The quarry in Dzikowiec as a geotouristic site and its importance for studies on the Upper Paleozoic in the Sudetes

Tags: Dzikowiec, Lower Carboniferous, Pal, Upper Devonian, Bardo Unit, Berlin, marine sediments, Tournaisian, Gattendorfia, sandstones, Central Sudetes, Klodzko Metamorphic Unit, metamorphic rocks, Bederke, Wapnica Hill, grey limestone, The History of Geological Studies, Liegendes des oberdevonischen Kalkes von Ebersdorf bei Neurode, Upper Paleozoic, Institute of Geological Sciences, Wroclaw, Blat Neurode, Materialy Konferencji Terenowej Nowa Ruda, Schlesien, Wapnica Formation
Content: The quarry in Dzikowiec as a geotouristic site and its importance for studies on the Upper Paleozoic in the Sudetes Kamieniolom w Dzikowcu jako obiekt geoturystyczny i jego znaczenie dla bada utworуw gуrnego paleozoiku w Sudetach Jolanta Muszer1, Joanna Haydukiewicz1 1University of Wroclaw, Institute of geological sciences, Cybulskiego 30, 50-204 Wroclaw, Poland e-mail: [email protected]; [email protected] Abstract: The Dzikowiec quarry, which is situated in the north-western part of the Bardo Unit (Central Sudetes), includes a very interesting sequence of Upper Devonian and Lower Carboniferous marine sediments. Exposed an autochtonic succession has been subjected to geological and paleontological studies since over 200 years. It is one of a few European exposures where the continuous deposition at the Devonian/Carboniferous boundary can be observed. These sediments are famous among geologists for the abundance of fossils: algae, stromatopores, foraminifers, conodonts, ammonites as well as crinoids, ostracods, brachiopods and more rare gastropods and trilobites. The quarry is a common stop for conference trips and field training grounds for students, but it is an undervalued geotouristic site. Key words: Sudetes, Devonian and Carboniferous marine sediments, lithostratigraphy, biostratigraphy, geotouristic site Tre: W kamieniolomie w Dzikowcu, poloonym w pуlnocno-zachodniej czci jednostki bardzkiej, odslania si bardzo interesujcy profil morskich utworуw gуrnego dewonu i dolnego karbonu. Badania geologiczne i paleontologiczne tego autochtonicznego profilu prowadzone s od ponad 200 lat. Jest to jedno z niewielu miejsc w Europie, gdzie obserwowa mona ciglo sedymentacyjn na granicy dewon/karbon. Osady te s znane w rodowisku geologicznym jako obfite rуdlo skamienialoci: glonуw, stromatoporуw, otwornic, konodontуw i amonitуw, a take liliowcуw, maloraczkуw, ramienionogуw i rzadszych limakуw oraz trylobitуw. Kamieniolom jest popularnym punktem wycieczek konferencyjnych oraz studenckich wicze terenowych, ale jest niedoceniany jako obiekt geoturystyczny. Slowa kluczowe: Sudety, osady morskie dewonu i karbonu, litostratygrafia, biostratygrafia, obiekt geoturystyczny 243
Introduction and Geological Setting The Devonian and Carboniferous marine sediments exposed in the Dzikowiec quarry have been studied by geologists since over 200 years. It is one of a few European exposures and the only one in the Sudetes where the continuous deposition at the Devonian/Carboniferous boundary can be observed but it is still undervalued as a geotouristic site. This paper deals with the history of investigations of the deposits and their significance for a stratigraphical record of the Upper Paleozoic in the Sudetes. The Dzikowiec quarry is situated south to the Sowie Mts., at the north-western margin of the Bardo Mts., near Dzikowiec elevation (Fig. 1), on the western slope of the Wapnica Hill (579.6 meters a.s.l.), about 300 meters to the south-east from Dzikowiec village (formerly Ebersdorf). Geologically, the quarry is located in the Central Sudetes (Fig. 2), in the north-western part of the Bardo Unit (Fig. 3). The Bardo Unit borders the Metamorphic Rocks of the Sowie Mts. Block, the Lower Permian of the Czerwieczyce Graben, which belongs to the Intra-Sudetic Basin, the Paleozoic metamorphic rocks of the Klodzko Metamorphic Unit and the Variscan granitoids of the Klodzko­Zloty­Stok Massif. Its north-eastern border is the Sudetic Marginal Fault. The Bardo Unit consists mainly of Lower Carboniferous Sedimentary Rocks and some deposits representing a vast time span, from at least Late Ordovician to Fig. 1. The topographic map of the vicinity of Dzikowiec 244
Fig. 2. Geological sketch of the Sudetes (after Aleksandrowski et al., 1997); BU ­ Bardo Unit, DG ­ Doboszowice gneiss, ISF ­ Intra-Sudetic Fault, KCU ­ Kamieniec Unit, KG ­ Kudowa granite, KU ­ Klodzko Metamorphic Unit (Complex), KZG ­ Klodzko-Zloty Stok granitoids, NZ ­ Niemcza Zone, LG ­ Lusatian granitoids, SBF ­ Sudetic Boundary Fault, SSG ­ Strzegom-Sobуtka granitoids. SZ ­ Skrzynka Shear Zone; B ­ wiebodzice Basin. Inset map: hachured ­ pre-Permian crystalline rocks; EFZ ­ Elbe Fault Zone, ISF ­ Intra-Sudetic Fault, MGH ­ Mid-German Crystalline High, MO ­ Moldanubian Zone, MS ­ Moravo-Silesian Zone, NP ­ Northern Phyllite Zone, OFZ ­ Odra Fault Zone, RH ­ Rhenohercynian Zone, SX ­ Saxothuringian Zone, TB ­ Teplб-Barrandian Zone. Age assignments: Pt3 ­ Late Proterozoic; Cm ­ Cambrian; Or ­ Ordovician; D ­ Devonian; C ­ Carboniferous; Pz1 ­ Early Palaeozoic. Rectangle shows the location of Fig. 3. earliest Late Carboniferous. Its lithological column does not represent either single or continuous stratigraphic sequence. According to Wajsprych (1986, 1995), two sequences are present: autochthonous and allochthonous. The latter forms olistoliths of Ordovician, Silurian and Devonian age embedded in the flysch and wild flysch deposits of the uppermost part of the autochthonous sequence. The autochthonous (parautochthonous) Upper Devonian ­ Lower Carboniferous platform-to-foreland succession is composed of carbonates and several, facially differentiated series. According to Wajsprych (1995), the sediments of the allochthonous succession were thrusted over the platform deposits in the late stages of platform development, probably after the crenistria Chron. This idea of lithostratigraphy of the Bardo Unit significantly differs from the alternative, older 245
Fig. 3. Generalized geological map of the Bardo Unit (after Haydukiewicz, 2002, modified). 1 ­ Lower Permian sedimentary and volcanic rocks; 2 ­ Variscan granitoids of Klodzko­Zloty Stok massif; 3 ­ Upper Carboniferous sedimentary rocks; 4 ­ Lower Carboniferous clastic rocks; 5 ­ Lower Carboniferous Carbonate rocks; 6 ­ Upper Devonian limestones; 7 ­ olistoliths of Devonian rocks; 8 ­ olistoliths of Upper Ordovician and Silurian rocks; 9 ­ Palaeozoic metamorphic rocks of the Klodzko Metamorphic Unit; 10 ­ Upper Proterozoic-Lower Palaeozoic high-grade metamorphic rocks of the Sowie Mts. Block; 11 ­ faults and thrusts; 12 ­ locality of the Dzikowiec quarry. proposal of "autochthonous" permanent development of the geosynclinal basin lasting since the Late Ordovician up to the latest Early Carboniferous, which was proposed by Oberc (1957, 1972). The Palaeozoic succession of the Bardo Unit was folded at the turn of Early/Late Carboniferous and intruded by the Variscan Klodzko­Zloty Stok Pluton (Oberc, 1972). The Dzikowiec quarry was developed in the 18th century. It has been abandoned for a tens years. Recently, it is about 500 meters long and about 150 meters wide (Fig. 4). The quarry includes a very interesting succession of Upper Devonian and Lower Carboniferous marine sediments (from Upper Frasnian to 246
Tournaisian and probably Lower Visean), which represents a lower part of the autochthonous succession of the Bardo Unit. The History of Geological Studies The history of investigations of the exposed succession has over 200 years. The first general description of rocks forming the Wapnica Hill was published by von Buch (1797; fide Oberc, 1957). Intensive geological and paleontological studies of rocks from Dzikowiec quarry has Fig. 4. Sketch-map of the Dzikowiec quarry (after Mazur, started when von Buch (1839) 1987, modified). 1 ­ borders of the quarry; 2 ­ road; 3 ­ found first goniatites and clyme- fault, 4 ­ buildings. nids. These were the first Devonian ammonites described from the area of recent Poland (see Berkowski, 2001). Tietze (1870) was the first who distinguished two horizons: lower clymenid limestone and upper shale and graywackes of the Kulm facies. Next, he found fossils: corals, brachiopods, pelecypods, gastropods, cephalopods and ostracods in the main limestone (Tietze, 1871). In the 19th and at the beginning of the 20th centuries several concepts were developed on stratigraphy, tectonics and paleontology of exposed rocks (Gьrich, 1900, 1902; Dathe, 1901, 1904; Frech, 1902; Bederke, 1924; Schindewolf, 1920, 1921, 1923, 1937). Gьrich (1900, 1902) described Spherocodium zimmermanni in the lower part of carbonate sequence and recognized it as the Frasnian. Dathe (1901, 1904) acknowledged a discordance between gneissic sandstones and clymenid limestones, and explained it in terms of a sedimentary gap at the Devonian/Carboniferous boundary, while Frech (1902) described the ammonites. A litostratigraphical division of deposits from Dzikowiec was proposed by Bederke (1924). He distinguished some units in the stratigraphical order: gabbro breccia, basal beds, main limestone and clymenid limestone, and tried to estimate their thickness. Schindewolf (1920, 1921, 1923, 1937) continued an intensive paleontological investigations, especially of goniatites and clymeniids, but the majority of his specimens was found on the dumps. He assigned clymenid limestone to the Wocklumeria "Stufe" and grey limestone with goniatites to the Gattendorfia "Stufe" (Schindewolf, 1937). Further research contributed to precise determination of the age, biostratigraphy, types and number of deformations and interpretation of depositional en- 247
Fig. 5. Generalized lithostratigraphic section of the Dzikowiec quarry (after Haydukiewicz, 1990, modified) vironments (Oberc, 1957, 1972; Lewowicki, 1959; Weyer, 1965; Freyer, 1968; Chorowska, 1974, 1979; Wajsprych, 1986, 1995; Chorowska, Radlicz, 1987; Mazur, 1987; Dzik, 1997; Haydukiewicz, 1990; Streel et al., 2004; Korn et al., 2005) as well as paleotemperatures (Haydukiewicz, 2002). Paleontological investigations of ammonites were continued by Lewowicki (1959), Weyer (1965), Dzik (1997) and Korn et al. (2005). First studies of conodonts from the Dzikowiec were carried on by Freyer (1968) and were continued by Chorowska (1974, 1979), and Dzik (1997). These authors included the exposed Devonian and Carboniferous sediments into the standard conodont zones. Haydukiewicz (2002) determined the CAI (Color Alteration Index) values of conodonts from Clymenia and Gattendorfia limestones. The low CAI values (1.5) found in conodonts from both limestones suggest that the rocks were heated at temperature range of 50­90 °C (Haydukiewicz, 2002). Recently, Muszer (2007) published mineralogical and microtextural characteristics of accessory minerals and spherule-shaped forms from the rocks of the Dzikowiec succession. He ascertained the similar composition of accessory minerals (pyrite-marcasite, goethite, rutile-anatase-titanite spherules, zircon, magnetite, aggregate of Fe-Cu-Zn sulphides, native gold and native iron) in 248
Fig. 6. Outcrops of gabbro and limestone breccia in the central part of the Dzikowiec quarry (western wall) the Clymenia limestone, grey clay slate, Gattendorfia limestone and the yellow bed above the last one. The features of Ni-bearing and Cr-bearing native iron, which are accompanied by Zn-bearing chromite, monazite and large graphitic aggregates connected with pyrite framboides as well as the occurence of kamzite egzoclasts may indicate its meteoritic origin and deposition at the Famennian/Tournaisian boundary. Mixing of the cosmogenic and volcanogenic fall-out cannot be exluded in the case of the described stratigraphic condensate from Dzikowiec (Muszer, 2007). Lithostratigraphy and Biostratigraphy The lithostratigraphy of sediments from the Dzikowiec quarry includes three informal units named "formations" by Wajsprych (1995). These are in the stratigraphic order: Wapnica Formation, Gologlowy Formation and Nowa Wie Formation (Fig. 5). The Wapnica Formation is composed of marine carbonates: gabbro and limestones breccia, basal limestone, main limestone, Clymenia and Gattendorfia limestones. These sediments are about 60 meters thick and represent the Upper Devonian and the Lowest Tournaisian. In the study area the 249
Fig. 7. The eastern wall of the central part of the Dzikowiec quarry with outcrops of main limestone and gneissic sandstones and conglomerates. ml ­ main limestone; gsc ­ gneissic sandstones and conglomerates Gologlowy Formation is represented by fragmentary preserved Black SHAles. The shales are overlain by the Nowa Wie Formation, which comprises gneissic sandstones and conglomerates, and calcareous deposits. The calcareous deposits, formerly known as the Lower Carboniferous or coaly limestone ("Kohlenkalk"), are exposed on the northern slope of Wapnica Hill, but not in the quarry. The Nowa Wie Formation is over 200 m thick and is of Early Carboniferous age (from Tournaisian to probably Visйan). Now, in various parts of the quarry we can observe only its lower part. Furthermore, the intensive block tectonics makes correlation of these units rather difficult. The oldest strata probably belong to the upper part of the Frasnian (Gьrich, 1902; Bederke, 1929). These are represented by gabbro and limestones breccia, which belong to the the central part of the quarry, in its western wall (Fig. 6). Together with the overlying basal limestone of the lower part of the Famennian these sediments are 15 meters thick (Fig. 5). The breccia is composed of very intensively, primarily weathered gabbro blocks (up to 1 meter across) embedded within organodetrital limestone, which contains abundant algae filaments, foraminifers, brachiopods, poorly preserved corals (Scruttonia) and stromatopo- 250
Fig. 8. The northern part of the Dzikowiec quarry with outcrops of the Clymenia and Gattendorfia limestones (Wapnica Formation). Cl ­ Clymenia limestone; Gal ­ Gattendorfia limestone Fig. 9. The northern part of the quarry with outcrops of Clymenia and Gattendorfia limestones (Wapnica Formation). Cl ­ Clymenia limestone; Gal ­ Gattendorfia limestone 251
Fig. 10. The northern part of the Dzikowiec quarry ­ outcrop of shales of the Gologlowy Formation (GFm) roids (Berkowski, 2001). According to Wajsprych (1995), the stromatoporoidal coats on gabbro blocks indicate very shallow sedimentary environment (up to subaerial exposure). Permanent tectonic destruction of the basin floor and its sedimentary cover is recorded by development of polycyclic breccia. An extensional regime of that process is indicated by a network of open fractures (neptunian dykes) filled with laminated, light-grey carbonates, probably originating from low-temperature hydrothermal activity (Wajsprych, 1995). The basal limestone is exposed in the southern part of the quarry. It is a grey, mostly biosparitic limestone, in part irregularly bedded, with fragments of gabbro, granitoids and serpentinites (Wajsprych, 1986). It contains numerous algal and stromatoporoid elements, some corals, brachiopods and crinoid fragments, which are typical of the lower part of the Famennian (Bederke, 1929; Wajsprych, 1995). The next lithostratigraphic unit ­ the main limestone ­ appears on the eastern wall of the central part of the quarry (Fig. 7). It is about 40 meters thick and is represented by regularly thin-bedded, grey biosparite and calcarenite limestone, nodular at the top, interbedded with dark-grey, 1.0 to 3.0 cm thick layers of marly siltstone (Haydukiewicz, 1990; Wajsprych, 1995). The main limestone 252
Fig. 11. The northern part of the Dzikowiec quarry ­ outcrop of gneissic sandstones and conglomerates (Nowa Wie Formation) contains: algae, cyanobacteria, stromatoporoids, benthic foraminifers, crinoids, ostracods, small brachiopods, gastropods and corals (Tietze, 1871; Berkowski, 2001; Streel, 2004). However, its Late Devonian age was determined by means of conodonts (Freyer, 1968; Chorowska, 1979). The discussed limestone embraces conodont zones from the marginifera to the Lower expansa, which corresponds to the middle part of the Famennian. The uppermost part of the main limestone contains foraminifers from zones Df3 and Df3 (Streel et al., 2004). These sediments were deposited probably in shallow water of neritic zone. In the northern part of the quarry the Clymenia and the Gattendorfia limestones appear (Figs 8, 9). The Clymenia limestone is pink or grey nodular biomicrite of about 2­3 meters thick. It represents the Upper Famennian "Wocklumeria" (Stufe) stage. It contains Late Famennian clymeniids and goniatites fauna (Schindewolf, 1937; Lewowicki, 1959). The most abundant ammonites belong to Kosmoclymenia, Soliclymenia and Sporadoceras genera. This limestone also contains conodonts, which represents interval from the Middle expansa to the Lower praesulcata zones (Freyer, 1968; Chorowska, 1979; Streel et al., 2004). According to Wajsprych (1995), the Clymenia (cephalopod) limestone sedimen- 253
tation had to be strongly restricted to the Wapnica rise, which explains why it is known exclusively from the Wapnica section. The Clymenia limestone is separated from the Gattendorfia limestone by a thin layer (1­5 cm thick) of black clayey shale (Fig. 9). The shale is probably stratigraphically condensed and corresponds to the uppermost Famennian and the lowermost Tournaisian (Haydukiewicz, 1990), being an equivalent of the Hangenberg Shales. The uppermost part of the carbonate series in the Dzikowiec succession is represented by the Gattendorfia limestone. It is a grey, nodular biomicrite of Early Tournaisian age, actually only 1.5 m thick. It belongs to the Gattendorfia crassa ammonite zone (Weyer, 1965) and the sulcata ­ triangularis conodont zones (Dzik, 1997), i.e. it represents the Lower Tournaisian. The most complete exposure is located at the southern end of the quarry, to the right and above the gallery (Mazur, 1987). The Gattendorfia limestone contains abundant and highly diversified conodonts and ammonites (prionoceratids, gattendorfiids, prolecanitids, pseudarietitines, for details see Dzik, 1997). According to Wajsprych (1995), the Gattendorfia limestone is the deepest-water sediment of the Wapnica Formation deposited under calm conditions and it records the beginning of the facies unification in the basin. Both the Famenian and the Tournaisian limestones represent carbonate platform sediments. These limestones contain rich taphocoenoses composed mainly of the nektonic organisms (ammonites and conodonts) but fossils of benthic fauna appear much rarely. The domination of the nektonic fauna and the presence of palmatolepid-bispathodid conodont biofacies (Rudyk, 2002, unpublished data) indicate the relatively deep-water conditions of their deposition. The carbonates are covered by the fragmentary preserved black shales of the Gologlowy Formation (Fig. 10), which are dark-gray or black, siliceous and clayey shales containing the Early Tournaisian conodonts (Haydukiewicz, 1990). The shales exposed in the Dzikowiec quarry are several centimeters thick but perhaps more than one meter thick in the SE part of the quarry (Haydukiewicz, 1990; Dzik, 1997). Close to the limestone, the shales become yellowish and host a discontinuous, 3­5 cm thick, irregular limestone layer (Dzik, 1997). The black shales of the Gologlowy Formation marks a climax of the basin deepening and its unification (Wajsprych, 1995). The shales of the Gologlowy Formation are discordantly overlain by gneissic sandstones and conglomerates of the Nowa Wie Formation (Fig. 11). Its thickness in the Dzikowiec area reaches several tens of meters. The gneissic detritus was undoubtedly derived from the Sowie Mts. Block (see Haydukiewicz, 1990). The abovementioned rocks underlay the Lower Carboniferous Limestone, which are not exposed in the quarry except for the lowermost part of the Nowa Wie Formation. Chronostratigraphically, it may represent the uppermost part of the Tournaisian or the lowermost part of the Visean (Haydukiewicz, 1990; Gluszek, Toma, 1993). 254
Conclusions The Dzikowiec quarry is one of a few European exposures and the only one in the Sudetes, where the relict depositional continuity at the boundary between Devonian and Carboniferous systems can be observed. The section is complete enough to show the original, undisturbed fossils succession. Due to its scientific value, including the abundance of fossils (algae, stromatopores, foraminifers, conodonts, ammonites, crinoids, ostracods, brachiopods and more rare gastropods and trilobites), it belongs to exposures most commonly visited by geologists and paleontologists. In this quarry many conference trips and field training grounds for students were organized. In the southern part of the quarry the gallery is situated, which was famous especially among treasure hunters. They believed that gold once deposited in banks in Wroclaw was hidden in the quarry, same as arms and equipment of the "Wehrwolf" organization. Nowadays, in the quarry a shooting range is situated. As a geotouristic site, the quarry is undoubtedly underestimated by visitors despite its valours (Slomka et al., 2006), which are: picturesque landscape, contact with inanimated nature and discovery of fossils specimens. In the Dzikowiec village, which has been founded in the early 14th century, tourists can visit several valuable Historical Monuments. The oldest preserved buildings are the 17th manor house and 17th St. Marin church. Two chapels from 19th century are also preserved. The village is surrounded by hills, which are mostly overgrown with pastures or cropfields and locally with forests. References Aleksandrowski P., Kryza R., Mazur S., aba J., 1997. Kinematic data on major Variscan strike-slip faults and shear zones in the Polish Sudetes, northeast Bohemian Massif. Geol. Mag., 133: 727-739. Bederke E., 1924. Das Devon in Schlesien und das Alter der Sudetenfaltung. Fortschr. Geol. Palдont., 2, 7: 1-50. Bederke E., 1929. Die varistische Tektonik der mittleren Sudeten. Fortschr. Geol. Palдont., 7, 23: 429-523. Berkowski B., 2001. Geologia i paleontologia Dzikowca. W: Paleontologiczne oprуbkowanie profilуw geologicznych. Kurs terenowy 18­20 maja 2001 roku. Inst.Paleobiol. PAN: 7-12 Buch L., von, 1839. ber Goniatiten und Clymenien in Schlesien. Physik. Abh. der kцnig. Akad. der Wissenschaft., Berlin: 149-169. Chorowska M., 1974. Dewon gуrny okolic Klodzka w wietle bada konodontowych. Kwart. Geol. 18: 900-901. Chorowska M., 1979. Nowe wyniki bada stratygraficznych dewonu okolic Klodzka i problem granicy dewon/karbon. [In:] Wybrane zagadnienia stratygrafii, petrografii i tektoniki wschodniego obrzeenia gnejsуw sowiogуrskich i metamorfiku klodzkiego. Materialy Konferencji Terenowej Nowa Ruda, 8­9.09.1979, Wroclaw University: 143-152. Chorowska M., Radlicz K., 1987. Wapienie gуrnego dewonu i dolnego karbonu w kamieniolomie na gуrze Wapnica w Dzikowcu. [In:] Przewodnik LVIII Zjazdu PTG Walbrzych 17­19 wrzenia 1987r (red. Baranowski et al.), Krakуw: 188-190. Dathe E., 1901. Die Lagerungsverhдltnisse des Oberdevon und Culm am Kalkberge bei Ebers- 255
dorf in Schlesien. Jb. kgl. Preuss. Geol. Landesanst., Berlin, 21: 214-237. Dathe E., 1904. Erlдuterungen zur Geologischen Karte von Preussen und benachbarten Bun- desstaaten. Lief. 115; Blat Neurode; Berlin: 3-44. Dzik J., 1997. Emergence and succession of Carboniferous conodont and ammonoid communi- ties in the Polish part of the Variscan sea. Acta Palaeont. Polon., 42: 57-170. Frech F., 1902. Ьber devonische Ammoneen. Beitrдge zur Palдontologie und Geologie des Цsterreich-Ungarns und des Orients. 14: 27-112. Freyer G., 1968. Conodontenfunde aus dem Oberdevon und Unterkarbon von Dzikowiec Klodzki (Ebersdorf) und Gologlowy (Hollenau) in Dolny lsk (Niederschleisien). Geologie, Berlin, 17, 1: 60-67. Gluszek A., Toma A., 1993. Age of the Nowa Wie Formation (Bardzkie Mts., Middle Sudetes, SW Poland). Ann.Soc. Geol. Pol., 62, 3-4: 293-308. Gьrich E., 1900. ber Gabbro im Liegendes des oberdevonischen Kalkes von Ebersdorf bei Neurode in der Grafschaft Glatz., Ztschr.d.Dtsch.Geol.Ges., 52, Berlin: 14-23. Gьrich E., 1902. Zur Diskussion ьber das Profil von Ebersdorf., Ztschr.d.Dtsch.Geol.Ges., Berlin, 54: 57-65. Haydukiewicz J., 1990. Stratigraphy of Paleozoic rocks of the Gуry Bardzkie and some remarks on their sedimentation (Poland). Neue Jahrbuch Geol. Palдont. Abh., 179, 2/3: 275-284. Haydukiewicz J., 2002. Zakres przeobrae termicznych konodontуw i skal dewosko-dolnokarboskich Gуr Bardzkich. Acta Univer. Wratisl. Prace Geol.-Miner., LXXII. Wroclaw: 1-30. Korn D., Niedwiedzki R., Posieczek J.B., 2005. Age, distribution and phylogeny of the peculiar Late Devonian ammonoid Soliclymenia. Acta Geol. Polon., 55, 2: 99-108. Lewowicki S., 1959. Fauna wapieni klimeniowych z Dzikowca Klodzkiego [Fauna of Clymenia limestones from Dzikowiec near Klodzko (Sudety)]. Instytut Geologiczny Biuletyn, Warszawa, 146, 7: 73­118. Mazur S., 1987. Tektonika utworуw gуrnego dewonu i dolnego karbonu w kamieniolomie w Dzikowcu (Gуry Bardzkie). Przegld Geologiczny, 35: 327-332. Muszer A., 2007. Charakterystyka sferul i mineralуw akcesorycznych z wybranych utworуw fanerozoicznych i antropogenicznych. [Characteristic of spherules and accessoric minerals from selected Phanerozoic and anthropogenic sediments]. In Polish, with English summary. Fundacja Ostoja, Wroclaw: 355 pp. Oberc J., 1957. Region Gуr Bardzkich (Sudety). Przewodnik dla geologуw. Wydawnictwa Geologiczne, Warszawa: 218 pp. Oberc J., 1972. Sudety i obszary przylegle. W: Budowa Geologiczna Polski, 4. Tektonika, 2. Pastw. Inst. Geol., Warszawa: 143-179. Rudyk K., 2002. Biostratygrafia i biofacje konodontowe gуrnodewoskich wapieni w profilu Dzikowca. MSc thesis, University of Wroclaw, Library of Institute of Geological Sciences: 123 pp. Schindewolf O.H., 1920. Neue Beitrдge zur Kenntnis der Stratigraphie und Palдontologie des deutschen Oberdevons, Senckenbergiana, 2, Frankfurt am Main: 114-129. Schindewolf O.H., 1921. Versuch einer Palдogeographie des Europeischen Oberdevonmeeres. Z.Deutsch.Geol.Ges., Berlin, 73: 137-223. Schindewolf O.H., 1923. Beitrдge zur Kenntnis des Palдozoikums in Oberfranken, Ostthьringen und dem Sдchsischen Vogtlande, I. Stratigraphie und Ammoneenfauna des Oberdevons von Hof a.S. Neues Jb.Mineral. Geol. Palдont., Stuttgart, 49: 250-357, 393-509. Schindewolf O.H., 1937. Zur Stratigraphie und Palдontologie der Wocklumer Schichten (Oberdevon). Abh.der Preuss. Geol. Landesanst. N. F., Berlin, 178: 1-132. Slomka T., Kiciska-widerska A., Doktor M., Joniec A., (eds.), 2006. Katalog obiektуw geoturystycznych w Polsce. Krakуw: 16-17. Streel M., Belka Z., Dreesen R., Durkina A. V., Groos-Uffenorde H., Hance L., Hartkopf-Frцder 256
C., Haydukiewicz J., Korn D., Perri M. C., Piecha M., Spalletta C., 2004. Relation of the neritic microfaunas and continental microfloras with the conodont and other pelagic faunas within the latest part of the Famennian. SDS Annual Meeting Rabat, March 1 and 2, 2004: 67-73. Tietze E., 1871. Ьber die devonischen Schichten von Ebersdorf unweit Neurode in der Grafschft Glatz, eine geognostisch-palдontologische Monographie. Palaeontographica, 19: 103-158. Wajsprych B., 1986. Sedimentary record of tectonic activity on a Devonian-Carboniferous continental margin, Sudetes. In: IAS 7th Europ. Region. Meet. Excurs. Guidebook Krakуw -Poland. Wroclaw: 141-164. Wajsprych B., 1995. The Bardo Mts rock complex: The Famennian ­ Lower Carboniferous preflysch (platform) ­ to flysch (foreland) basin succession, the Sudetes. [In:] Guide to Excursion B2 of XIII Inter. Congr. on Carboniferous-Permian 28.08­02.09. Krakуw, Warszawa: 23-42. Weyer D., 1965. Zur Ammonoideen-Fauna der Gattendorfia-Stufe von Dzikowiec (Ebersdorf) in Dolny lsk (Niederschleisen), Polen. Berichte der geologischen Gesellschaft der DDR, 10, 4: 443-464. Podsumowanie Odslonicie utworуw dewonu i karbonu w kamieniolomie w Dzikowcu jest przedmiotem bada geologicznych od ponad 200 lat, gdy jest to jedno z nielicznych w Europie i jedyne w Sudetach miejsce, gdzie obserwowa mona ciglo sedymentacji na granicy dewon/karbon. Osady te podzielone zostaly na trzy nieformalne jednostki ("formacje"): Wapnicy, Gologlуw i Nowej Wsi (Wajsprych,1995). Formacja Wapnicy obejmuje morskie osady gуrnego dewonu i najniszego turneju: brekcje gabrowe i wapienne, wapie podstawowy, wapie glуwny, wapie clymeniowy i wapie gattendorfiowy, o miszoci ok. 60 m. Formacja Gologlуw reprezentowana jest przez fragmentarycznie zachowane czarne lupki. Formacja Nowej Wsi to piaskowce i zlepiece gnejsowe oraz osady wapienne (wapie wglowy), o miszoci ponad 200 m, nalece do dolnego karbonu (turnej, prawdopodobnie wizen). W kamieniolomie odslonita jest tylko najnisza cz tego profilu. Profil osadуw ukazuje niezaburzone nastpstwo skamienialoci o wielkiej wartoci naukowej. Mona tu znale glony, stromatopory, otwornice, konodonty, amonity, liliowce, maloraczki, ramienionogi oraz rzadsze limaki i trylobity. Ze wzgldu na warto naukow kamieniolom w Dzikowcu jest czsto odwiedzany przez geologуw i paleontologуw. Jest te popularnym punktem wycieczek konferencyjnych oraz studenckich praktyk terenowych. Pomimo wartoci naukowych, dydaktycznych i turystycznych: odslonitych skal, zawartych w nich skamienialoci, a take malowniczego krajobrazu (Slomka et al., 2006), kamieniolom w Dzikowcu jest niedoceniany jako obiekt geoturystyczny. Ponadto we wsi Dzikowiec, zaloonej na pocztku XIV w., znajduj si ciekawe zabytki: dwуr i kociуl z XVII w. 257

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