbonate Platform of Kielce region Stanisław Skompski Geological settings: Górno Quarry is located Łagów synclinorium (northern part of the Kielce in the northern limb of the Radlin Syncline – region). This Variscan syncline is composed the second-order tectonic unit within the Kielce- of the Devonian on the limbs and the Lower

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Fig. 12. General view of the eastern wall in Górno Quarry; marly limestones with numerous intercalations of allodapic beds. Photograph by Stanisław Skompski. Carboniferous (Culm facies) in the core. Its sim- posits of submarine gravity flows (Szulczewski ple form is complicated by longitudinal faults, 1968, 1971). On the eastern wall of this small bordering the Carboniferous core, which forms and abandoned quarry occur typical intraforma- the internal anticline (Czarnocki 1938; Żakowa, tional, synsedimentary breccias. On the southern Pawłowska 1961). wall, in the equivalent stratigraphic interval the Devonian succession in the region is repre- submarine slumps occur. sented by Eifelian dolomitic complex and then by different Givetian to Frasnian limestones, typical of the intra-shelf basinal environment (Szulczewski 1971; Małkowski 1981). Finally, oc- cur the nodular limestones intercalated with in- traformational breccias and allodapic limestones, well visible on the eastern wall of the quarry (Figs 12, 13). This type of facies, transitional between shallow water Kielce facies and basinal Łysogóry facies is known in the literature as Kostomłoty facies (and/or Kostomłoty Beds). It will be pre- sented more precisely in the Stop 7. Kostomłoty Beds are typical platform slope 5cm deposits, composed of marly shales or micritic and nodular limestones, intercalated with nu- merous layers of intraformational conglomerates Fig. 13. Intraformational breccias typical of Kosto- and graded limestones, interpreted as the de- młoty Beds (old quarry in the Górno village).

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The Devonian (Frasnian) succession out- Szulczewski, M. 1968. Slump structures and turbid- cropped in the Górno village illustrates the pro- ites in Upper Devonian limestones of the Holy cess of disappearance of a shallow carbonate Cross Mts. Acta Geologica Polonica, 18, 304–326. platform, developed during Middle Devonian Szulczewski, M. 1971. Upper Devonian conodonts, stratigraphy and facial development in the Holy time in central part of the Holy Cross Mountains Cross Mts. Acta Geologica Polonica, 21, 1–129. area (e.g. Szulczewski 1971, 1995; Racki 1993). Szulczewski, M. 1995. Depositional evolution of the References Holy Cross Mts. (Poland) in the Devonian and Carboniferous – a review. Kwartalnik Geologic- Czarnocki, J. 1938. Ogólna mapa geologiczna Polski, zny, 39 (4), 471–488. arkusz 4 Kielce, skala 1 : 100 000. Państwowy In- Żakowa, H., Pawłowska, J. 1961. Dolny karbon na stytut Geologiczny; Warszawa. obszarze między Radlinem i Górnem w synklino- Małkowski, K. 1981. Upper Devonian deposits at rium kielecko-łagowskim (Góry Świętokrzyskie). Górno in the Holy Cross Mts. Acta Geologica Po- [The Lower Carboniferous in the area between lonica, 31, 223–232. Radlin and Górno, in the Kielce-Łagów syncli- Racki, G. 1993. Evolution of the bank to reef complex norium (Święty Krzyż Mountains)]. Biuletyn In- in the Devonian of the Holy Cross Mountains. stytutu Geologicznego, 167, 101–166. (In Polish Acta Palaeontologica Polonica, 37, 87–182. with English extended abstract).

Stop 5. Krzemionki Opatowskie – prehistoric flint mines Leader: Stanisław Skompski

Keywords: Upper Jurassic carbonates, flint concretions, Neolithic mines GPS coordinates: 50°58’19.96”N, 21°29’28.06”E Location: Forested area 8 km north-east of Ostrowiec Świętokrzyski.

Upper Jurassic shallow water succession with horizons of striped flint concretions; underground route presenting prehistoric flint mines functioning for most of the Neolithic age and at the beginning of the Bronze Age (3900–1600 B.C.); a candidate for the UNESCO World Heritage List Stanisław Skompski

Highlights: This unique place merges the geolog- time the place has been intensively investigated ical phenomenon of occurrence of striped flints by archeologists. During nearly 2 000 years of horizons and the archeological site, which is one exploitation the striped flint excavated here was of the most valuable relics of prehistoric mining. treated as feedstock, from which different tools The numerous exploitation shafts and under- and axes were produced and distributed through ground cavities are perfectly preserved and some the Central Europe. In addition, there have been of them are available for tourists. The exploitation two other fields recognised in the neighbouring of striped flints started 3 900 years B.C. The vast villages of Borowina and Wojciechówka. exploitation field (Fig. 14), with nearly four thou- In the present guide, only geological setting sands of shafts, has been discovered by geologist is described; arecheological information is pre- Jan Samsonowicz, during cartographic investi- sented in the attached folder. gations carried out in July 1922 (Samsonowicz 1934). He informed about this discovery the Geological settings: Krzemionki Opatowskie are archeologist Stefan Krukowski and since that located within the north-eastern Mesozoic margin

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Jurassic (Oxfordian and Kimmeridgian) rocks form the succession characterised by shallow- ing upward sedimentary environment. The suc- cession traceable in the Kamienna valley started with massive ‛rocky’ unit, composed of bioher- mal limestones with sponges and microbial struc- tures. This relatively deep water unit is covered by bioclastic and reef limestones, with numerous flat colonies of corals from genera Microsolena and Thamnasteria, echinoids, brachiopods and rhodophycean algae (Roniewicz 1966). Finally, the Jurassic complex is terminated by bioclas- tic-oolitic unit (Gutowski 1998), outcropped in the nearby villages Bałtów and Skarbka. The shal- lowing of the sedimentary environment is treated as an effect of eustatic fall of sea level and progra- dation of carbonate platform from the east to the west (Matyja et al. 1989; Gutowski 1998). Flint horizons: The occurrence of 3 flint hori- zons is limited to the upper members of succes- Fig. 14. The ‘Krzemionki’ exploitation area on the sion; lowermost horizon (‘brown flints’) appeared LIDAR photograph (www.geoportal.gov.pl); abundant within the coral limestones from Bałtów, two up- exploitation shafts are visible. per horizons (‘striped flints’ and ‘chocolate flints’) are located within oolitic limestones. This part of the Holy Cross Mountains. The slightly folded of succession, generally shallow water, is char- Jurassic complexes, with general strike of 135°, acterised by cyclothemic type of deposition, with are here cut down by Kamienna river, flowing microbial laminites, oolitic intercalations and ero- from the south to the north (Fig. 15). The Upper sional surfaces in the topmost part of cyclothems,

Fig. 15. The meandering river in the souhern part of Kamienna Valley near Ćmielów. Photograph by Stanisław Skompski.

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ceans, similarly to the well known forms from the Cretaceous chalk deposits (Bromley 1967; Bromley, Ekadale 1984). The infilling of crusta- cean burrows is interpreted as a nucleation centre for formation of early diagenetic flint nodules. Relatively high permeability of deposits infilling the crustacean burrows allowed their impregna- tion by solutions with increased content of silica. The main source of silica was decomposition of clay minerals, derived from the carbonate rocks, during process of weathering in tropical or sub- tropical climate. The specific chemical context of the flint nodules formation (lowering of pH) was provided by organic particles introduced to the burrows by crustacens. Fig. 16. The section of striped flint nodule. Photograph by Stanisław Skompski. Another hypothesis concerning the nature of flint nodules has been presented by Migaszewski et al. (2006). According to these authors the flint nodules formed as a result of an episodic influx of SiO2 rich fluids and numerous processes of multi- stage direct precipitation, dissolution and recrys- tallization. However, they also considered that the process of flint nodules formation could be con- trolled by hydrothermal activity on the sea-floor. The striped flints observed in the Krzemionki mine differ from other types of f lints by presence of dark-grey/light-grey bands (Fig. 16). This fea- ture is visible only in macroscopic view, in pol- ished slabs; in the thin sections there are no dif- Fig. 17. Polygonal network of Decapoda burrows, ferences between 2 types of strips. According to impregnated by SiO . according to interpretation of 2 Migaszewski et al. (2006) the onion-skin texture Gutowski and Pieńkowski (2004). Photograph by Anna Żylińska. of nodules is caused by different level of pore im- pregnation by silica: ‘There is evidence showing interpreted as tidal flats or lagoonal deposits that the fewer and smaller pores, the darker the (Pieńkowski, Gutowski 2004). The flint horizons bands. The largest numbers of non-impregnated (Fig. 16) are regularly developed in the upper- pores are exhibited by the porcelain-like rind’. most part of cyclothems. Abundant occurrence of References flint nodules is reported only from north-eastern Bromley, R.G. 1967. Some observations on burrows Mesozoic margin of Holy Cross Mts., they are of Thalassinidean Crustacea in chalk hard-grounds. absent in the south-western margin. It means that Geological Society of Denmark Bulletin, 29, 111– flints developed only in the proximal parts of the 118. prograding carbonate platform. Nodule horizons Bromley, R.G., Ekdale, A.A. 1984. Trace fossils pres- are more or less parallel to the bedding and have ervation in flint in the European chalk. Journal of stratigraphic correlation significance. Palaeontology, 58, 298–311. Gutowski, J. 1998. Oxfordian and Kimmeridgian of the Flints origine: According to Pieńkowski and northeastern margin of the Holy Cross Mountains, Gutowski (2004) the flint nodules form a net- Central Poland. Geological Quarterly, 42, 59–72. works (Fig. 17), which correspond to the tem- Matyja, B.A., Gutowski, J., Wierzbowski, A. 1989. plate of burrows produced by Decapoda crusta- The open shelf-carbonate platform succession at

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the Oxfordian/Kimmeridgian boundary in the SW (Genesis of the Upper Oxfordian flints in Krze- margin of the Holy Cross Mts: stratigraphy, facies, mionki Opatowskie, Poland). Tomy Jurajskie, 2, and ecological implications. Acta Geologica Po- 29–36. (In Polish with English abstract). lonica, 39, 29–48. Roniewicz, E. 1966. Les madréporaires du Jurassique Migaszewski, Z.M., Gałuszka, A., Durakiewicz, T., supérieur de la bordure des Monts de Sainte-Croix, Starnawska, E. 2006. Middle Oxfordian–Lower Pologne. Acta Paleontologica Polonica, 12, 157– Kimmeridgian chert nodules in the Holy Cross Mountains, south-central Poland. Sedimentary 254. Geology, 187, 11–28. Samsonowicz, J. 1934. Objaśnienia do arkusza Opatów Pieńkowski, G., Gutowski, J. 2004. Geneza krzemieni ogólnej mapy geologicznej Polski w skali 1 : 100 górnego oksfordu w Krzemionkach Opatowskich 000. Państwowy Instytut Geologiczny, Warszawa.

Stop 6. Łysa Góra Leader: Ewa Głowniak

Keywords: Upper Cambrian quartzites, boulder field, periglacial environment GPS coordinates: 50º51’37”N 21º02’49”E Location: Platform viewpoint on the peak of Łysa Góra (at 595 m a.s.l.).

The highest range of the Holy Cross Mountains; boulder fields (gołoborze) of periglacial origin; biostratigraphic data on the Cambrian of Łysogóry Anna Żylińska (based on Żylińska 2015, 2017, supplemented) Geographical and geomorphological settings: Jeleniowskie Range, covered by fir-beech for- The Main Range of the Holy Cross Mountains, ests and protected by the Jeleniowski Landscape running from west to east for a distance of Park. The axis of this range is shifted by about 4 about 75 km, is generally composed of Cam- km to the south in relation to the axis of Łysogóry brian sandstones and quartzites that form an along the N-S-trending Łysogóry Fault. asymmetric anticlinal structure known as the Pleistocene stone runs: A noteworthy feature Łysogóry Anticline. Three orographic units of sandstone weathering in the periglacial con- are distinguished within the range: the western ditions of the Pleistocene are stone runs, known Masłowskie Range, the central Łysogóry, and in Polish as ‘gołoborze’, vast fields of sharp- the eastern Jeleniowskie Range. The eponymous edged boulders extending directly below the Łysogóry Range forms the highest part of the ridges and generally not covered by vegetation Main Range and is one of the few ridges in the (see the cover page figure). They are commonly area whose heights in relation to the surrounding located on the northern slopes of the Łysogóry valleys exceed up to 300 m. Its strongly forested and Jeleniowskie ranges. The first who rec- eastern part, covered by the historical Jodłowa ognised the nature of these boulder fields that (Engl. ‘Fir’) Forest, common composed of fir formed as a result of sandstone weathering in (Abies alba) with rarer beech (Fagus silvatica), temperate climate conditions was Łoziński with Łysica (at 612 m a.s.l.), the highest peak of (1909); he also introduced the term ‘periglacial the Holy Cross Mountains, and Łysa Góra, is facies’ into international geological literature protected by the Świętokrzyski National Park, (Łoziński 1912). whereas the western part, with Radostowa and Kraiński Grzbiet, is much lower and woodless. Toursist facilities: The platform offers a view The easternmost part of the Main Range is the towards the north, onto Chełmowa Góra Hill,

82 FIELD TRIP: Top Geosites of Góry Świętokrzyskie

Fig. 18. Cambrian trilobites from Wiśniówka Duża Quarry. A, B, D. Aphelaspis rara; reconstruction after Żylińska (2001), slightly modified; C, E. Protopeltura aciculata. Scale bars equal to 0.5 cm.

Las Serwis and the Bostowskie Range, and at the Formation (Orłowski 1975), visible in ‘kamec- same time allows for the direct observation of znice’, i.e. deep, forested ravines incised into the the boulder fields without destroying this unique slopes of Łysogóry (e.g. Salwa 2006), whereas geological phenomenon. from the north occurs the mudstone and clay- stone-dominated Klonówka Shale Formation, Geological settings: The geology of the Main which was recognized in boreholes to the north Range can be examined in the quarries on of the Main Range (Tomczykowa 1968; Żylińska Wiśniówka Hill (western tip of the range) and in 2002) but occurs also in small exposures along Wąworków (easternmost tip of the range). The the Lubrzanka gorge within the Masłowskie succession visible in these outcrops includes Range (Orłowski 1968; Żylińska 2002). thick- and medium-bedded quartzitic sandstones, associated with thick intervals of mudstones Age: The age of the rocks exposed in the Main and claystones with thin interbeds of quartz- Range has been the subject of long-term debate. itic sandstones (heteroliths), which represent The only exposures yielding trilobites are the the Wiśniówka Sandstone Formation (Orłowski Wiśniówka Duża and Wąworków quarries. Here, 1975; Żylińska 2002; Żylińska et al. 2006). From the trilobites including Aphelaspis rara (Fig. 18A, the south, this sandstone-dominated unit bounds B, D), Protopeltura aciculata (Fig. 18 C, E), with the claystone and mudstone-dominated and Olenus solitarius, occur in the Wiśniówka succession representing the Pepper Mts Shale Formation and indicate the Parabolina brevispina

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Biozone (Żylińska 2001, 2002), that is the lower Łysogóry Unit of the Holy Cross Mts. Przegląd part of the Furongian. This age has also been Geologiczny, 54, 513–520. (In Polish) indicated by acritarch assemblages from the Szczepanik, Z., Malec, J. 2017. New data on the li- Wiśniówka Quarry (Żylińska et al. 2006). The thology and acritarch biostratigraphy of Cambri- an rocks of Łysica Mt., the highest summit of the only age determinations for rocks of the Łysogóry Holy Cross Mountains. Przegląd Geologiczny, 65, Range come from mudstones and shales of the 564–575 (In Polish) underlying Pepper Mts Formation (Szczepanik, Tomczykowa, E. 1968. Stratigraphy of the Uppermost Malec 2017) and are based on acritarch as- Cambrian deposits in the Świętokrzyskie Moun- semblages that point to the transition between tains. Prace Instytutu Geologicznego, 54, 5–85. Cambrian Series 3 and the Furongian. (In Polish) Żylińska, A. 2001. Late Cambrian trilobites from the References Holy Cross Mountains, central Poland. Acta Geo- Łoziński, W. 1909. Das diluviale Nunatak des Pol- logica Polonica, 51, 333–383. nischen Mittelgebirges. Zeitschrift der Deutschen Żylińska, A. 2002. Stratigraphic and biogeograph- Geologischen Gesellschaft, Monatsberichte, 61, ic significance of Late Cambrian from Łysogóry 447–451. (Holy Cross, Mountains, central Poland). Acta Łoziński, W. 1912. Die periglaziale Facies der mecha- Geologica Polonica, 52, 217–238. Żylińska, A. 2015. Cambrian of the Main Range. In: nischen Verwitterung. Compte Rendu de la XIe ses- S. Skompski, A. Żylińska (Eds), The Holy Cross sion du Congrès Géologique International, Stock- Mountains – 25 journeys through Earth History, holm, 1910, 1039–1053. p. 59–65. University of Warsaw, Faculty of Geo- Orłowski, S. 1968. Cambrian of the Łysogóry Anticline logy; Warsaw. in the Holy Cross Mountains. Biuletyn Geologic- Żylińska, A. 2017. Stop B4. Łysa Góra. In: A. Żylińs- zny Wydziału Geologii, 10, 153–222. (In Polish) ka (Ed.), 10th Baltic Stratigraphic Conference, Orłowski, S. 1975. Cambrian and upper Precambri- Chęciny, 12–14 September, 2017, Abstracts and an lithostratigraphic units in the Holy Cross Mts. Guide Book, p. 145–147. Warszawa. Acta Geologica Polonica, 25, 431–448. (In Polish Żylińska, A., Szczepanik, Z., Salwa, S. 2006. Cambri- with English summary) an of the Holy Cross Mountains, Poland: biostra- Salwa, S. 2006. Preliminary structural-petrography tigraphy of the Wiśniówka Hill succession. Acta characteristic of phyllite from Podmąchocie in the Geologica Polonica, 56, 443–461.

Stop 7. Mogiłki Quarry Leader: Stanisław Skompski

Keywords: basin to slope carbonates, allodapic limestones, chevron faults GPS coordinates: 50º55’26.84”N 20º34’48.02”E Location: Abandoned quarry near Kostomłoty village, NE of Kielce.

Upper Devonian succession typical of Kostomłoty facies: transition from deep basin to slope allochthonous deposits, redeposited from the Central Carbonate Platform of Kielce Region Stanisław Skompski (based on Wańkiewicz, Konon 2015) Lithologic sequence and stratigraphy: Struc- limb of the Miedziana Góra Syncline, belong- turally, the beds exposed in the Mogiłki Quarry ing to the Kielce Fold Zone, developed during (Fig. 19) constitute a fragment of the southern Variscan deformation. Facially, the area rep-

84 FIELD TRIP: Top Geosites of Góry Świętokrzyskie resents the northern margin of the Kielce Region of the Holy Cross Mountains, which in the Late Devonian was characterised by a diversity of carbonate facies, reflecting the development and disappearance of a shallow carbonate platform (e.g. Szulczewski 1971, 1995; Racki 1993). This type of facies, transitional between shallow wa- ter Kielce facies and basinal Łysogóry facies is known in the literature as Kostomłoty facies (and region). In the quarry the Szydłówek Beds and Kosto- młoty Beds are outcropped (composite descrip- Fig. 19. General view of chevron faults on the eastern tion of Stop 4 – this excursion). Kostomłoty wall of the Mogiłki Quarry. Photograph by Stanisław Skompski. Beds, which were presented in limited range only in the Górno Quarry, here are developed in the most typical form. These deposits include micritic and nodular limestones, and marly shales, with numerous interbeds of clastic lime- stones with variable grain sizes (Fig. 20). The bioclastic interbeds have since long been con- sidered as deposits of submarine gravity flows with a high contribution from turbidity currents (Szulczewski 1968, 1971). Micritic and nodular limestones (Fig. 21) and marly shales formed due to slow, local sedimentation on the slopes of the carbonate platform, whereas the increasingly abundant and thicker beds of clastic limestones and intraformational carbonate breccias from the Fig. 20. Grain supported breccias with large flat upper part of the sequence were deposited at the clasts, derived from the platform slope. Photograph foot of this slope (Wańkiewicz, Konon 2015). by Aleksandra Wańkiewicz. Such a succession of deposits indicates an appar- ent withdrawal of the platform margin, drowned due to local tectonics and/or global sea level rise (see discussion in Szulczewski 1995). The most interesting tectonic structures in the quarry include minor folds occurring in cen- tral part of the eastern wall (Fig. 19). Axes of these folds are sub-parallel to the axis of the Miedziana Góra Syncline, with an orientation of about 100°. The folds are dominated by sim- ilar (chevron) folds with steeply inclined axial planes. In the fold fragments where beds of dif- ferent thicknesses occur, a transition from simi- Fig. 21. Nodular limestone. Photograph by Aleksan dra Wańkiewicz. lar to concentric folds can be observed. Cleavage is tectonic feature visible commonly in most The tectonic style typical of Kostomłoty/ of beds. The characteristic chevron folds in the Łysogóry (northern) and Kielce (southern) re- Mogiłki Quarry formed due to horizontal stress, gions is completely different. The observed dif- perpendicular to the fold axial planes (Konon ferences exemplify a phenomenon occurring in 2006a, b). the entire Holy Cross Mountains area, where

85 9th ProGEO Symposium, Chęciny, Poland, 2018 rocks significantly differing in mechanical prop- Szulczewski, M. 1968. Slump structures and turbid- erties occur adjacent to each other (Wańkiewicz, ites in Upper Devonian limestones of the Holy Konon 2015). Cross Mts. Acta Geologica Polonica, 18, 303–330. Szulczewski, M. 1971. Upper Devonian conodonts, References stratigraphy and facial development in the Holy Konon, A. 2006a. Młodopaleozoiczna ewolucja struk- Cross Mts. Acta Geologica Polonica, 21, 1–129. turalna Gór Świętokrzyskich. In: S. Skompski, A. Szulczewski, M. 1995. Depositional evolution of the Żylińska (Eds), 77 Zjazd Naukowy Polskiego To- Holy Cross Mts. (Poland) in the Devonian and warzystwa Geologicznego, Ameliówka k. Kielc, Carboniferous – a review. Geological Quarterly, 28–30 czerwca, 2006 r., materiały konferencyjne, 39, 471–488. 82–104. Konon, A. 2006b. Buckle folding in the Kielce Unit, Wańkiewicz, A., Konon, A. 2015. Sedimentation Holy Cross Mountains, central Poland. Acta Geo- and tectonics in the Devonian carbonate rocks logica Polonica, 56, 375–405. of Mogiłki Quarry. In: S. Skompski, A. Żylińska Racki, G. 1993. Evolution of the bank to reef complex (Eds), The Holy Cross Mountains – 25 journeys in the Devonian of the Holy Cross Mountains. through Earth History, p. 112–117. University of Acta Palaeontologica Polonica, 37, 87–182. Warsaw, Faculty of Geology; Warsaw.

Stop 8. Zachełmie Quarry near Zagnańsk Leader: Stanisław Skompski

Keywords: Devonian peritidal carbonates, epi-Variscan unconformity, Buntsandstein sandstones, tetrapod tracks GPS coordinates: 50º58’10.11”N 20º41’23.03”E. Location: Abandoned quarry on the western slope of Chełmowa Hill, between Zagnańsk and Zachełmie villages, about 10 km to the north of Kielce.

Epi-Variscan unconformity in the Holy Cross Mountains: Devonian dolomites of the Wojciechowice and Kowala formations, unconformably covered by Buntsandstein deposits; tidal sedimentation with record of emersion episodes Stanisław Skompski (based on Waksmundzki 2015; Kozłowski 2017) Lithologic succession and stratigraphy: Za- ern limb of the Bodzentyn Syncline are exposed cheł mie is one on the most interesting geolog- in a small area from beneath the Buntsandstein ical sites in the north-western part of the Holy cover belonging to the north-western Mesozoic Cross Mountains. It exposes variable facies of margin of the Holy Cross Mountains. Dolomites the Devonian (Eifelian), which in this local- of the Wojciechowice Formation (Eifelian) dip at ity terminate the Variscan tectonic stage; and about 40º to the NNE and reach 90 m in thick- the unconformably overlying Lower Triassic ness (Narkiewicz, Narkiewicz 2010). The strata (Buntsandstein facies) strata of the Alpine tec- include homogenous dolomicrites with bed thick- tonic stage (Fig. 22). Recently, the exposure has nesses reaching several tens of centimetres, inter- become famous for the tracks of the oldest tetra- bedded with marly dolomicrites, often with hori- pods discovered in Devonian rocks. zontal lamination. The millimetre-thick laminae have a variable clay content and due to weathering Eifelian: Devonian rocks composing the northern split into thin plates. Desiccation cracks can be limb of the Łysogóry Anticline and the south- observed on the bedding planes of the laminated

86 FIELD TRIP: Top Geosites of Góry Świętokrzyskie

Fig. 22. Variscan unconformity in Zachełmie Quarry. Buntsandstein deposits overlie the Eifelian dolomites with a large angular unconformity. Channel deposits of a braided river in the Buntsandstein facies are visible in the uppermost right of the wall. Photograph by Stanisław Skompski. beds. The cracks can be quite deep, reaching even 2015; Narkiewicz et al. 2015). Each of more than to the basal bedding planes, most probably due to a dozen cycles has a thickness from several tens the ‘inheritance’ of a once formed crack pattern of centimetres to 2 m and consistently begins in the subsequent layers of the slowly deposited, with clay-dolomitic laminites or homogenous do- periodically drying-up carbonate mud. lomites, which pass up into dolomites with dis- Part of the laminated sets is characterised continuous wavy lamination, in the upper part of- by irregular, wavy distribution of laterally thin- ten with desiccation cracks and sometimes with ning out laminae and the presence of fenestral tepee structures related to pseudomorphs after structures, which originated through microbial evaporites, visible to the naked eye. The upper processes. In the remaining beds, regular lami- surfaces of these sets are erosionally sheared or nation is resulted from carbonate deposition that contain poorly developed paleosols in the form was subtly and rhythmically ‘dissolved’ by the of nodular horizons with root traces at the top supply of terrigenous clay (Niedźwiedzki et al. (Narkiewicz, Retallack 2014). This part of the 2010). One well-exposed bed reveals pillow-like succession lacks macrofauna; only one dolomi- swellings, which are stromatolite structures that crite sample collected from the lowermost part partly mimic the polygon pattern of the under- of the sequence yielded index conodonts of the lying bed with desiccation cracks (Fig. 23). The Lower Eifelian (Narkiewicz, Narkiewicz 2015). dolomicrites generally do not record high-energy The scarcity of fossils is compensated by the events, with the exception of a single horizon sensational finds of tracks of the world’s old- with intraformational breccias, filling an ero- est tetrapod-four-limbed vertebrates capable of sional trough. The entire succession is charac- treading (Niedźwiedzki et al. 2010). So far, the terised by cyclic sedimentation (Grabowski et al. succession has yielded three horizons with these

87 9th ProGEO Symposium, Chęciny, Poland, 2018 fascinating trace fossils, all within the lower or middle part of the shallowing upward cycles, in deposits not registering emergence (Narkiewicz et al. 2015). The higher part of the Wojciechowice Forma- tion is characterised by more massive bedding, more frequent occurrence of strongly bioturbated beds and lack of microbial structures, and by the occurrence of dissecation cracks and paleosol horizons, as compared to the lower part. Marine body fossils come almost exclusively from this part of the succession (the only exception are the oldest conodonts from beds preceding the first horizon with tetrapod tracks); the fossils, rec- ognised in thin sections and in the residue from dissolved rock samples, include conodonts, echi- noderms, bryozoans, scolecodonts, bivalves and gastropods. The boundary with the overlying Kowala For- mation is marked by a distinct lithological change – the dolomicrites are replaced by dolosparites, and amphipores and tabular stromatoporoids ap- pear in a few biostromal horizons. The medium – and thick-bedded deposits are either homogenous or indistinctly laminated (Narkiewicz, Narkiewicz 2010; Niedźwiedzki et al. 2010). Fig. 23. Stromatolites mimicking the polygonal pat- Very well preserved sedimentary structures tern of desiccation cracks in the underlying bed; and the presence of clasts of earlier lithified do- Eifelian, Zachełmie Quarry, Holy Cross Mountains. lomitic sediments indicate a very early origin for Photograph by Anna Żylińska. the dolomites of the Wojciechowice Formation et al. 2015). The depositional processes were cy- (Narkiewicz et al. 2015). clic, and proceeded according to a rhythm gen- During Eifelian time, the Łysogóry Region erated by astronomical factors (Grabowski et with the Zachełmie area was part of a vast, al. 2015). Salinity exceeding normal levels and rather flat, shallow-marine carbonate platform, frequent emergent intervals did not favour the extending from the area of present-day Moravia presence of stenohaline fauna on the sea floor. to the Holy Cross Mountains, and located on In turn, the upper part of the Wojciechowice the Euramerican (Laurussian) shelf. The lower Formation and the Kowala Formation originated part of the Wojciechowice Formation exposed in in a less restrictive setting with a higher contri- the quarry, with the tetrapod tracks, in particu- bution from waters with normal salinity levels, lar was formed in an extremely shallow marine which favoured the appearance of benthic fauna. setting. At a large distance from land, carbon- ate muds with a small admixture of terrigenous Buntsandstein: Close to the quarry entrance, silt of eolian origin were deposited in calm con- in the eastern wall, is exposed a text-book ex- ditions only sporadically interrupted by storm ample of a contact between two tectonic stages, events (intraformational breccias probably origi- the Variscan and Alpine stages (Fig. 24). A na- nated during storm events), in an area covered by ture monument was established here in 1987. lagoons with depths probably not exceeding sev- Eifelian dolomites are covered with a large angu- eral metres, surrounded by flat islands that were lar unconformity by the Buntsandstein deposits. scantily covered by early land plants (Narkiewicz The Devonian rocks were folded after the early

88 FIELD TRIP: Top Geosites of Góry Świętokrzyskie

Fig. 24. Sedimentary environments of the Buntsandstein in Zachełmie Quarry (after Waksmundzki 2015).

Carboniferous during Variscan deformation, in of the Buntsandstein succession belongs to the which, among other structures, the Łysogóry Zagnańsk Formation (Kuleta et al. 2006). It in- Anticline and the Bodzentyn Syncline were cludes slightly lighter coloured, compared to the formed. The flat-lying beds of the Buntsandstein underlying beds, medium- to thick-bedded quartz represent the lowermost part of the Alpine stage. sandstones which infill channels that erosionally The top of the dolomites is uneven and shaped cut into the sand-mud deposits. Channel soles by karst and fluvial processes. Depressions in sometimes contain accumulations of flat clay its surface are filled with strongly lithified do- intraclasts or dolomite clasts, which represent lomite breccias with clasts reaching up to 30 cm residual lags. The sandstones reveal large-scale in size. No sorting and grading are observed, trough and tabular cross-bedding and represent resulting in a chaotic distribution of the clasts. channel facies of braided rivers that incised the The clasts occur in a red, calcareous-ferruginous floodplains (Fig. 24; cf. Szulczewski 1995). matrix with admixture of detrital quartz and sub- Due to the lack of precise biostratigraphic ordinate muscovite. Several metres thick, easily tools, the age of the Buntsandstein deposits, weathered, red, thin-bedded, fine-grained quartz especially their lowermost part, is a matter of sandstones with interbeds of quartz mudstones controversy. Magnetostratigraphic data indicate occur above. Apart from quartz, they contain an Early Triassic age (Nawrocki et al. 2003), fine muscovite and subordinate quantities of ka- whereas conchostracans point to the late Permian olinitised feldspars. These rocks overlie the brec- (Ptaszyński, Niedźwiedzki 2004; see discussion cias or lie directly on Eifelian dolomites. Both the in Becker 2014). breccias and the sandstones are assigned to the Jaworzna Formation (Kuleta et al. 2006). This References part of the Buntsandstein succession was formed Grabowski, J., Narkiewicz, M., De Vleeschouwer, D. as a result of interfingering between deposits of 2015. Forcing factors of the magnetic suscepti- alluvial fans (the so-called ‘sheet-flood’ deposits) bility signal in lagoonal and subtidal deposition- and fine sediments of a river floodplain environ- al cycles from the Zachełmie section (Eifelian, ment (Szulczewski 1995). The uppermost part Holy Cross Mountains, Poland). In: A.C. da Silva,

89 9th ProGEO Symposium, Chęciny, Poland, 2018

M. Whalen, J. Hladil, L. Chadimova, D. Chen, Narkiewicz, K., Narkiewicz, M. 2015. The age of the S. Spassov, F. Boulvain and X. De Vleeschouw- oldest tetrapod tracks from Zachełmie, Poland. er (Eds), Magnetic Susceptibility Application: A Lethaia, 48, 10–12. Window onto Ancient Environments and Climatic Narkiewicz, M., Retallack, G.J. 2014. Dolomitic pa- Variations. Geological Society of London Special leosols in the lagoonal tetrapod track-bearing suc- Publications, 414, p. 225–244. cession of the Holy Cross Mountains (Middle De- Kozłowski, W. 2017. Stop A1. Zachełmie Quarry vonian, Poland). Sedimentary Geology, 299, 74–87. near Zagnańsk. In: A. Żylińska (Ed.), 10th Baltic Nawrocki, J., Kuleta, M., Zbroja, S. 2003. Buntsand- Stratigraphic Conference, Chęciny, 12–14 Sep- stein magnetostratigraphy from the northern part of tember, 2017, Abstracts and Guide Book, p. 108– 110. Warszawa. the Holy Cross Mountains. Geological Quarterly, Kuleta, M., Zbroja, S., Gągol, J., Niedźwiedzki, G., 47, 253–260. Ptaszyński, T., Studencka, J. 2006. Excursion W2. Niedźwiedzki, G., Szrek, P., Narkiewicz, K., Nark- Terrestrial Buntsandstein sediments in the northern iewicz, M. and Ahlberg, P.E. 2010. Tetrapod track- Mesozoic margin of the Holy Cross Mountains: ways from the early Middle Devonian period of sedimentary conditions, vertebrate tracks, resour- Poland. Nature, 463 (7277), 43–48. ces. In: S. Skompski, A. Żylińska (Eds), 77 Zjazd Ptaszyński, T., Niedźwiedzki, G. 2004. Conchostraca Naukowy Polskiego Towarzystwa Geologicznego, from the lowermost Buntsandstein of Zachełmie, Ameliówka koło Kielc, 28–30 czerwca, 2006, Ma- Holy Cross Mountains. Przegląd Geologiczny, 52, teriały Konferencyjne, p. 174–178. (In Polish). 1151–1155. (In Polish). Narkiewicz, M., Grabowski, J., Narkiewicz, K., Nied- Szulczewski, M. 1995. Zachełmie quarry. In: S. źwiedzki, G., Retallack, G.J., Szrek, P. and De Skompski (Ed.), Guide to Excursion A2. XIII In- Vleeschouwer, D. 2015. Palaeoenvironments of the ternational Congress on the Carboniferous –Perm- Eifelian dolomites with earliest tetrapod trackways ian, Kraków, Poland, August 28 – September 2, (Holy Cross Mountains, Poland). Palaeogeography, p. 32–33. Palaeoclimatology, Palaeoecology, 420, 173–192. Narkiewicz, K., Narkiewicz, M. 2010. Mid Devonian Waksmundzki, B. 2015. Tracks of Devonian tetra- carbonate platform development in the Holy Cross pods and the Variscan unconformity in Zachełmie Mts. Area (central Poland): new constraints from Quarry. In: S. Skompski, A. Żylińska (Eds), The the conodont Bipennatus fauna. Neues Jahrbuch Holy Cross Mountains – 25 journeys through für Geologie und Paläontologie, Abhandlungen, Earth History, p. 132–136. University of Warsaw, 255 (3), 287–300. Faculty of Geology; Warsaw.

Stop 9. Tumlin Quarry Leader: Ewa Głowniak

Keywords: Buntsandstein, aeolian sedimentation, Polish-Danish Trough GPS coordinates: 50°58’06.8”N 20°34’36.0”E. Location: Large quarry situated in the Tumlin village, near the road Kielce-Piotrków Trybunalski.

Eolian sediments in the Lower Triassic succession of the Mesozoic margin of the Holy Cross Mountains Stanisław Skompski Lithologic sequence and stratigraphy: Medium Sandstone, in formal classification as Tumlin Beds and fine-grained, moderately sorted ferrugine- (according to Kuleta, Zbroja 2006), corresponding ous sandstones, traditionally classified as Tumlin to the Baltic Formation of Polish Lowlands. The

90 FIELD TRIP: Top Geosites of Góry Świętokrzyskie

Fig. 25. Idealized blokdiagram showing gross internal geometry of the Tumlin Sandstone (after Gradziński et al. 1979). MB – main bounding surface; AB – additional bounding surface; AER – eolian ripples; WR – wave ripples; MC – mud cracks; WTL – water-level terraces; SS – lens of structurless sandstone; SC – scoop-like termination. sandstones consist mainly of quartz; feldspars and As it was indicated by the presence of Bunt- micas occur as accessory grains. sandstein sediments in other quarries, during The Lower Triassic sandstone complex (typ- Early Triassic time the sandstone deposits most ical Buntsandstein facies) in the margin of the probably covered the whole Variscan area of the Holy Cross Mts. is usually developed as fuvial Holy Cross Mountains. deposits. The Tumlin Sandstone, outcropped in References the Tumlin and neighbouring quarries, represents another facies, characteristic only for this area. Gradziński, R. 1992. Deep blowout depressions in the aeolian Tumlin Sandstone (Lower Triassic) of the According to Gradziński et al. (1979), Gradziński Holy Cross Mountains, central Poland. Sedimen- (1992) the presented complex is interpreted as eo- tary Geology, 81, 231–242. lian sediments, with 2 different sedimentary as- Gradziński, R., Uchman, A. 1994. Trace fossils from sociations: dune and interdune settings (Fig. 25). interdune deposits – an example from the Lower Dune association features: Large-scale-cross- Triassic aeolian Tumlin Sandstone, central Po- stratification with giant scoop-like bottom sur- land. Palaeogeography, Palaeoclimatology, Palae- faces and thickness of individual beds of several oecology, 108, 121–138. Gradziński, R., Gągol, J., Ślączka, A. 1979. The Tum- meters, relatively large dips of the depositional lin Sandstone (Holy Cross Mts., Central Poland): surfaces, presence of lenses of massive sands, Lower Triassic deposits of aeolian dunes and inter- resulting from avalanche-like sand deposition on dune areas. Acta Geologica Polonica, 29, 151–176. the leeward dune slopes. Kuleta, M., Zbroja, S. 2006. Wczesny etap rozwo- Interdune association features: The presence ju pokrywy permsko-mezozoicznej w Górach of flat-laminated sand and siltstone deposits, Swiętokrzyskich. In: S. Skompski and A. Żylińska (Eds), 77 Zjazd Naukowy Polskiego Towarzystwa presence of dessication cracks, mud curls, rip- Geologicznego, Ameliówka koło Kielc, 28–30 ple marks and raindrop impressions. Gradziński czerwca, 2006, Materiały Konferencyjne, p. 105– and Uchman (1994) and Ptaszyński and Niedź- 125. (In Polish). wiedzki (2004) described from this association Ptaszyński, T., Niedźwiedzki, G. 2004. Late Perm- several vertebrate (Chirotheridae group of ich- ian vertebrate tracks from the Tumlin Sandstone, nofossils) and invertebrate (Diplocraterion and Holy Cross Mountains, Poland. Acta Palaeonto- Planolites) tracks. logica Polonica, 49, 289–320.

91 Warszawa 2018 ISBN 978-83-945216-5-3