International Conference ProGEO WG Northern Europe
GEOLOGICAL HERITAGE – BRIDGE JOINING COUNTRIES GEOLOGINIS PAVELDAS – TILTAS JUNGIANTIS ŠALIS
Papil÷, Venta Regional park September 10–12, 2008
CONFERENCE MATERIALS EXCURSION GUIDE
Geological Heritage – Bridge joining countries = Geologinis paveldas – tiltas jungiantis šalis: International Conference ProGEO WG Northern Europe, Papil÷, Venta Regional Park, September 10–12, 2008: Conference materials, Excursion Guide / Compiled by: J. Čyžien÷, J. Satkūnas, A. Nicius, J. Bitinas; Editor: J. Satkūnas; Lithuanian Geological Survey. – Vilnius: LGT, 2008. – 46 p: iliustr. – Bibliogr. str. gale
ORGANISERS State Service of Protected Areas Venta Regional Park Polish Geological Institute Environment, Geology and Meteorology Agency Lithuanian Geological Survey
ORGANISING COMMITTEE Vidas Bezaras, State Service of Protected Areas, Lithuania Apolinaras Nicius, Venta Regional Park Wlodzimierz Mizerski, Polish Geological Institute Uldis Nulle, Latvian Environment, Geology and Meteorology Agency Jonas Satkūnas, Lithuanian Geological Survey
TOPICS OF THE CONFERENCE • Jurassic geoheritage in Baltic Region and Poland, network of Jurassic parks; • Cross border geological heritage and eco tourism; • Geodiversity – holistic value; • Geoparks; • History of geological investigations – cultural heritage.
PROGRAMME OF THE CONFERENCE September 10, Wednesday 8:00 departure from Vilnius to Papil÷ Geological and cultural sites of vicinities of Papil÷ Evening lectures: Prof. dr. hab. Marek Graniczny “From Augustow Canal to Venta: Polish Lithuanian cross border geoenvironmental cooperation” Apolinaras Nicius & Andrius Almanis “Welcome to Venta Regional Park”
September 11, Thursday Field trip to Venta Regional Park and it‘s vicinities Evening lectures: Geological heritage of Latvia Jurassic geological heritage in Baltic region
September 12, Friday Lectures 9:00 9:45 Isabella Ploch “Tracking dinosaurs” 9:45 10:15 Dr. Jonas Satkūnas “Value of geological heritage” 10:15 11:30 Discussions and summing up of results of the Conference Press Conference 16:00 Arrival to Vilnius
VENUE OF THE SEMINAR AND ACCOMMODATION FOR PARTICIPANTS “Algirdo Martyšiaus kaimo turizmo sodyba“ Nepriklausomyb÷s Str. 96, Papil÷ Phone: + 370 69845548
Published by Lithuanian Geological Survey Compiled by: J. Čyžien÷, J. Satkūnas, A. Nicius, J. Bitinas Editor: J. Satkūnas Layout and cover design: I. Virbickien÷
Circulation: 50 copies
© Lietuvos geologijos tarnyba
International Conference GEOLOGICAL HERITAGE – BRIDGE JOINING COUNTRIES CONFERENCE MATERIALS
CONTENTS
CONFERENCE MATERIALS ...... 4
STATE OF ART OF INVENTORY OF GEOTOPES AND GEOCONSERVATION IN LITHUANIA Donatas Pupienis, Vidas Mikul÷nas, Giedrius Mikalauskas & Jonas Satkūnas ...... 5
GEODIVERSITY AND GEOLOGICAL HERITAGE – POTENTIAL FOR GEOTOURISM OF NORTHERN POLAND, LITHUANIA, LATVIA AND ESTONIA Jonas Satkūnas, Marek Graniczny, Szymon Uscinowicz, Grazyna Miotk Szpiganowicz, Dace Ozola, Uldis Nulle, Krista Täht Kok . . 6
FROM AUGUSTOW CANAL TO VENTA: POLISH LITHUANIAN CROSS BORDER GEOINVERONMENTAL COOPERATION Marek Graniczny, Zbigniew Kowalski, Monika Krzeczyńska, Donatas Pupienis, Jonas Satkūnas ...... 10
DINOSAUR TRACKS IN JURASSIC DEPOSITS IN POLAND Włodzimierz Mizerski ...... 11
GEOLOGICAL HERITAGE – BRIDGE JOINING COUNTRIES EXCURSION GUIDE Compiled by: Jolanta Čyžien÷, Jonas Satkūnas, Apolinaras Nicius, Jaunutis Bitinas ...... 15
LOCATION OF EXCURSION SITES ...... 16
GEOLOGICAL HERITAGE OF VENTA RIVER VALLEY, LITHUANIA Jonas Satkūnas & Apolinaras Nicius ...... 17
JURAKALNIS OUTCROP ...... 26
ŠALTIŠKIAI QUARRY ...... 28
KARPöNAI QUARRY ...... 29
ŽAGARö DOLOMITE DEVONIAN OUTCROPS, ŽAGARö REGIONAL PARK ...... 31
ŽAGARö ESKER, ŽAGARö REGIONAL PARK ...... 36
GEOLOGICAL HERITAGE OF VENTA RIVER VALLEY IN LATVIA Uldis Nulle & Atis Mūrnieks ...... 37
GEOLOGICAL HERITAGE OF LATVIA Atis Mūrnieks ...... 40
DEVONIAN DOLOCRETES AT THE MOUTH OF THE RIVER LĒTĪŽA Ăirts Stinkulis ...... 44
FOR NOTES ...... 46
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CONFERENCE MATER IALS
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STATE OF ART OF INVENTORY OF GEOTOPES AND GEOCONSERVATION IN LITHUANIA
Donatas Pupienis 1, Vidas Mikul÷nas 1, Giedrius Mikalauskas 2 & Jonas Satkūnas 1, 1Lithuanian Geological Survey, 2 State Service of Protected Areas
Interest in geological heritage during last years in Lithuania has been increasing especially in protected areas, which occupy approximately 12% of territory of Lithuania. The list of protected objects of nature heritage of Republic of Lithuania currently contains 154 geological, 34 hydrogeological, 32 geomorphological and 22 hydrographical sites, totaly 242 objects of inanimate nature. However, the collection of geological information, investigations of particular geological and geomorphological features is the main duty of geoscientists.
The Data Base of GEOTOPES, maintained at Lithuanian Geological Survey currently (2008 05) contains data on 431 geotope. The geotopes include the above mentioned sites protected by law and other sites, with particular or very characteristic geological geomorphological features, that generaly are called geotopes. The information about geotopes includes much of all available geological, historical, archaelogical data, that are accessible via internet.
Protected areas (green) and location of Geotopes (dots) in Lithuania
The number of information stands, geological trails, special publications is constantly increasing, witnessing growing understanding of value of geological heritage and its integration in tourism and economical development plans. Geological heritage also serves for development international cooperation especially in cross border areas (e.g. Polish Lithuanian project GAJA).
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GEODIVERSITY AND GEOLOGICAL HERITAGE – POTENTIAL FOR GEOTOURISM OF NORTHERN POLAND, LITHUANIA, LATVIA AND ESTONIA
Jonas Satkūnas, Marek Graniczny, Szymon Uscinowicz, Grazyna Miotk Szpiganowicz, Dace Ozola, Uldis Nulle, Krista Täht Kok
Increasing number of geoparks (c.f. Global Geoparks Network), educational trails, different other geotourism products (The Stones…, 2005; Vulkaneifel…, 2007; Geotourism..., 2008; Koźma J., Kupetz M., 2008; The Geological landscape…, 2008) over the world witness growing interest of broader society in geological landscapes and natural diversity. In this context the regional geodiversity is an essential framework for identification of most valuable features of geological heritage and better development of research, geotourism and related activities (Wimbledon et al., 1998; Słomka, 2008).
Akmen÷s stone. Tytuv÷nai Regional Park, Lithuania (photo J. Satkūnas)
Number recent cross border projects (e.g. Graniczny et al., 2007a, 2007b, 2008; International Conference…, 2006, 2007; Geological heritage…, 2007; Estijos…, 2006), ProGEO activities (Pupienis et al., 2007; Satkunas et al., 2007) national geotopes inventories (e.g. Satkunas, Pupienis, Lazauskiene, 2007) etc. enable to identify and better characterize rich geodiversity and related geoheritage of the Easter Baltic region including Northern Poland, Lithuania, Latvia and Estonia (Jurys et al., 2008; Kaali…, 2007; Panga…, 2007; Słomka et al., 2006; Suuroja, 2006.)
Geodiversity of the area can be generally characterized by several criteria. From the point of view of stratigraphy, the geosites of the area display sedimentary history of all geological periods starting with Palaeozoic (e.g. Cambrian Devonian geosites of Estonia and Latvia, Devonian – Neogene geosites of Lithuania, Neogene and Pleistocene and Holocene geosites in Poland) and ending with Holocene. Especially rich is geodiversity of Quaternary period containing number of stratigraphic geosites (e.g. lower boundary of Quaternary system in Lithuania, stratotypes of all known ice free intervals – interglacials and interstadials, scattered in all region), variety of glacial and postglacial landforms (drumlins, eskers, kames, boulder fields and giant single erratics, terminal moraines, thermokarstic holes, subglacial channel valleys and erosional river valleys etc.) of marginal, insular and other formations. Number of impressive geosites deals with: coastal processes – e.g. Estonian glint, coastal cliffs of Poland, Kaliningrad region, accumulative spits (Vistula, Hel, etc.) sometimes with high moving dunes (Curonian and Leba), karstic phenomena (Lithuania, Latvia, Estonia), river erosion valleys and waterfalls, meteoritic craters (Estonia) and other elements of geodiversity.
Lists of the most representative geosites of nations of Northern Europe are under compilation and are accessible through the ProGEO ( http://www.progeo.se/ ) and other websites, publications.
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Marginal moraines. Suwalki landscape park (photo M. Graniczny)
The geodiversity and geoheritage of the area under consideration provide good prerequisites for development of geotouristic and educational scientific routes in the Eastern Baltic region and possibly for development of geoparks (Guidelines…, 2006).
Triassic clay quarry in Šaltiškiai, NW Lithuania (photo A. Nicius)
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Jagala waterfall – the mightiest in Baltic region (photo K. Täht Kok)
Curonian Spit, Lithuania (photo A. Bitinas)
On the basis of available information over national borders, several representative geoheritage theme roads for science, education, tourism and management tentatively could be proposed: ● Changing Baltic Coasts: Lagoons, Barriers and Cliffs; ● Journey through Geological Time Scale: from Paleozoic to Holocene; ● Climate and Environments through Quaternary; ● Glacial History of Landscapes; ● Eyes of Earth and Sky: meteoritic impacts and karstic phenomena;
It has to be emphasized that the proposed thematic roads are tentative and all these roads can be combined in different ways and geoheritage can be displayed in integrated way or new themes can be formulated under the topical request or interest. However, at any rate, the knowledge on geodiversity and geoheritage over the borders is of great value for tourism and education.
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REFERENCES
Estijos geologija, kraštovaizdžiai, gamtinis ir kultūrinis paveldas – unikalūs bruožai ir bendros sąsajos Baltijos regiono kontekste: mokomasis lauko seminaras, 2006 m. geguž÷s 4–6 d. / aprašymą pareng÷ Satkūnas J., Čyžien÷ J.; Lietuvos geologijos tarnyba. – Vilnius: LGT, 2006 Geological heritage of Venta River Valley: Lithuanian Latvian field seminar, April 4–6, 2007: Field Trip Guide / Editor Satkūnas J.; Compiled by: Bitinas J., Čyžien÷ J., Damušyt÷ A., Grigien÷ A., Jusien÷ A., Mažeika J., Nicius A., Satkūnas J.; Lithuanian Geological Survey. – Vilnius : LGT, 2007. – 38 p. The Geological Landcape of Emilia Romagna. – 1:250 000 / Servizio Geologico, Sismico e dei Suoli; Servizio Tecnico Bacini degli Affluenti del Po. Bertolini G., Cazzoli M. A., Centineo M. C., Cibin U., Martini A. – 2008 Geotourism Resources of Iran / Geological Survey of Iran. – 22 p. 2008 Global Geoparks Network / UNESCO // http://www.unesco.org/science/earth Graniczny M., Czarnogorska M., Grigien÷ A., Jusien÷ A., Satkūnas J., Pupienis D., Kmita J., Kowalski Z. Geological and geomorphological heritage of Polish Lithuanian cross border area and its integration for sustainable development // Italo Maltese Workshop on Integration of the geomorphological environment and cultural heritage for tourism promotion and hazard prevention, Malta, 24–27 April 2007 : Abstracts and Field trip guide. Modena, 2007. – P. 41–42 Graniczny M., Mizerski W., Nicius A., Satkūnas J. Jurajskie dziedzictwo geologiczne Litwy: Polski // Przegląd Geologiczny. – 2007. – Vol. 55. – Nr. 3. – P. 224–225 Graniczny M., Kowalski Z., Czarnogórska M., Krzeczyńska M., Pupienis D., Satkūnas J. Projected Geopark Yotvings – Polish Lithuanian cross border area // Przegląd GeologiczNY. – 2008. – vol. 56, No. 8/1. – P. 611–613. Guidelines and Criteria for National Geoparks seeking UNESCO’s assistance to join the Global Geoparks Network // Episodes. – 2006. – Vol. 29, No. 2. – P.115– 118 International Conference "Geoheritage for Sustainable Development", May 27–30, 2006, Druskininkai, Lithuania: Volume of Abstracts and Excursion Guide / Lithuanian Geological Survey. – Vilnius: LGT, 2006 International Conference "Geoheritage and International Borders – Perspective for Sustainable Development", June 11–12, 2007, Augustów, Poland: Volume of Abstracts. – Augustów: Polish Geological Institute, 2007 Jurys L., Kaulbarsz D., Koszka Maroń D., Zaleszkiewicz L. Baltic cliffs and much more // Przegląd Geologiczny. – 2008. – Vol. 56, No. 8/1. – P. 595–603 Kaali Visitor Centre, 2007 // http://kaalitrahter.ee [leaflet] Koźma J., Kupetz M. The transboundary Geopark Muskau Arch (Geopark Łuk MuŜakowa, Geopark Muskauer Faltenbogen) // Przegląd Geologiczny. – 2008. – Vol. 56, No. 8/1. – P. 692–698 Panga [Mustjala] Cliff – a wonderful object of primitive nature. 2007 [leaflet] Pupienis D., Graniczny M., Czarnogorska M., Grigien÷ A., Jusien÷ A., Satkūnas J., Kowalski Z. Integration of geological and geomorphological heritage for sustainable development: experiernce from the Polish Lithuanian cross border area // Geodiversity and Geology of Nature Heritage: ProGEO Northern European Working Group International Conference, Vaasa, Finland, May 20 – May 24, 2007 : Abstracts. – Kokkola, 2007. – P. 36 Satkūnas J., Čyžien÷ J., Pupienis D., Jusien÷ A., Ozola D., Lācis A., Nulle U., Stinkulis Ă., Markots A., Nicius A. Geological heritage of Venta river valley (Lithuania and Latvia) // Geodiversity and Geology of Nature Heritage: ProGEO Northern European Working Group International Conference, Vaasa, Finland, May 20 – May 24, 2007: Abstracts. – Kokkola, 2007. – P. 37 Satkūnas J., Pupienis D., Lazauskien÷ J. Inventory of Geotopes and development of geoconservation in Lithuania // Geo Pomerania Szczecin 2007: Geology cross bordering the Western and Eastern European Platform: Joint Meeting PTG DGG, Monday, 24 th to Wednesday, 26 th September 2007, University of Szczecin, Poland: Abstract Volume. – Hannover, 2007. – P. 240 Słomka T. Geodiversity of Poland // Przegląd Geologiczny. – 2008. – Vol. 56, No. 8/1. – P.584 587 Słomka T., Kicińska Świderska A., Doktor M., Joniec A. et al. Katalog obiektów geoturystycznych w Polsce / Redaktorzy T. Słomka, M. Doktor, A. Joniec, A. Kicińska Świderska; Ministerstwo Środowiska. – Kraków, 2006 Suuroja K. Baltic Klint in North Estonia as a Symbol of Estonian Nature / Eds.: Miidel A., Raukas A. – Tallin, 2006 The Stones of Bologna: Lithology of a city. – 1:3:500 / Servizio Geologico, Sismico e dei Suoli. Regione Emilia Romagna; Dipartimento di Scienze della Terra e Geologico ambientali. Universita degli Studi di Bologna; Dipartimento di Filologia Classica e Medievale. Universita degli Studi di Bologna – Florence, Italy. – 2005 Vulkaneifel Magazine / Natur und Geopark Vulkaneifel GmbH. – 2007 Wimbledon et al 1998. A first attempt at a geosites framework for Europe – an IUGS initiative to support recognition of world heritage and European geodiversity // Geologica Balcanica. – Vol. 28. – No. 3–4. – P. 5–32
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FROM AUGUSTOW CANAL TO VENTA: POLISH LITHUANIAN CROSS BORDER GEOENVIRONMENTAL COOPERATION
Marek Graniczny 1, Zbigniew Kowalski 1, Monika Krzeczyńska 1,Włodzimierz Mizerski 1, Donatas Pupienis 2, Jonas Satkunas 2 1Polish Geological Institute, 2Lithuanian Geological Survey
The Polish Lithuanian cross border area occupies very valuable and spectacular complexes of landscape formed during the last (Weichselian, Vistulian) continental Fennoscandinavian glaciation. This is a classical area with marginal moraines, glaciolacustrine and outwash plains, ravines, glacial depressions and valleys, kames, eskers, and erratic boulder fields. It is a pattern of classical glacial hilly landscape however resulting from interaction of its geological structure, neotectonics, the palaeorelief of the pre Quaternary basement. Geomorphology of the area under discussion demonstrates erosional and depositional processes of ice sheets, subsequent erosional and depositional action of the melt waters. The area is also characterised by high values of archeological and historical heritage and number of nature areas protected by law.
This region due to its exceptional beauty, natural and environmental advantages and almost no injury by human activity is very promising for geotourism development.
Polish Geological Institute (the lead partner) and Lithuanian Geological Survey have completed in 2007 the INTERREGIII/A project No. 2005/041 “Elaboration of geoenvironmental assumptions for ‘Geopark Yotvings’ in the cross border Polish Lithuanian area” – GAJA.
Augustow canal (photo I. Virbickien÷)
The project aimed to promote better understanding of geological heritage and to strengthen trans boundary co operation and promote initiatives in application of elements of the geological heritage in sustainable develop ment (geotourism). Environmental geological data are of particular importance for economical development of cross border areas, however joint genvironmental studies of neighboring countries yet are very few.
The concept of the Geotouristic Map of the project area was elaborated. The map includes DTM and Landsat satellite data at the scale scale 1:200 000. The explanatory notes describes in two languages – Polish and Lithuanian. Map will cover also: four touristic routes (two in Lithuania along Nemunas river and in the Vištytis regional park) and two in Poland (eastern bank of Hancza river and along the Augustow channel); landuse (on the basis of the satellite data analysis), main roads, railways, national boundaries, main cities, lakes and rivers; geotopes, view points; protected areas etc. Panoramic views will be situated on map corners (NE to SW, SW to NE). Separately photos of 14 geotopes and their descriptions are located on the map: Rospuda valley, Smolniki view point, Cisowa Hill, Hancza Lake, Castle Hill, Bachanowo boulder field, Wigry Kame, Dunojus Hill, Raigardas Valley, Vištytis boulder, Šilo spring, Vilkas spring, Velnio boulder and Snaigupeles outcrop.
It is planned the next stage of Polish–Lithuanian geoenvironmental cooperation will deal with Jurassic geoheritage.
REFERENCE
Graniczy M., Mizerski W., Nicius A., Satkūnas J. Jurajskie dziedzictwo geologiczne Litwy i Polski // Przegląd Geologiczny. – 2007. – Vol. 55, Nr. 3. – P. 224–225
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DINOSAUR TRACKS IN JURASSIC DEPOSITS IN POLAND
Włodzimierz Mizerski, Polish Geological Institute
Introduction
Polish dinosaurs were first recognized in 1959, when their fossil footprints had been discovered by Dr. Władysław Karaszewski (1911–2003) in Gliniany Las site, 20 kilometres northwest from Kielce. Doctor Karaszewski, one of the oldest and most experienced staff members of the Polish Geological Institute in Warsaw, has been already known from many important discoveries. Only a good field naturalist could spot dinosaur tracks on two ordinary rock fragments, especially that nobody expected them to occur there.
For may decades it has been claimed that the lack of dinosaur remains from Poland is due to the fact that the country’s territory was submerged throughout the whole Dinosaur Era. This claim is, however, only partly true. During the geological history of Central Europe, seas many times encroached onto the land, but also often receded from here. It has been also the case in many other parts of the world known for dinosaur finds; they also were once dry land, or were under the sea.
The Palaeozoic core of the Holy Cross Mountains is surrounded from the north by outcrops of younger sediments, dating from the Mesozoic era. They contain footprints of Jurassic dinosaurs, telling the story of a real “Holy Cross Jurassic Park”, extending from the northern outskirts of Kielce, as far as near Radom.
Despite intensive geological and palaeontological research carried out in Poland, until recently no skeletal remains of dinosaurs have been found. One of the closest hits come from a clay mine in Krasiejów in the Opole Silesia (southern Poland). Only in 2003, Professor Jerzy Dzik (Institute of Palaeobiology Polish Academy of Sciences) described a Late Triassic dinosauromorph Silesaurus opolensis (a primitive relative of dinosaurs, resembling the earliest ornithischians, such as Pisanosaurus). At the same time, a young dinosaur tracker, Grzegorz Niedźwiedzki, discovered fragmentary bone remains of a small dinosaur in the long known Early Jurassic track locality of Sołtyków in the Holy Cross Mountains.
Even more recently, dinosaur skeletal remains have been also discovered in the Late Triassic strata of Poland. However, due to the scarcity of bone fossils, it is the footprint record that remains the main source of our knowledge about the Polish dinosaurs.
You are invited to join us in a journey to discover the past rulers of the Earth, almost literally following their footsteps. The fossil sites and exhibits belong to a network of the Central European Dinosaur Park, part of the Trans European Dinosaur Safari, following dinosaur trails from Portugal and Spain through France, Switzerland and Germany to Italy and Slovenia. In many field localities you can find additional detailed information on bilingual explanatory stands. We also provide GPS coordinates to help you find the relevant tracks in situ. Many fine specimens can be now seen in museums, both in the Holy Cross Mountains area, and in Warsaw.
Dinosaurs and their footprints
Dinosaurs (Dinosauria) are a group of archosaurs (ruling reptiles), together with crocodiles, extinct flying reptiles (pterosaurs), as well as some early Triassic groups. Dinosaurs are known since the middle of the Triassic Period, the first period of the Mesozoic Era; thus they evolved almost simultaneously with mammals. They diversified rapidly at the Triassic Jurassic boundary and during the following Jurassic period. They ruled the Earth for about 150 million years — till the end of the Cretaceous period. The major evolutionary lines of dinosaurs are theropods, sauropodomorphs (the two groups are collectively known as saurischians, or lizard hipped dinosaurs) and ornithischians (bird hippeddinosaurs). Theropods were mostly carnivorous, the other groups were exclusively plant eaters. Many hundreds of dinosaur species have been described; some reached 50 metres in length and weighed up to a hundred tons, while others were less than a metre long.
Footprints provide unique knowledge about dinosaur locomotion and mode of life, about their ecosystems and evolution. Fossil tracks help us reveal the evolutionary history of dinosaurs and their distribution (palaeozoogeography), because these fossils occur also in strata documenting those sections of the Earth’s
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geological past from which dinosaur bones are absent or very rare. The study of fossil footprints or other animal traces is called palaeoichnology (from Greek ichnos, trace).
First, however, you need to identify the footprints. In order to do this, you have to compare various measurements and parameters, like digit ratios (proportions of toe , their divarication angles or shape. The classification of tracks is called “parataxonomy” (parallel to the standard zoological systematics or taxonomy). Various related animals can leave similar footprints, assigned by scientists to the same ichnogenus (e.g., members of several sauropod families left Parabrontopodus tracks, while others – those assigned to the ichnogenus Brontopodus).
The best preserved footprints can be compared with foot skeleton of various dinosaurs to identify their trackmakers. Some footprint types can fill in the missing links in dinosaur evolution.
Dinosaur limbs are derived from typical pentadactyl (five digit) limbs of earlier land vertebrates. However, the number of toes or fingers often underwent reduction and most dinosaur limbs were tri or tetradactyl. Toe pads were located under the joints (like in modern birds), and not under phalanges (toe bones), like in us, mammals. The digits ended in claws (surrounded by keratinous, or horn, sheets); in ornithischians they were often blunt and hooflike, while the theropods had sharp hook like claws.
Sauropods had elephantine, pillar like legs with feet supported by an elastic heel pad and with claws barely extending beyond the oval foot outline; their front limbs, touching the ground only with the fingertips, left much smaller, kidney shaped imprints. Toes are easily rcognizable in footprints of other dinosaur groups. Three toes of the “hoofed” stegosaurs and ornithopods were short and blunt, so their imprints look like rhinoceros footprints. Theropod legs were very birdlike, with elevated tarsometatarsus, though not as tightly connected as in avian feet.
As shown by their fossil footprints, dinosaurs walked on erect (straight) legs, placing their feet close to the trackway’s midline, and were not dragging their tails (like often depicted in older restorations).
The best and longest lasting imprints are those left in soft, wet sediment, like mud. For leaving tracks, silty sediments are much better substrates than sand. When dried, the traces can survive many summer days or weeks if there is no rain. To be preserved longer, they have to be buried under another layer of sediment, differing from the substratum, fe.g., by sand brought by a flooding river over muddy banks. After millions of years, when the sand hardens into sandstone, the footprints would be occurring as convex natural casts on the bottom surface of the sandstone layer. Sometimes also “undertracks” are found, imprinted in the sandy bed underlying a thin mud layer (the original mud layer is rarely preserved, because silts and loams swell and crack due to changes in humidity).
Fossilized dinosaur footprints fascinated people from the time immemorial. Tracking animals was a valued skill in hunter gatherer tribes and the fossil tracks they found inspired legends of the early societies. In many places, the dinosaur tracks are accompanied by cult objects, e.g., rock carvings in Utah, made by Anasazi Indians.
In the Holy Cross Mountains, in a settlement called Kontrewers, there are also rock carvings (depicting human like silhouettes) on a boulder with Jurassic dinosaur footprints. Dinosaur tracks found by our ancestors are probably responsible for the three toed bird like feet of European dragons, trolls or devils, as in the case of the Holy Cross Mountains. It seems that the local folklore inspired the great Polish poet, Adam Mickiewicz to describe in one of his ballads (published in 1820) the devil, Mephistopheles, visiting a Polish nobleman, Jan Twardowski, as having chicken feet with claws of a sparrowhawk, instead of traditional goat hooves.
The First Dinosaurs in the Region
Almost 250 million years ago, at the beginning of the Triassic period, thick aeolian (desert in origin) beds called Buntsandstein (variegatedsandstone in German) has been deposited in Central Europe. Near Ostrowiec Świętokrzyski Chirotherium footprints left by thecodonts (early archosaurs) have been found (they are on display in the Museum of Nature and Technology in Starachowice and by the river dam in Wióry. Dinosaur footprints appear almost 50 million years later, in an outcrop a dozen kilometers SW, in gullies around Skarszyny near the village Broniszowice. There are two kinds of footprints there – smaller Evazoum and larger raditionally called Tetrasauropus. They were probably left by smaller and larger early
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plant eating sauropodomorphs. One of the footprints has been left in situ. to be seen byt tourists. It has been probably made by an early prosauropod, such as the Plateosaurus known from Germany.
The Plain
In the earliest Jurassic, almost 200 million years ago, the northern margin of the Holy Cross Mountains was a plain with winding rivers. Sparse conifer trees (Hirmeriella) grew among lower vegetation, whose leaves are known as Podozamites. The wood of Hirmeriella. is preserved as a precious kind of coal, called jet and used as a gemstone. This was the environment where the Zagaje Formation sediments formed. Dinosaur footprints were preserved in these strata. The most common type of footprints found there, Kayentapus, fit the feet of a theropod dinosaur, Dilophosaurus, known from the Lower Jurassic of Arizona. The six metre long predator had a double crest on its head. Interestingly, only this kind of footprints was found in that locality for quite a long time, as if dilophosaurs were the only inhabitants of the area in the earliest Jurassic. Dilophosaurs could have hunted for fish along the river banks A swimming theropod track (Characichos tridactylus) has been indeed found in Sołtyków. Small footprints Anomoepus and Delatorrichnus (left presumably by small ornithichian herbivores) have been also found in small quantities.
Only in 1999, researchers discovered there two parallel trackways of large sauropods heading south and four trackways of juveniles heading north side by side, and then simultaneously accelerating their pace and turning slightly to northeast. It is the oldest record of gregarious behaviour among sauropods worldwide. The young sauropods from Sołtyków marched as a herd. A solitary juvenile left its tracks in the bottom of a slightly younger bed of the Skłoby Formation in Gro madzice; its natural cast can be seen in the outcrop GPS: N 50°53.157’; E 21°21.427’). The herd of young sauropods from Sołtyków could have been startled by two dilophosaurs, approaching from the northeast and from the southeast; their footprints nave been also preserved. The juveniles hurriedly turned towards the northeast, while two adults came towards them, as if to protect the young by entering between them and the predators. Adult sauropods could have certainly scared away the dilophosaurs. But even the adults would be in serious trouble, when attacked by a huge theropod, whose tracks, measuring more than half a metre, have been unearthed nearby. The track bearing surface in Sołtyków has been chemically hardened and protected under a roof; there are also information stands. Thus, the geological preserve Gagaty Sołtykowskie (Stąporków forestry headquarters) is a worthwhile tourist site.
Some 15 km to the SE, in Kontrewers near Mniów, a Moyenisauropus footprint, left by a large ornithischian, probably a scelidosaur, has been found in rocks of the same Zagaje Formation (probably of Hettangian age). Such tracks are more common only in strata a couple million years younger.
At the Seashore
Some 196 million years ago, by the end of the Hettangian stage of the Early Jurassic, few million years after the formation of track bearing surfaces in Sołtyków, Kontrewers and Gromadzice, new dinosaur traces were imprinted. There was a shallow sea crossing the present territory of Poland from the NW to the SE. In its SW shore, a lagoon formed around the present day Gliniany Las near Mniów. Its sediments are known as the Przysucha Ore Bearing Formation in present territory of Poland from the NW to the SE. In its SW shore, a lagoon formed around the present day Gliniany Las near Mniów. Its sediments are known as the Przysucha Ore Bearing Formation km north, near present day Zapniów.
Small carnivorous dinosaurs resembling the North American Coelophysis, scurried along the beach. They scavenged animal remains drifted ashore by waves, or hunted invertebrtes, such as horseshoe crabs, whose traces are also found on rock surfaces in the Zapniów ceramic clay mine.
Fossil mollusk shells and corals occur in the area, so geologists believed that a sea covered the area in the Late Jurassic, like the whole territory of present day Poland. However, footprints have been found not only in Bałtów; other tracks have been discovered in Upper Jurassic limestones in Wólka Bałtowska, OŜarów, Wierzbica and Błaziny. The Błaziny specimen — a Dinehichnus track left probably by an ornithopod, is on display at the Regional Museum in IłŜa. Thus, at least periodically, islands must have emerged from the Late Jurassic sea. Their beaches were built of carbonate sand, made of remnants of animal skeletons. The Bałtów corals bear traces of breaking by waves. Land plants and traces of their roots are also known from Wólka Bałtowska.
The largest track from Bałtów is a footprint with three short blunt toe imprints (displayed in the Museum of Nature and Technology in Starachowice), perhaps left by a bipedally walking stegosaur.
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The smallest track from Bałtów (Wildeichnus), was made by a tiny theropod dinosaur, such as Compsognathus, whose skeleton has been found in lagoon sediments of equal age in Solnhofen, Bavaria, from where also the famous earliest bird, Archaeopteryx has been found. The track is housed in the Bałtów Jurassic Museum. In Bałtów, you can walk through a “Jurassic Park” along trails leading to dinosaur tracks and watch life size restorations of prehistoric animals. Especially noteworthy are those representing local fossil fauna. In the Permian and Triassic sectors of the park, there are restorations of synapsids (mammal like reptiles), labyrinthodonts (amphibians)and thecodonts (early archosaurs) similar to those that left their foorprints in the Triassic sandstones in the area. Somewhat further along the route, you pass by a Coelophysis from the Triassic/Jurassic boundary, and a Sołtyków scene with two dilophosaurs, a pair of adult sauropods (based on South African Vulcanodon) and four juveniles. Next stands an Early Jurassic Scelidosaurus. In the Late Jurassic sector, there is a group of Kentrosaurus (stegosaurs, restored in bipedal stance), ans a large Allosaurus similar to the largest terrestrial predators ever living in Poland.
The Cretaceous part of the open air exhibition two duckbill dinosaurs (hadrosaurs) are shown: a Parasaurolophus and a Corythosaurus. Their cousin left its tracks some 130 km east from Bałtów, in the Roztocze region (SE Poland), where in the latest Cretaceous times (some 70 million years ago), a margin of the Małopolska land or an archipelago of carbonate islands was emerged. Footprints of large hadrosaurs have been recently found in Potok near Zwierzyniec (hadrosaur bones were found in the neighbouring Ukraine. Hadrosauripus tracks consist of a small diamond shaped manus (hand) imprint and much larger triactyl pes (foot). A large theropod footprint, resembling Irenesauripus from western Europe and North America, has also been found. The fossils can be seen in the agrotouristic cottage Zagroda Guciów near Zwierzyniec.
You are welcome to visit the “Holy Cross Mountains Jurassic Park”, as well as the Geological Museum of the Polish Geological Institute in Warsaw, and the Museum of the Holy Cross Branch of the PGI in Kielce, where you can find not only the dinosaur footprints, but also the background information on geological heritage of this unique area. Other dinosaur related exhibits are available also in the Museum of Evolution, Warsaw and at the excavation site in Krasiejów (SW Poland). Precious Heritage
Dinosaur footprints are among the most telling elements of our geological heritage, providing a unique insight into the bygone world of Mesozoic giants and teach us about the fragility of all species, including our own. They also an, as shown by many examples worldwide, boost local economy providing tourist attractions and educational value.
Let’s help to preserve them for future generation, as they survived already for hundreds of millions of years. Please do not touch or damage the exposed track bearing surfaces, and notify the local authorities (police, forestry staffe, etc.) about observed cases of vandalism or other hazards to the fossils.
REFERENCES
Gierliński, G. & Pieńkowski, G. (1999). Dinosaur track assemblages from the Hettangian of Poland. Geological Quarterly, 43: 329–346 Gierliński, G. & Sabath, K. (2002). A probable stegosaurian track from the Late Jurassic of Poland Acta Palaeontologica Polonica, 47: 561–564 Gierliński, G. & Niedźwiedzki, G. (2002). Dinosaur footprints from the Upper Jurassic of Błaziny. Geological Quarterly, 46: 463–465 Gierliński, G., Niedźwiedzki, G., & Pieńkowski, G. (2004). Tetrapod track assemblage in the Hettangian of Sołtyków, Poland, and its paleoenvironmental background. Ichnos, 11: 195–213 Gierliński, G. & Niedźwiedzki, G. (2005). New saurischian dinosaur footprints from the Lower Jurassic of Poland. Geological Quarterly, 49 (1): 99–104. Polish Geological Institute (Geological Museum) www.pgi.gov.pl Bałtów Jurassic Park: www.parkjurajski.pl Museum of Nature and Technology, Starachowice www.ekomuzeum.pl
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EX CURSION GUIDE
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LOCATION OF EXCURSION SITES
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GEOLOGICAL HERITAGE OF VENTA RIVER VALLEY, LITHUANIA
Jonas Satkūnas, Lithuanian Geological Survey, ProGEO Northern WG Apolinaras Nicius, Venta Regional Park
Venta River is a river is north western Lithuanian and western Latvia. The total area of the Venta basin is 11 800 km 2, of which 67% is situated in Latvia. Venta River source is near Kurš÷nai in the Lithuanian Šiauliai County and flows into the Baltic Sea at Venspils in Latvia. The Venta has many tributaries, but only one of them, the Abava River, exceeds 100 km in length. The tributary Virvyčia at 99.7 km is just shy from 100 km mark. Another tributary Varduva is 96 km long and flows into Venta at the Lithuanian–Latvian border. Along the Venta River – a lot of valuable geological heritage objects are located.
Location of Venta river basin
Outcrops of Jurassic rocks in Venta river valley are known since 1811, when Dionizas Poška, famous writer and collector of antiquities visited Papil÷ village and collected number of fossils. However the first scientific investigations of Jurassic outcrops were carried out by engineer Jan Ulman in 1825–1826. Later on, the outcrops were visited and reinvestigated by great number of researchers from universities and other geological organisations of Russia, Germany Poland, Lithuania and other countries. Due to long history of investigations rich collections of fossils from Papil÷ now are disposed in geological museums of many European cities.
The Jurassic outcrops in Papil÷ town and its vicinities are unique in the Baltic region and are of great scientific significance. The course of Venta river valley with outcrops was established as geological protected area in 1960 and the outcrop in very Papil÷ town was established as geological natural monument since 1964. On basis of the Jurassic geological values the Venta Regional Park was established.
The outcrops attract reseachers of Jurassic period up to now and they are being visited by students of geology from Vilnius University each summer.
The Papil÷ outcrop is included in the list of most representative geosites of the Baltic region (Satkūnas J., Ransed G., Suominen Y., Taht K., Raudsep R., Mikul÷nas V., Vdovets M., Makarikhin V., Cleal C.,
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Erikstad L. et al. Geosites listings for Northern Europe – a status report // 32 nd International Geological Congress, Florence, Ital. August 20–28, 2004: Volume of Abstracts. Part 1. – [Florence], 2004. – P. 581.
According to A. Linčius, more than 300 species of fossils have been identified in Jurassic rocks: ammonites, foraminiferra, fishes etc. Among them fossils of mollusca (41 species) and ammonites (25 species) prevail. The name of Papil÷ town is included into names of several species of ammonites – Indosphinctes (Elatmites) papilensis (Pak.), Binatisphinctes (Okaites) popilanicus (Krenk.), Cardioceras (Plastmatoceras) popilaniense Bod. Astarte (Astarte) papilensis Rotkyt÷ L. The Papil÷ outcrop is the stratotype of the Papil÷ Formation.
Besides Jurassic outcrops there are number of other valuable geotopes in the Venta regional park: Quaternary outcrops, picturesque erosional remnants, erratic boulders etc.
Quarries of Triassic clay and Permian limestone, located nearby the Venta regional park are additional interesting sites for visitors, studying geodiversity.
Geological mapping in Venta regional park was recently completed. In the course of the mapping it were revealed interesting features of the Quaternary cover. For example, the area is characterised of wide occurence of Middle Weichselian lacustrine deposits, outcroping in several exposures in the Venta river valley. It is necessary to stress that sites with Middle Weichseliann deposits are very few in entire Baltic region. Therefore, the Venta regional park is of great interest for Quaternary researchers as well.
Besides the values of geological heritage in the park's territory there are many villages with historical and architectural values: chapels, roadside poles with a statuette of a saint, mounds and rests of the manor's parks. In this regional park there are Purviai reserve with unique part of the Uog÷ river, Purv÷nai geomorphologic reserve, Avižliai, Dabikin÷, Virvyt÷ hydrologic reserves, Užpelkiai botanic zoological reserve, Viekšniai urban rezerve. There are four water mills left in this park, two of them (Viekšniai and Augustaičiai mills) are still working. Other valuable object – the Dubiškiai estate. In the park of this estate there are 13 local and 9 introduced tree species. Totally in Venta regional park there are 670 species of plants with abundance of orchid family, 140 species of birds, 184 – insects, 27 – mammals, 7 – amphibians and 3 – reptilians.
Thanks to endeavours of National service of protected areas of Lithuania and Venta Regional Park, the outcrops of jurassic rocks now are installed for visitors. The geological trails are equipped with information stands, view sites etc.
The section of the Papil÷ outcrop (according to L. Rotkyt÷ (1968)
Depth of layers from the top of Geological age Sediments and fossils the outcrop 0.0–15.0 m Quaternary Glacial brown clayey loam with boulders. Jurassic period, Black clay with mica, with interlayers of sandstone and lenses of 15.0–17.8 m Callovian age, siderite. Fossils of ammonites Astarte sauvalei., Astarte Skinija Formation trembiazensis Lor., belemnites. Sandstone, yellow, with interlayers of black clay. Ammonites: Kosmoceras transitionis Nik., Kosmoceras cf. Compressum 17.8–18.8 m Quenst. Mollusca Oxytoma inaequivalvis (Sow.), Chlamys (Aequipecten) fibrosa (Sow.), Protocardia cognata (Phill.), Trigonia zonata Ag., Myophorella undulata (Ag.). 18.8–19.3 m Limestone dark brown, sandy. Fossils of brachiopoda, bivalvia. Sandstone brownish, weekly cemented. With detritus of fossils 19.3–20.5 m and wood. Jurassic period, Sand grey, very fine. Fossils of bivalvia, brachiopoda, tracks of 20.5–21.0 m Callovian age, worms. Papartyn÷ Formation Konglomerate. Fauna – ammonites: Kosmoceras jason Rein., 21.0–23.9 m Kosmoceras castor Rein., obductum Buck. Jurassic period, Sand yellow. Fine grained with interlayers of grey clay. 23.9–25.4 m Callovian age, Papil÷s Formation
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Geological cross section MH 1:220 000
Geological cross section MH 1:220 000 (author J. Bitinas)
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Legend of geological cross section (part 1)
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Legend of geological cross section (part 2)
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Jurassic outcrop in Papil÷ town is now installed for visiting. Such type of demonstration of exposure, protected by roof from precipitation is the first at all in Lithuania
Works during the installation of the Jurassic outcrop. Two Jurassic layers are exposed – black clay and sandstone (below)
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Geological trail in Jurakalnis (Jurassic Hill). Vistors here can have opportunity to take a look into Venta river valley, examine Jurassic rocks. The site is interesting due to active process of formation of ravines, occurence of landslides, springs and exibition of erratic boulders
The artificial outcrop of Jurassic sandstones at the Papartyn÷ locality is maintained for collectors of fossils
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Erosional remnant in cofluence of rivers of Avižlys and Venta is a particular landform. This narrow horn is 100 m lenght and of only few metres wide
Exposure with Quaternary lacustrine gyttja in Venta river valley. Presence of shells of mollusca indicate favourable paleoclimatical conditions during the sedimentation. The site is under stratigraphical investigations
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Loops of Venta river
Exibition of collection of amonites collected by Česlovas Pakuckas (1898–1965) in Papil÷ outcrops, located in Geological Museum of Vilnius University. Ammonites are prevailing fossils. The ammonite, symbol of sedimentary geology and biostratigraphy is the logotype of Lithuanian geological survey and Venta Regional Park
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JURAKALNIS OUTCROP
The geological outcrops of Jurrasic are known in vicinities of small Papil÷ town of Akmen÷ district in the valley of Venta River. A lot of fossils is found here. The sediments of Jurrasic crops out on both sides of Venta River in almost of 5 km long interval from Augustaičiai mill to the bridge across Venta in Papil÷ and in ravine called Jurakalnis on the left bank of river as well. Exposures of Jurrasic sediments also are known along the Venta River to south from Papil÷ in Papartin÷ and Rudikai.
The description of it is present below, with the indexes of strata in letters introduced into practice by prof. J. Dalinkevičius in 1926 (Fig. 2)
Fig. 1. Jurakalnis (Jurassic Hill) (photo I. Virbickien÷)
Jurakalnis ravine, the left bank of Venta River, at distance of 75 m above the mouth of ravine. Under the Quaternary sediments beds reveal (downwards from above), as follow:
J3ox 1 u Siltstone clayish, dark grey, micaceous, contains thin interbeds of light grey sandy siltstone in upper part, non carbonaceous, thickness 2.5 m.
t Siderite brown gery in fracture, very hard, with metallic lustre, heavy, lies in the form of concretion loafs, thickness 0.1 m.
s2 Siltstone claysh, black micaceous compact; poorly preserved fauna: Cardioceras excavatum (Sov.), Cardioceras sp., thickness 2.4 m. J2cl 3 s1 Siltstone analogous to described above, fauna wasn’t found; concretions of siderite from bed on the lower contact, thickness 2.0 m. r Concretions of siderite in the brownish, oolitic, clayish, highly ferruginous sandstones, thickness 0.35 m. r Silty clay, black, micaceous, ferruginous, contains tare grains of oolites, thickness 0.25 m. r Concretions of siderite in the dark brown, oolitic, ferruginous sandstone 0.2 m. q Silty clay, black, micaceous; frequent large belemnites: Cylindrotheutis beamontiana (Orb.) 0.3 m. 2 J2cl 2 P3 Sandstone clayish, light brownish, fine grained, enriched by leery hard lumps of the same sandstone overfilled by remains of fauna and charred wood; in the upper part of bed the sandstone is weakly cemented; enclosing and interbeds of above lying clays; fauna Kosmoceras pollux (Rein.), Peltoceras sp., Reineckia sp., Rhynchonella alemanica Rollier , gastropods 0.65 m. P1 2 Sand clayish, yellowish grey, fine grained, weakly cemented, containing fragments of fauna and remains of lignite 0.65 m. o Sandstone, light grey, fine grained, very hard, fractured, splits into large pieces, weathered and ferruginous in cracks; fauna is rare Gryphaea sp. 0.4 m. n Sand clayish, yellowish brownish, fine grained, weakly cemented, containing pockets filled by fragments of shells; the observed thickness 0.3 m.
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Fig. 2. Composite section of Jurassic rocks in Papil÷ (after A. Grigelis, 1985): 1 – pebble, gravel; 2 – sandstone; 4 – aleurite; 5 – limestone; 6 – clayey limestone; 7 – marl; 8 – concretions (silicificated, carbonate); 9 – finds of fossils (Amonites); 10 – hiatus
REFERENCES
Dalinkevičius J., 1934. On the Profile of Jurassic and Tectonics in Papil÷. Summary. Kosmos , v. 15, 294–304 Grigelis A., 1985. The Zonal Stratigraphy of Baltic Jurassic on Basis of Foraminifers. Sumarry. Moscow, Nedra, 131 p.
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ŠALTIŠKIAI QUARRY
The claystones of Nemunas Formation, Lower Triassic, occurs in Akmen÷ district (Fig. 1). The thickness of the Triassic variegated claystones reaches up to 100 m. In places where the overburden of Quaternary or Jurassic rocks is thin deposits of Alkiškiai and Šaltiškiai were prospected. The productive deposit of claystones lie on the erosional surface of the Upper Permian limestone (Fig. 2). The succession dips south , south westwards at an angle of incidence of 20º. The claystone is brown, reddish brown with lenses and interbeds of bluish grey clay. The reddish coloured clay is plastic, sometimes of lump structure. The bluish grey clay sometimes contains very fine grained (1–10 mm) lenses and thin vein of fine grained quartz sand or silt. In some cases carbonate concretions (up to 1– 3 cm of size) and grains of gravel (up to 1–3 mm of size) located in the sandy intervals are found in the upper part of productive deposits.
Šaltiškiai quarry (photo J. Čyžien÷)
The common thickness of the clay, in both deposits reaches up to 100 m. Clay is medium disperse, heavily ferruginous dolomitized, rather homogenous. It compresses: illite (50–60%), smectite (30–40%) and chlorite (5–10%). Such a great amount of smectite is not common for clay of other geological systems. Due to such a mineralogical composition, the Triassic clay has very good absorption properties. Such a clay is fit raw material for production of cement because of very small quantities of oxides of alkali metals and good silicate (1.8–2.7) and aluminates (1.7– 2.8) modulus. The fraction of fine grained sand is formed mostly by quartz (90%), feldspars (3–4%), carbonates (1%). Quartz comprises up 60% of silty fraction, carbonates – 20 30%, feldspars – 7%, micas – 2.5%.
The Šaltiškiai caly deposit has been exploited since 1972. The reserves are 20.8 million tones of clay.
REFERENCES
Mikaila V., 1971. The Mode of Occurrence of Triassic Sediments of North Lithuania and Predicted Areas of Clay Deposits. Summary. – In: P erspective Mineral Products of South Baltic Region. Proceedings of Lith. Geol.Sci. Res. Inst. , vol. 18, 45–52 Rajeckas R., Saul÷nas V., 1977. Exploration and Prospecting of Mineral Resources. Summary. – In: Works of Geologists in Soviet Lithuania , 25–37
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KARPöNAI QUARRY
The quarry of Karp÷nai is situated in Akmen÷ district about 1.5 km to east from town of Naujoji Akmen÷ near the cement factory. These cement factory exploit the limestones of Upper Permian Naujoji Akmen÷ Formation. The principal limestone quality feature on which its practical use depends is its chemical composition. Physical mechanical properties are only important during limestone utilization as a natural building material. Utilization possibilities are mostly determined by the content amounts of four components: CaO, MgO, SiO 2 and Fe 2O3.
Limestone is devided into six industrial varieties according to value of the principal components, taking also into account the indices limiting its use: especially pure, very pure, pure with increased content of clay, slightly clayey or slightly clayey dolomitized and dolomitized to dolomitic. Each variety may be useful for different branches of production joined into six groups on the basis of similarity of requirements for limestone quality.
Karp÷nai quarry (photo J. Bitinas)
The Upper Permian Naujoji Akmen÷ Formation (analogue of Zechsteinkalk cycle (Ca1) of Lower Zechstein Z1 in Westerm Europe) bed of carbonate rocks (up to 38.2 m thick) has a variable thickness and is composed of three groups of strata: lower clayey limestone, intermediate – limestone and upper – dolomite. Most often the greater part (60–100%) of the bed consisits of limestone rocks: microcrystalline slightly clayey chemogenic limestone and slightly clayey dolomitized limestone. Other sorts of limestone are less wide spread. Besides chemogenous, there has also formed an organogenous calcite. Limestone thickness is locally increased in these accumulation places of carbonate mud containing animal shells, supposedly shallow, because the great part of shells is reduced to fragments. In this connection may be mentioned the magnified thickness of the limestone bed in Karp÷nai deposits:
1 – limestone grey and dark grey, clayey, fine grained, vaguely stratified, medium hard, porous (up to 30%), in some places it has spotted structure which appears from painted by limonite walls of pores. It contains Pelecypoda Schizodus schlotheimi Gein., Pseudobakewellia ceratophagaeformis Noin. and Ichtyofauna Paleoniscidae gen. indet.
2 – limestone light grey and grey, fine grained, nonstratified or unclear stratified, medium hard, porous and cavernous. Caverns frequently contain druses of calcite. Balls and lenses of more dark limestone are distributed (all over the bed). They consist of hard shell like fractured fine grained rock granular limestone.
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Such a section is to the top of pack wall of quarry in these places where biomorphic detrital limestone is absent in upper part of section. There are found: Pseudobakewellia ceratophagaeformis Noin., Schizodus sp., Turbo obtusus Brown, also Palacophycus insignis Gein.
3 – limestone analogous to one of stratum 2 but contains interlayers and lenses of organogenous detrital limestone.
The latter limestone is light grey, formed by shells of bivalve mollusks and their fragments. Thickness of these interlayers and lenses is 0.2–0.8 cm. Limestone is porous and cavernous; shells are cemented by fine grained calcite. Fauna is the same as in stratum 2.
4 – fractured the upper part of bed of limestone. It consists of various sizes and forms pieces of fine grained and biomorphic detrital limestone and grounded up limestone. Here and there it is brightly limonitized.
Whole bed of limestone is split by fissures to pieces of various sizes. In some places of quarry the upper part of bed of limestone is karsted. The karsted pits are filled by dark sandy sediments of Upper Jurassic age, parti coloured clays of Lower Triassic age or Quaternary sediments. The upper part of bed frequently is limonitized.
The exploitation of limestone in quarry of Karp÷nai started since 1952, now annually are exploited about 1 million tons of raw materials, reserves of prospected raw materials of quarry make up 90 million tons. It is useful for cement (73.3%), building lime (21.5%) and several other branches of production (5%). Karp÷nai limestone quarry is operated by SC „Kalcitas“. The quarry is operated in two levels – one of topsoil and one of production. The topsoil is removed by a walking excavator EŠ 10/70 and moved to the depleted part of the quarry that currently occupies an area of approximately 400 ha. The production level is loosened by blasting and excavated by direct excavation, using the electrically powered excavators EKG 10 and EKG 8. The rocks are loaded into „Belaz“dumpers and transported to the grinding facility.
For draining of ground water in Karp÷nai quarry, water collection canals are installed all over the quarry from which the water is collected into the sump and pumped by means of the pumps into a rivulet Dabikin÷ outside the quarry. Before discharging the water into the rivulet, all the water from the quarry flows through a cesspool where the particles suspended in the water are sedimented and the water impureness is reduced to the permitted values, conform the “Environmental requirements for the waste water treatment” approved by the order No. 495 of October 5, 2001, issued by the Environmental minister of the Republic of Lithuania. Approximately 5.5 million m3 of water per year is pumped out of the quarry. Part of the water is used for cement production.
REFERENCES
Gasiūnien÷ V. E., Kadūnas V., 1997. Lithuanian limestone distribution, quality and utilization. Lithuanian Geological Survey Special Publication , Vilnius 1997, 54 p. Vodzinskas E, Kadūnas V., 1969. Carbonate products of the Lithuanian SSR. Dolomites and limestones. Summary. Vilnius, Mintis, 127–129
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ŽAGARö DOLOMITE DEVONIAN OUTCROPS, ŽAGARö REGIONAL PARK
The rocks of Devonian Skaistgirys beds are found in outcrops of Švet÷ River in Žagar÷ town. The sandy metasomatic dolomites with interbeds of sandstones prevail in the lower part of the beds. The Old Žagar÷ beds cover Skaistgirys beds. They are accessible for investigation on large area in outcrops of Šv÷t÷ River and in the quarry of Žagar÷. Lithologically and facially their section is stable, they were formed in environments of offshore lagoon of regressing basin. The interbed of conglomerate – type, dolomite (thickness 15 cm) restricted by two abrasive surfaces, marks the lower contact boundary with Skaistgirys beds. The summary thickness of beds reaches 2–4 m.
The quarry of Žagar÷:
2.0–2.53 m Dolomite yellowish grey with greenish pockets, fine crystalline, hard with random stratification of layers of 10–15 cm thickness, contains rare caverns.
2.53–3.40 m Dolomite yellowish grey with bluish – greenish spots, hard, fine crystalline, contains frequent accumulations of casts of Bivalvia on surfaces of layers, rare caverns.
3.40–4.46 m Dolomite yellowish grey with bluish greenish spots of marly dolomite, fine crystalline, with caverns.
The section of Skaistgirys quarry gives an important data for better recognition of rocks of Old Žagar÷ beds.
Lithologically and paleontologically there are many likenesses between this section and one described in Žagar÷ quarry (Fig.). Among fossils of the section of Skaistgirys beds Brachiopoda dominate in form of imprints and casts. Finds of Cyrtospirifer kapsedensis (Liep.), Centrorhynchus sveticus (Liep.) are rather characteristic. Besides that, the accumulations of segments of Crinoidea and Bryozoa are common. Lences of clay contain rare shells of fossil fishes: Dinichthyes sp., Dipterus sp. The Old Žagar÷ beds are characterized by poor finds of fosils. Among them the accumulations of Bivalvia shells on surfaces of beds dominate.
The deposits of dolomites of Žagar÷ Horizon, Upper Famenian, are important source of dolomitic products in Lithuania. The Skaistgirys field of dolomites is intensively exploited since 1970. The overburden of the deposit is formed of glacigenic morainic loam. Its average thickness further development plot contains up to 4.2 million m 3 of prospected resources of dolomite. The exploitation rate of dolomites is 300 000 m3/year. Dolomites are used for production of ballast for roads construction. The Žagar÷ dolomite field was in reserve for some time at present exploitation started again.
Fig. Location scheme of Žagar÷ quarry
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(author J. Bitinas, original scale000) Bitinas, original J. 1:50 (author a scale 1:200 000 scale 1:200 a
Pre at quaternary Žagar÷ area ofgeological map the
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(author R. Guobyb÷) (author R.
Quaternary1:200 000 Mmap geomorphological
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(author J. Bitinas, original scale000) Bitinas, original J. 1:50 (author scale 1:200000scale
the at Žagar÷ quarry a Geological cross section of
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(after S. Žeiba) (after S. Cross section of Žagar÷ Cross sectionŽagar÷ Formation of
REFERENCES
Dalinkevičius J., 1939. The Devonian Stratigraphy and Traces of Lower Carboniferous transgression in Lithuania. Summary. Proceeding of Faculty of Math. Nat. Sci. of University of Vytautas in Great. Kaunas, 1939, v. 13, No. 4, 12– 29 Žeiba S., 1958. On the occurrence of Žagar÷ and Klykoliai Strata, Upper Devonian (D23) on the territory of Lithuania. Summary. Proceedings of Acad. of Sci. Of LSSR . Ser. B. 1956, No. 2, 91–98
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ŽAGARö ESKER, ŽAGARö REGIONAL PARK
The esker of Žagar÷ (Fig.) is a typical glaciofluvial geomorphological form, which appeared when radial crevasses of glacier were filled by coarse grained sediments. It was formed during the North Lithuanian phase of the last ice age. The glacier occupied the whole Žemgal÷ plain, meanwhile the ridge of Linkuva was pushed together on its edge. Water from melting glacier flowed from its central part by formed radial crevasses and washed out the channel not only in glacier but in the floor rocks too. Later this narrow canyon like river was filled up by gravel and sand and when the banks of ice melted it was transformed to the narrow causeyshaped ridge. It begins in Latvia and ends by the fan – shaped delta at a distance of about 10 km to south west Žagar÷, where the Martyniškiai deposit of gravel is prospected. This delta together with the indistinct frontal moraine of North Lithuanian phase fixed the former edge of the glacier.
The structure of esker is illustrated by block diagram of the gravel deposits of Žvelgaičiai, it’s nature of stratification – by pictures of structure, the direction of flow of former glacial river by rose diagram of inclination dip of cross beds.
The whole south western part of esker stretches – along the Švet÷ River. Here many of gravel and sand deposits were prospected at different time. The deposits are small and narrow like esker itself. The lower part of beds falls down under the surface of ground water and surrounding plain. By the intensive exploitation of deposits the great part of this rather rare geomorphologic form and geological body was destroyed.
Block diagram of gravel of Žvelgaičiai deposit (after G. Juozapavičius)
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GEOLOGICAL HERITAGE OF VENTA RIVER VALLEY IN LATVIA
UldisNulle, Atis Mūrnieks, Latvian Environment, Geological and Hydrometeorological Agency
In Latvia a great number geological monuments are located in the Venta river valley and its vicinities and belong to different geological periods and formations: Upper Devonian, Lower Carboniferous, Jurassic, Quaternary. Also there are located number of valuable features of present landscapes such as ravines, boulders, waterfalls, caves and springs.
Location of Geological and Geomorphological Nature Monuments of Venta river valley in Latvia
Geological and Geomorphological Nature Monuments of Venta river valley in Latvia:
Kalni outcrop – brown coal of the Callovian Stage, Middle Jurassic;
Losis outcrop – deposits of the ZaĦa Formation, Callovian Stage (Middle Jurassic) occur: yellowish sand, fossiliferous limestone concretions and black kaolinite clay;
Outcrops as L. research of the ZaĦa River – deposits of the ZaĦa Formation (Callovian Stage, Middle Jurassic): grey and black clay, sandstone, limestone, limestone concretions. In these deposits abundant remains of marine organisms – molluscs, ammonites, brachiopods etc;
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Location of Geological and Geomorphological Nature Monuments of Latvia
OgĜukalns outcrop – below the red, in places bluish grey, till deposits there is sand, clay, silt and dense, gyttja containing peat bed with total thickness of 3.3 m. Geological, palynological and palaeocarpological investigations indicate that this bed belongs to the Pulvernieki (Holsteinian) interglacial;
Embute ravines – an impressive ravine erosion landform area rich in biological variety;
Šėērvelis boulder – length 5.1 m, width 4.6 m, height 2.9 m, perimeter 15.5 m, volume ~18 m 3;
Lēgernieki outcrop – the Middle Jurassic (Callovian Stage) deposits composed of alternation of white quartz rich sand and black kaolinite clay with fossilised wood (lignite) fragments. As outlier transported from other location by the Quaternary glacier;
PlieĦi outcrop sandstone and clay of the Lētīža Formation (Lower Carboniferous);
Zoslēni outcrop – the highest outcrop of Jurassic deposits (Papil÷ Formation, Lower Callovian Substage, Middle Jurassic), 15 m high, represents white cross stratified quartz sand, in places with small brown coal lenses and clay pebbles, rarely sulphide nodules;
Sudmaikalns (Nikrāce) boulder – length 7.5 m, width 5.0 m, height 1.7 m, perimeter 21.0m, volume ~20 m 3; Dolomite outcrop at lower reaches of the Šėērvelis River – greenish grey dolomite with cellular structure. Stratotype of the Nīkrāce Member, Šėervelis Formation (Upper Devonian);
Ketleri outcrop – cross stratified sandstone with conglomerate layers, fish and tetrapod fossils. This famous paleontological site is stratotype of the VarkaĜi Mamber, Ketleri Formation (Upeer Devonian);
Ātraiskalns hill – in its lower part light, cross stratified, carbonate cemented sandstone is exposed (GobdziĦas Member, Šėervelis Formation, Upper Devonian). It is overlain by massive dolomite (Nīkrāce Member, Šėervelis Formation, Upper Devonian). Stratotype of the Šėervelis Formalion;
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GobdziĦas cliffs – in cliffs lower part light, cross stratified, carbonate cemented sandstone is exposed (GobdziĦas Member, Šėervelis Formation, Upper Devonian). It is overlain by massive dolomite (Nīkrāce Member, Šėervelis Formation, Upper Devonian); stratotype of the GobdziĦas Member;
Pavāri outcrops – in loose sandstone of the Ketleri Formation (Upper Devonian) there have been many founds of vertebrate remains. Very important are tetrapod Ventastega curonica remains discovered in August 1991;
Šėēde outcrop – stratotype of the Mūri Formation (Upper Devonian); light yellow, fine grained, cross stratified sanstone with interlayers of fossiliferous dolomite; well preserved fossils of brachiopods Camarotoechia, Cyrtospirifier and Cyrtiopsis;
Venta rumba (waterfall) – is widest waterfall in Latvia; its width in summer is ~110 m, during flood up to 150 m; height is 1.8–2.2 m. Venta waterfall has been formed in strong fossiliferous dolomite of the Ape Member. PĜaviĦas Formation (Upper Devonian) – ancient reef like barrier in the Devonian sea, which existed along southern part of the Tukums Kuldīga tectonic step. Reef like barrier has been inhabited by various Devonian organisms:algae, stromotoporoids, corals, brachiopods, molluscs etc. Dolomite is rich in voids formed due to dissolution of fossils of these organisms. Fine crystalline dolomite with clay and sandstone interlayers (also the PĜaviĦas Formation) lay under the fossiliferous dolomite. This is not so resistant, therefore the falling water of Venta River erodes it, and the waterfall year by year is gradually moving upstream;
Riežupe waterfall and outcrops – dolomite outcrops; stratotype of the Ape Member, PĜaviĦas Formation (Upper Devonian);
Riežupe sand caves – a labyrinth of artificial caves with total length of 460 m are cut into the loose sandstone (sand) of the Amata Formation (Upper Devonian). Caves have been made during several centuries, in result of sand mining; sand has been used to scrub dishes, to cover floors of rooms and later for glass manufacture;
Baltavots (White Spring) and Melnavots (Black Spring) – are high yield upward springs;
Muižagāji cliffs – reddish and yellowish sandstone and red clay of the Gauja Formation;
Ėīvmežs boulder – length 6.35 m, width 4.35 m, height up to 2.8 m, perimeter 17.5 m; volume above ground ~43 m 3;
Vecumi boulder – length 6.7 m, width 4.2 m, height 2.8 m, perimeter 17.5 m, volume above ground ~42 m3;
DampeĜi outcrop – located in Ventspils, on the left bank of the Venta River, 300 m downstream the Dampeli Farm. It is stratotype of the boundary between the deposits of the Ancylus Lake and the Litorina Sea (both the Quaternary);
Grīži Velna beĦėis (Devil’s seat) – is a boulder: length 6.8 m, width 4.6 , height up to 3 m, perimeter 17.8 m, volume above ground ~42 m3;
Staldzene steep coast – deposits of previous stages of the Baltic Sea and glacial deposits are exposed in a 4–8 m high typical abrasion coast of the Baltic Sea, 4 km to the NW of Ventspils. The lower part of the coastal exposure is presented by glacial deposits: grey till of the Kurzeme Glaciation and brownish varved clay accumulated in ice meltwater basin during the Late Glacial of the Latvia Glaciation. Above there are deposits of previous stages of the Baltic Sea. Oldest of them are bluish grey silt, silty clay and light sand formed the Ancylus Lake Stage (before 9000–8300 years). Possibly in some places deposits of the Yoldia Sea Stage (before 10000–9000 years). Above in the geological section there follows the lagoonal deposits of the Litorina Sea (before 7500–2800 years) – sand, silt, clay and gyttja, covered by peat bed. The latter probably has formed during the last phase of the Litorina Sea development. Upper part of exposure is composed of younger sandy and clayey river deposits and sand dune deposits.
Rich geological heritage and geodiversity of Venta river valley and its vicinities, displaying paleoenvironments and sedimentation history during Devonian, Carboniferous, Permian, Triassic, Jurassic, Quaternary periods as well as present landscapes provide excellent possibilities for development of cross border cooperation, scientific research, geoturism and education.
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GEOLOGICAL HERITAGE OF LATVIA
Atis Mūrnieks, Latvian Environment, Geological and Hydrometeorological Agency
Kalni outcrop: Jurassic brown coal
The Jurassic deposits are the youngest in the Pre Quaternary sequence of Latvia. These deposits occur in south western Latvia. Glacial erosion has strongly affected the irregular shape of their present distribution area. Many blocks of Jurassic deposits have been deformed and transported by glacier.
The Jurassic sequence of Latvia has various and peculiar composition – mostly siliciclastic deposits (grey and white sand, black and grey clay with interbeds of silt), but also beds and lenses of brown coal and fossiliferous sandy limestones. Total thickness of Jurassic deposits in Latvia does not exceed 25 m.
Mostly the deposits of the Middle Jurassic Callovian Stage (Papil÷ and Zana fms.) are present in Latvia, but in south westernmost corner also the Upper Jurassic Oxfordian Stage (Dunika Fm.) has been found. In Lithuania deposits of the Early, Middle and Upper Jurassic are present.
The deposits of Callovian Stage in Latvia have been divided into 3 substages (Liepins, 1961). Lower Callovian substage (Papil÷ Formation ) is composed of white sands with high content of quartz – more than 85% and even 90% – with admixture of feldspars and micas less than 10–15%. Also the heavy minerals are represented by mature assemblage – zircon, tourmaline, rutile, disthene and staurolite with minor garnet, hornblende and epidote. Sand usually is medium grained and fine grained, texturally mature, often cross stratified. Interlayers of weakly cemented sandstones are present in the Jurassic sands as well.
Beds of clay also occur in the Papil÷ Formation. Jurassic clays shovv peculiar mineral composition – dominant kaolinite with less illite. Admixture of organic matter and sulfides gives to clay its spectacular black and dark grey colour. Silts have minor role in the Papil÷ Formation. The Jurassic deposits is the only part of the geological seąuence of Latvia, where coal is present. Brown coal is dark brown, almost black earthy mass, which forms lenses and beds, up to 2.5 m thick.
In the Papil÷ Formation only such fossils as petrified wood, spores and pollen are present. The Middle and Upper Callovian substages (Zana Formation) are composed of grey sands, clays and fossiliferous limestones. Limestones often contain many fossils of marine invertebrates – bivalves, foraminifera, gastropods, brachiopods, echinoderms and ammonites. Besides clayey deposits bear rounded carbonate concretions with fossils. Sandy fossiliferous limestones are exposed in some places at coasts of small rivers Zana and Lose. These limestones contain also goethite ooids (in places sulfidised), which can be recognised on a weathered rock surface by their black colour.
Rich fossil assemblages allowed to recognise both Middle and Upper Callovian substages (Liepins, 1961) in the lithologically similar deposits of Zana Formation. Middle Callovian seąuence contains following fossils: ammonites Kosmoceras jason Rein. and K. castor Rein., brachiopod Rhynchonella varians Schloth., gastropods Cerithium sp. and Pleurotomaria sp. Also one tooth of pliosaur Peloneustes sp. has been found in the beginning of this century, but currently its location is not known exactly – probably in Germany.
Upper Callovian substage bears fossils such as ammonites Quenstedticeras lamberti Sow., Kosmoceras proniae Teiss. and K. ornatum Schl, belemnites Cylindroteuthis beaumontianus d‘Orb. and Pachyteuthis sp. etc.
The deposits of Upper Jurassic Oxfordian Stage (Dunika Formation) are found only in two boreholes in a small area near Rucava and Siksni. These deposits, up to 1.6 m thick, are represented by black sandy silts and dark grey fine grained sands and attributed to the Oxfordian Stage according to remains of mollusks and foraminifera.
The deposits of the Papile Formation (Lower Callovian substage) are supposed to be formed in Continental environment. Brown coal deposits are elongated and have curved shape, which resembles meanders of rivers. Besides sand seąuences shovv very changeable dip azimuths of cross strata in small distances, which also could be indicative of aliuviai origin. The same is shown by lack of marine fossils.
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In the Zana time (Middie and Late Callovian times) sea transgressed over the south western areas of Latvia, and marine deposits rich in invertebrate fossils accumulated. Goethite ooids presumably originated in shoal environment.
There are many evidences (deposits of brown coal, kaolinite rich clays, compositionally mature sands) that humid climate prevailed over area of southern Baltic at the boundary time between the Middie and Late Jurassic.
The Callovian sands poor in iron compounds after enrichment are useful as a raw material for glass and mould production. The most important is the Skudras deposit located south of Rudbarzi Village. Kaolinite clay could be useful for production of refractory ceramics, and due to small amount of iron oxides also for light colour materials, however mineral deposits are too small and have difficult mining conditions. Jurassic brown coal contains much ash and sulfur, therefore is low quality fuel comparable to peat. In summer of 1940 the Jurassic brown coal has been mined for several months and sent to the Riga and Broceni cement factories, where burned together with imported hard coal.
KALNI OUTCROP situated at the left coast of the Lose River in the Kalni Village is the best exposure of the Jurassic brown coal in Latvia. Coal bed reaches here thickness of more than 1.5 m. Kalni outcrop is situated 2 km southwards from Grieze – a locality where brown coal has been mined in 1940. Previous quarries are completely overgrown and flooded.
Lose River outcrop 1: Jurassic kaolinite claysandfossiliferous limestones
LOSE RIVER OUTCROP 1 is situated at the left coast of the Lose River (left coast tributary of the Venta River) 200 m upstream from its mouth. In this small exposure the Jurassic (Callovian, Zana Formation) deposits are seen (Fig. 1). Likely there is exposed a part of large erratic block, because the bedding is steeply inclined (up to 40°). Most interesting are typical Jurassic black kaolinite clays, as well as sandy limestones containing goethite ooids and many fossils – mostly bivalves, but also brachiopods, echinoderms and spectacular ammonites. The later are easily recognisable even in small fragments by their rainbow like lustre. Sometimes very well preserved ammonites have been found in this locality. Limestones usually contain small fragments of petrified wood, which likely were transported in sea from continent by currents and waves.
Description of section (from left to right): 1 sand yellowish grey. J 2cl. 2 limestone grey and dark grey. In places fossils are absent, but in other places limestone is rich in remains of bivalves, ammonites, brachiopods etc. J2cl. 3 clay grey (to left) and black (to right). J 2cl. 4 till reddish brown. Between beds 3 and 4 – sand interlayer. gIII ltv (?). Fig. 1. Geological section of outcrop of the Jurassic deposits (Zana Formation) at the left coast of the Lose River
Lose River outcrop 2: Triassic smectite clays
Like the Permian and Jurassic sequence, the Triassic deposits are present only in the south western part of Latvia. Irregular island like shape of present distribution area of the Triassic deposits is largely due to influence of the Quaternary glacial erosion. A lot of erratic blocks of Triassic deposits transported by glacier
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are present. The Triassic, as well as overlying Jurassic deposits was strongly subjected to erosion because are dominated by soft rocks with a minimum lithification degree.
In Latvia only lowermost part of the Lower Triassic – the Nemunas Formation – is present. In the area of Lithuania this formation is covered also by younger lower Triassic deposits. Middle Triassic is present neither in Latvia, nor in Lithuania, and some deposits of Upper Triassic (the Nida Formation) are found only in Lithuania.
The Triassic sequence of Latvia (the Nemunas Formation) is dominated by reddish and greenish grey clays with interbeds of sand and silt. Its maximum thickness reaches 30–74 m south from Nīgrande and close to Rucava. The Triassic clayey deposits are interesting by their mineral composition – smectite is dominant (50– 80%) among the clay minerals. Origin of smectite in these beds is still unclear.
Geological age of the Triassic deposits of Latvia has been determined according to phyllopods Estherites gutta (Lutk.), E. aequale (Lutk.), Estheria albertii Voltz. Ostracodes are represented by Darwinulla sp. Remains of small gastropods, fishes and spores Bullulina plicata Mal., Aggerella bullulinoides Mal., A. bullulinaeformis Mal., Neocalamites punctata Mal., Lophotriletes pussilus (Waltz.), Dilaterella exilis f. typica Mal. are also found (Gavrilova, 1979).
Deposits of the Nemunas Formation likely accumulated in continental settings under arid climate conditions (Paškevičius, 1997).
The Triassic smectite clays contain small amount of K 2O and Na 2O, therefore are used for production of high quality cement in Lithuania. In Latvia, however, clay is more sandy and therefore less qualitative, besides only quite small deposits with relatively thick rock cover are present. The Triassic clays could be used also for production of bricks and refmement of polluted waters.
LOSE RIVER OUTCROP 2 is situated at the left coast of this river 400 m upstream from its mouth. About one metre thick seąuence of red (in lower part) and green (in upper part) carbonate clays is exposed. These deposits are attributed to the Lower Triassic (Nemunas Formation). As usually in the Triassic of Latvia, these clays are dominated by smectite. Fig. 2. Geological section of the Pleistocene glacial deposits in the Vecvagari outcrop: tills of three glaciations in Vecvagari outcrop (after Aija Cerina) one belt of outcrops
VECVAGARI OUTCROP (Fig. 2) is only one area in Western, Northern and Eastern Europe, where the tills of three glaciations are seen at once in several outcrops, and the fourth till lies below being found by core (Kalnina, 1999). The valley of the Letiza River is favourable place for a detailed investigation of the tills.
Description of the 3 rd Vecvagari outcrop, which is situated approxi mately 8 m above a water level of the Letiza River (from base to top):
1. (1.3 m). Grey, very dense tiil with greenish grey and bluish grey belts (the most clayey layers) and rusty belts (silty layers). The till contains a lot of small pebbles and also larger pebbles (up to 5–10 cm in diameter, mostly carbonate rocks, rarely igneous rocks). Orange brownish colour appears along fractures, and in the lower part of bed iron hydroxide crusts, 3–7 mm thick, are present. The upper contact of the bed is quite sharp, fine hummocky, and is emphasised by an interlayer of bluish grey till, 1–2 cm thick;
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2. (1.25 m). Grey silty clay with greenish, in places greenish brown tone and obscure bedding. Upwards it grades into silt, which composes the upper 0.5 m of the section. The silt is light greenish and brownish grey and contains light yellowish grey inclusions. In places along fractures and bedding planes a rusty colour appears due to presence of the iron hydroxides. The upper contact of the bed is sharp, finely wavy;
3. (1–1.2 m). Yellowish grey sand with planar and lenticular, in places deformed lamination. The sand contains considerable admixture of silt, and in the lower part of the bed, 0.3 m thick, fine grey silty clay interlaminae are present. The upper contact of the bed is irregular, hummocky;
4. (1.5 m). Violet brown till with pebbles and small boulders of igneous and carbonate rocks. In the middle of the bed a lens of sand occurs.
5. (1.5 m and more) scree and soil with wood remains up to the upper part of a bluff.
The Latvia till in the southwestern part of Kurzeme and in the Vecvagari section is distinguished by a large content of clayey and silty size grains, large values of predominance of limestones over dolostones, and in all area of Western Kurzeme distinguished by the highest content of sandstones. The distinctions observed in the composition of different tills are interpreted by various positions of the ice flows. During the Kurzeme Glaciation the glacier advanced more westwards than during other glaciations. The glacier of the Latvia Glaciation advanced to the east and was submeridionally directed in general. The general direction of ice movements during the Letiza Glaciation has the intermediate position between directions of glacier movement during the Kurzeme and Latvia glaciations (Kalnina, 1999).
Zosleni Cape: Jurassic cross stratified white sands
Famous outcrop called ZOSLENU RAGS (cape) is situated in deep valley of small Dzelda River 80 m upstream from its connection with the Šėervelis River. Typical deposits – white sands – of the Lower Callovian (Papil÷ Formation) are exposed in this 15 m high outcrop. Sand is texturally mature and has various grain size – from coarse to very fine grained. Dominant sedimentary structures are trough cross stratification, as well as wavy and lenticular bedding. In very fine grained sand layers sedimentary structures are almost invisible. In places, usually in the upper parts of single layers – bedding deformation structures are present. Sands contain many small lenses and lenticular laminae of grey to black clay, carbonaceous clay and brown coal. In places drapes of clayey material occur on the inclined cross beds.
Two sedimentary (aliuvial?) cycles can be divided in the outcrop. Contact between the cycles is marked by a clay and coal conglomerate with gravelly sand matrix. Upward sand gradually becomes finer. Below the conglomerate silty and very fine grained sand is changing downwards into fine grained sand. Sand is white and light grey in largest part of the outcrop, but in lower 4 metres of the outcrop it has yellow colour.
Measurements of cross stratification shows dip azimuth to west, but in another smaller outcrop situated 150 m from Zoslēni Cape the dip azimuth is to south east Probably it indicates that the sand beds have accumulated in meandering river. It is supported also by cyclic structure of the sand sequence and many inclusions of brown coal.
Recent mineralogical study by Dr. Bernarda Klagisa shows that sand is highly mature in all sequence, but feldspar/quartz ratio increases downwards (content of feldspar in the upper part of outcrop is 7–10%, but in lower part – 10–15%). This ratio seems to be independent from cyclicity of a sequence.
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DEVONIAN DOLOCRETES AT THE MOUTH OF THE RIVER LĒTĪŽA
Ăirts Stinkulis, University of Latvia
Dolostone of the Nīkrāce Member, Šėervelis Formation, Famennian Stage correspond to the uppermost part of the Devonian sequence in Latvia. These youngest Devonian beds of Latvia are well exposed at left bank of the River Lētīža near its mouth. The outcrops are approximately 300 m long and 4–5 m high, which corresponds to whole thickness of the Nīkrāce Member.
Dolostones have several features, which indicate their origin and diagenesis in desert like environment during regression of the Devonian basin: • irregular bedding of dolostone (Fig. 1); • cellular structure – cell shaped vugs in dolomite are filled with clay (Figs. 1 and 2); • clayey material within the vugs contains clay mineral paligorskite indicating subaerial settings and arid climate; • admixture of chert together with high content of magnesium also shows shallow basin / subaerial environment and arid climate; • dolostone contains rounded, irregularly concentric grains – pisoids (pisolites), 0,5–5 mm in diameter, which have pendant shape and are sorted in reverse grading – their size increases upward (Fig. 3). Such pisoids are typical indicators of soil processes, and their pendant shape have formed as pisoids grew in vadose environment under influence of vertically migrating groundwater; • aggregates of several pisoids attached to each other by bridge like cement also show groundwater movement along grain contacts and vadose environment (Fig. 4); • cell shaped vugs often have pendant shape indicating their formation in vadose zone as well; • fine wavy laminated crusts, lower part of which is more irregular than upper, are typical for carbonate crusts formed in continental environment.
These features are ubiquitous in these youngest Devonian deposits and indicate that almost all the dolostone sequence of the Nīkrāce Member is dolocrete – carbonate crust formed in continental settings under arid climate conditions. The above data show that it corresponds to dolomitized alpha calcrete, which are dominated by micrite (very fine carbonate material), contains large dolomitised calcite rhombo hedra and there is almost no influence of organisms.
Fig. 1. Fragment of dolostone (Nīkrāce Member, Šėervelis Formation, Upper Devonian) exposure at mouth of the River Lētīža
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Fig. 2. Cellular structure of dolostone in Fig. 3. Reverse grading of pisoids (upper part of exposure at the River Lētīža mouth. “Cells” are photograph) in a dolostone macro sample from empty due to weathering; originally they are exposure at the River Lētīža mouth (photo by Ints filled with clay, which contains paligorskite Indāns)
Fig. 4. Thin section photomicrograph: Dolomite pisoids and intraclasts (rounded grains) with bridge like contacts indicated by arrows. Light brownish grey inclusions are quartz (fine sand) grains. Thin section is made of dolostone from exposure at the River Lētīža mouth (photo by Ints Indāns)
Carbonate crusts are exception in the Devonian sequence on the Main Devonian Field (Baltic States, north western part of Russia, northern part of Belarus and other neighbouring areas) which have formed mostly in a shallow sea. However, these crusts give opportunity to trace episodes of regressions of the Devonian basins, which are not apparent in other way.
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FOR NOTES
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