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A new Lower Coniacian fauna from the Jerzmanice Zdrój region of the North Sudetic Basin, SW Poland
Abstract
This paper describes and interprets a newly discovered Lower Coniacian (lower Upper Cretaceous) macro- and microfossil fauna (vertebrate and invertebrate remains) from sedimentary rocks of the Jerzmanice Zdrój region of the North Sudetic Basin of SW Poland. Several inoceramid bivalve taxa that previously were only known from other parts of the North Sudetic Basin were recovered from light grey, marly sandstones of Early Coniacian age. A fragment of ammonite was also discovered, as was a shark's tooth from the family Cretoxyrhinidae: this may be ?Cretoxyrhina mantelli Agassiz, 1843, a species not hitherto known from the Lower Coniacian (Emscherian sensu Scupin (1912-13)) of the North Sudetic Basin. Abundant foraminifers were observed in thin sections. The newly discovered inoceramid bivalves - Cremnoceramus deformis erectus Meek, 1877, Cremnoceramus waltersdorfensis waltersdorfensis Andert, 1911 and Inoceramus lusatiae Andert, 1911 - fit into the current biostratigraphic scheme for the region. The inoceramids can all be as - signed to the Cremnoceramus deformis erectus Zone, which correlates with the Gavelinella moniliformis foraminiferal Zone and thereby confirms an Early Coniacian age. The Turonian-Coniacian boundary in the North Sudetic Basin can now be placed between the respective inoceramid zones of Inoceramus costellatus Woods, 1912 (actually Mytiloides costellatus Woods, 1912) and Inoceramus schlśnbachi Böhm, 1911 (actually Cremnoceramus crassus crassus Petrascheck, 1903). The macrofossils found in the Jerzmanice section suggest that the host sediments were laid down in a Late Cretaceous epicontinental basin, under the North Sudetic Sea, that had deepened during the Early Coniacian. This interpretation agrees with the global bathymetric curve for the Late Cretaceous in Europe.
... The quartz sandstones are interpreted as bar and storm deposits, which were mainly deposited in the foreshore/ upper shoreface (Leszczyński, 2010). The stratigraphy of the Upper Cretaceous deposits is based predominantly on inoceramid bivalves (Walaszczyk, 1992(Walaszczyk, , 2008Chrząstek, 2008;Walaszczyk & Wood, in press), but also on other biota (e.g., foraminifera, cephalopods and echinoids; see Walaszczyk et al., 2016). According to Milewicz (1979Milewicz ( , 1985Milewicz ( , 1997, these sandstones are of early Coniacian age, a hiatus comprising the middle Coniacian. ...
... Andert (1934) cited Lima haidingeri from the same quarries as above, from the Coniacian at Żeliszów Quarry and from the Upper Cretaceous of Rakowice Małe and Żerkowice and Austria. ?Lima haidingeri has also been described from the Coniacian at Jerzmanice Zdrój (North Sudetic Synclinorium; Chrząstek, 2008). ...
The Coniacian quartz sandstones (Żerkowice Member, Rakowice Wielkie Formation) that crop out at quarries near Czaple-Nowa Wieś Grodziska (North Sudetic Synclinorium) contain a low-diversity assemblage of trace fossils: Gyrochorte isp., Ophiomorpha nodosa Lundgren, 1891, Ophiomorpha isp., Phycodes cf. curvipalmatum (Pollard, 1981), ? Phycodes isp., Planolites cf. beverleyensis (Billings, 1862), Thalassinoides paradoxicus Woodward, 1830 and ? Thalassinoides isp. Moreover, interesting compound burrow systems, here referred to as Thalassinoides - Phycodes cf. palmatus and ? Thalassinoides - Phycodes , were recognised at the Czaple Quarry. Additionally, ? Gyrochorte isp., Phycodes cf. flabellum (Miller and Dyer, 1878) and ? Treptichnus isp. were encountered at correlative levels in the Rakowice Małe Quarry. Some of these ichnotaxa have not been recorded previously from Coniacian sandstones of the Żerkowice Member. Additionally, in slabs of these sandstones, the gastropod Nerinea bicincta Bronn, 1836 and the bivalve Lima haidingeri Zittel, 1866 were found. These interesting finds, in particular the gastropods, were already noted from the study area in the first half of the twentieth century by Scupin (1912–1913). Ethologically, the trace fossil assemblage is represented by domichnia or domichnia/fodinichnia ( Ophiomorpha , Thalassinoides ), fodinichnia ( Phycodes ) and pascichnia ( Gyrochorte , Planolites ). The compound burrow systems ( Thalassinoides - Phycodes ) are interpreted as dwelling/feeding structures. The possible tracemakers are crustaceans ( Ophiomorpha , Thalassinoides ) or worm-like animals (annelids and other) ( Planolites , ? Phycodes , Gyrochorte and ? Treptichnus ). The assemblage of trace fossils is characteristic of the Skolithos ichnofacies and Cruziana ichnofacies, typical of shallow-marine settings. Ichnological studies, as well as the presence of accompanying fossils (bivalves, gastropods), confirm the palaeoenvironmental reconstruction of the Żerkowice Member sandstones by Leszczyński (2010). That author interpreted the Coniacian sandstones as bar and storm deposits laid down in a shallow epicontinental sea (mainly the foreshore-upper shoreface; up to the middle shoreface) under normal oxygenation and salinity, in soft substrate, above fair-weather wave base. The deposition of the Żerkowice Member sandstones is linked to a regression that started after uplift of the southeastern part of the North Sudetic Synclinorium.
... Kędzierski (2005) noticed that the Turonian, as understood by the authors, comprised also a part of the Coniacian. A similar situation occurred in the North Sudetic Synclinorium (Chrząstek, 2008a). This may have resulted in erroneous datings of sediments that contain I. cuvieri. ...
The ammonites Lewesiceras peramplum Mantell
and ?Lewesiceras sp. are reported from the
Upper Cretaceous in the Nysa Kłodzka Graben; they date from the
Middle Turonian and ?Coniacian, respectively. The Middle Turonian
limestones of the Stara Bystrzyca quarry contain an abundant assemblage
of inoceramids ( Inoceramus cuvieri Sowerby
and I. lamarcki Parkinson) and other bivalves, including oysters, as
well as brachiopods and trace fossils. Micropalaeontological data show
the presence of foraminifers and siliceous sponge spiculae, bryozoans,
ostracods and fragments of bivalves and gastropods. The Middle Turonian
calcareous deposits belongs to the upper part of the
Inoceramus lamarcki Zone (late Middle
Turonian) and were deposited on a shallow, subtidal offshore shelf. They
overlie the Middle Turonian Bystrzyca and Długopole Sandstones,
which represent foreshore-shoreface delta deposits. The fossil
assemblage suggests a moderate- to low-energy, normal-salinity
environment with occasionally an oxygen deficit.
The large quarries of the Cement Industry in the environs of Opole, Southern Poland, provide an opportunity for detailed studies and faunal collecting in the Turonian and Lower Coniacian interval of the Opole Cretaceous sequence. Basing on the rich paleontological material 10 well defined, inoceramid zones are recognized. Their correspondance to the zones established elsewhere and their correlation with the international ammonite standard division is presented. -Author
New studies of sections in southern England (Bridgewick Pit, Downley, Shoreham Cement Works Quarry), eastern England (Kiplingcotes Station Quarry, Arras Road Pit), Germany (Salzgitter-Salder Quarry, a potential candidate GSSP for the Coniacian Stage) and central Poland (Słupia Nadbrzeżna, another potential candidate GSSP) have enabled a re-evaluation and refinement of the inoceramid biostratigraphy of the higher part of the Upper Turonian and the Turonian-Coniacian boundary transition. The inoceramid record at Słupia Nadbrzeżna below the terminal Turonian entry of Cremnoceramus is shown to be more complete than at the standard Salzgitter-Salder Quarry section. A new inoceramid event (Inoceramus lusatiae Event) identified at Słupia Nadbrzeżna is inferred to be present at the Sonnenberg Quarry, Waltersdorf, the type locality of Inoceramus lusatiae, as well as of I. glatziae and Cremnoceramus waltersdorfensis, and it is possibly represented in the condensed Navigation Hardgrounds in southern England. The absence of this event at Salzgitter-Salder suggests a significant hiatus. An inoceramid assemblage characterised by a taxon of uncertain affinities that immediately precedes the flood occurrence of Cremnoceramus (waltersdorfensis I Event) at Salzgitter-Salder has been identified at a comparable biostratigraphic position in eastern England (Yorkshire) and, tentatively, also in southern England. Inoceramids from this assemblage in the UK had previously been incorrectly assigned to Cremnoceramus waltersdorfensis and the basal Coniacian marker taxon, C. deformis erectus. The position of the base of the Coniacian has accordingly been revised upwards in both the southern and eastern England successions.
An integrated inoceramid-foraminiferal zonation for the topmost Turonian and Lower Coniacian near Briansk, SW of Moscow is presented. The inoceramid fauna enables the application of the refined zonal scheme currently applied in central and western Europe. Three zones based on benthic foraminifera, the Gavelinella moniliformis, Ataxophragmium nautiloides and Stensioeina granulata granulata zones; and three zones based on planktonic foraminifera, the Whiteinella archaeocretacea, Marginotruncana pseudolinneiana and Marginotruncana renzi zones, are distinguished. The Turonian/ Coniacian boundary, defined by the first appearance of the inoceramid Cremnoceramus deformis erectus (MEEK, 1877), falls within the basal part of the Stensioeina granulata granulata Zone and the basal part of Marginotruncana renzi Zone. In foraminiferal terms the Turonian/Coniacian boundary interval is marked additionally by a sudden, short-lived increase in the plankton/benthos ratio, caused primarily by more abundant shallow-water morphotypes.
The Turonian/Coniacian boundary succession in the United States Western Interior is characterized by the same inoceramid faunas as recognized in Europe, allowing the application of the same zonal scheme in both regions; Mytiloides scupini and Cremnoceramus waltersdorfensis waltersdorfensis zones in the topmost Turonian and Cremnoceramus deformis erectus Zone in the lowermost Coniacian. The correlation with Europe is enhanced, moreover, by a set of boundary events recognized originally in Europe and well represented in the Western Interior: Didymotis I Event and waltersdorfensis Event in the topmost Turonian, and erectus I, II and ?III events in the Lower Coniacian. First "Coniacian" ammonite, Forresteria peruana, appears in the indisputable Turonian, in the zone of M. scupini, and the reference to Forresteria in the boundary definition should be rejected. None of the North American sections, proposed during the Brussels Symposium as the potential boundary stratotypes, i.e. Wagon Mound and Pueblo sections, appears better than the voted section of the Salzgitter-Salder. The Pueblo section is relatively complete but markedly condensed in comparison with the German one, but it may be used as a very convenient reference section for the Turonian/Coniacian boundary in the Western Interior. The Wagon Mound section was mis-interpreted in respect of its biostratigraphical position and is entirely of Late Turonian age.
The Intrasudetic Basin (ISB) and Nysa Trough (NT) are evidently extensional synsedimentary tectonic features bounded by deep marginal faults. They represented the main depositional areas during the late Cretaceous in Sudetes, A characteristic littoral-to-shelf succession was formed in that period due to southwesterly directed successive progradation of the shallow marine depositional systems. Deposition was dominated by permanent alongshore drift and periodic storm events. The tectonic escarpments induced spectacular giant bedforms - accumulation terraces, and related facies association. The architecture from superimposed global events and local tectonic activity.
Two basic types of ichnofabrics occur in the marlstone-dominated Turonian-Coniacian deposits in the Opole region, namely the Thalassinoides and Chondrites ichnofabrics. Trace fossils (Chondrites, Ophiomorpha, Palaeophycus, Phycosiphon, Planolites, Taenidium, Teichichnus, Thalassinoides, Trichichnus) indicate the Cruziana ichnofacies. In the Thalassinoides ichnofabric, the trace fossils occur almost entirely against a totally bioturbated background, indicating relatively well-oxygenated sediments. In the Chondrites ichnofabric, trace fossils are smaller and the background is almost entirely bioturbated. Only in the lower part of the Odra quarry section, primary lamination is locally preserved. Generally, the Chondrites ichnofabric indicates less oxygenated and possibly deeper sediments than the Thalassinoides ichnofabric. Occurrence of the Chondrites ichnofabric in the Lower Turonian and Upper Lower Coniacian can be related to widely known anoxic events.
A neoselachian fauna from the Early Campanian of Höver near Hannover (NW Germany) comprises 12 taxa: Hexanchus gracilis Davis
1887?, Squalus? vondermarcki MÜller & SchÖllmann 1989, Deania? n. sp., Eoetmopterus supracretaceus MÜller & SchÖllmann 1989,
Palaeomicroides ursulae n. g. et n. sp., Cretascymnus westfalicus MÜller & SchÖllmann 1989, Centroscymnus praecursor MÜller
& SchÖllmann 1989, Squatina baumbergensis Von der Marck 1885?, Hemiscyllium n. sp., Cretolamna appendiculata (Agassiz 1843),
Palaeogaleus havreensis Herman 1977, and Paratriakis decheni (Von der Marck 1863)?. Being dominated by squalomorph sharks
the fauna shows closer relations to the Late Campanian neoselachian fauna of the Münster basin (NW Germany) than to the Early
Campanian fauna of the Aachen area (W Germany). The dominance of squalomorphs indicates that the Early Campanian sea reached
a considerable depth (probably several hundred meters) at Höver.
In einer Neoselachierfauna aus dem Unter-Campanium von Höver bei Hannover (NW Deutschland) sind 12 Taxa enthalten: Hexanchus
gracilis Davis 1887?, Squalus? vondermarcki MÜller & SchÖllmann 1989, Deania ? n. sp., Eoetmopterus supracretaceus MÜller
& SchÖllmann 1989, Palaeomicroides ursulae n. gen. et n. sp., Cretascymnus westfalicus MÜller & SchÖllmann 1989, Centroscymnus
praecursor MÜller & SchÖllmann 1989, Squatina baumbergensis Von der Marck 1885?, Hemiscyllium n. sp., Cretolamna appendiculata
(Agassiz 1843), Palaeogaleus havreensis Herman 1977, and Paratriakis decheni (Von der Marck 1863)?. Das Überwiegen squalomorpher
Haie belegt eine engere faunistische Beziehung zu der Neoselachierfauna aus dem Ober-Campanium des Münsterländer Beckens (NW
Deutschland) als zu der aus dem Unter-Campanium der Aachener Region (W Deutschland). Die Dominanz squalomorpher Haie verweist
außerdem auf eine erhebliche Wassertiefe (wahrscheinlich mehrere hundert Meter) des untercampanzeitlichen Meeres bei Höver.
Six teeth species, five lamniform sharks and one osteichthyes from the upper part of Umm Ghudran Formation, of Wadi at Tayyiba and Wadi Al Khafar, western Irbid, NW Jordan are the oldest shark and bone fish teeth known from Jordan. The large sharks and the large bone fishes in Jordan indicate a transgressive phase, deepening of the sea ground, and a following influence of an upwelling current in the area. The teeth assemblage confirm the Late Santonian age of the upper part of Umm Ghudran Formation. Anomotodon toddi and Scapanorhynchus texanus could have been originated in the region.
Three lithofacies characterize the Turonian/Coniacian sequences in the Upper Cretaceous of the Elbe Valley. The marly lithofacies, between Weinböhla - Dresden - Heidenau, consists of marls and calcareous clays (Strehlen Formation). A transitional lithofacies, with alternations of marls, clays and blocky sandstones, follows to the southeast (area between Rosenthal - Pirna - Lohmen). A sandy lithofacies, with blocky sandstones, is developed even farther to the southeast (Elbsandsteingebirge). The T/C boundary is situated in the lower part of the Strehlen Formation in the marly lithofacies, known from several boreholes. Coniacian index ammonites are absent across the T/C boundary in the three investigated boreholes apart from a deformed and incomplete specimen of Placenticeras cf. orbignyanum (GEINITZ). Therefore, bivalves must be used to place the T/C boundary. The Didymotis event II (Dresden-Marienhof Borehole), with Cremnoceramus waltersdorfensis (ANDERT), lies at the top of the Upper Turonian M. scupini Zone. The rarity or absence of the bivalve Didymotis in the Dresden-Blasewitz and Graupa boreholes is caused by facies changes. The FAD of Cremnoceramus rotundatus (TRÖGER non FIEGE), especially the C. rotundatus Event (Graupa Borehole, Hinterjessen Marl), can be used to place the T/C boundary. A small interval below the FAD of C. rotundatus and above the Didymotis II event, which may belong to the basal Coniacian, yields Cremnoceramus waltersdorfensis (ANDERT). Cremnoceramus waltersdorfensis hannovrensis (HEINZ), Mytiloides carpathicus (SIMIONESCU) and Placenticeras cf. orbignyanum (GEINITZ). In the sandy lithofacies fossils are rare. It is not possible to place the boundary in either the Herrenleite Sandstone or in sandstone d. In the marly lithofacies of the Upper Cretaceous of Saxony bracketing of the T/C boundary is possible by means of planktonic foraminifera. It is possible to identify the evolution of planoconvex double-keeled globotruncanids of the Dicarinella hagni - Dicarinella primitiva - Dicarinella concavata group from the Upper Turonian. In the Dresden-Blasewitz and Dresden-Marienhof boreholes this group is represented in the T/C boundary interval by Marginotruncana paraconcavata PORTHAULT and Dicarinella cf. concavata (BROTZEN). They are of rare occurrence because they are facies controlled. It is not possible to recognize the boundary between the schneegansi and concavata zones because of the restricted occurrence and rarity of the index forms in the investigated sections. In the Dresden-Blasewitz and Dresden-Marienhof boreholes the benthonic species Stensioeina granulata (OLBERTZ) was identified.
The stratigraphy, ammonite and inoceramid content of the Turonian - Coniacian deposits of Far East Russia are presented. The evolution of North Pacific ammonites and inoceramids at the boundary of the two stages was studied and the levels of fundamental changes within the ammonite and inoceramid biota are recognized. The established palaeobiogeographic difference between the Sakhalin and the North-East region palaeobasins is reflected in the existence of the independent local zonal schemes. The main criteria of the Turonian-Coniacian stage boundary in the Far East of Russia were established on the basis of the two schemes. The Turonian/Coniacian (T/C) boundary is clearly marked by the change in the taxonomic diversity of the zonal inoceramid assemblages. It is defined at the base of the Inoceramus uwajimensis Zone. The appearance of the endemic ammonite species Jimboiceras mihoense MATSUMOTO is the ammonite criterion for recognising the T/C stage boundary in Sakhalin. This is supported by occurrences of the cosmopolitan Coniacian genera Peroniceras and Forresteria.
Upper Cretaceous strata are well exposed in many areas of Japan, although good exposures through the Turonian/Coniacian boundary are not common. This paper focuses on six areas in Hokkaido, Shikoku and Kyushu and documents the stratigraphical distributions of inoceramid species. These data are used to summarise the stratigraphical ranges of Turonian/Coniacian taxa in Japan. In part 1 of the paper, 17 species are described, with some biometric data and phylogenetic interpretation.These species are: Inoceramus (Inoceramus) hobetsensis NAGAO & MATSUMOTO. I.(I.) teshioensis NAGAO & MATSUMOTO, I.(I.) iburiensis NAGAO & MATSUMOTO, I.(I.) tenuistriatus NAGAO & MATSUMOTO, I.(I.) pedalionoides NAGAO & MATSUMOTO, I.(I.) lusatiae ANDERT, I.(I.) uwajimensis YEHARA, I. Cremnoceramus) rotundatus FIEGE, I. (Cr.) ernsti HEINZ, I. (Cr.) deformis MEEK, I. (Cr.) lueckendorfensis TRÖGER, I. (Platyceramus) tappuensis nom. nov., I. (PI.) szaszi NODA & UCHIDA, I. (Volviceramus koeneni MÜLLER, Mytiloides incertus (JIMBO). M. mytiloidiformis (TRÖGER), and M. sublabiatus (MÜLLER. In part 2, the stratigraphical distribution and correlation of these species are discussed.
Twenty-three elasmobranch taxa have been recovered from the Upper Cretaceous Carlile Shale (Middle Turonian to Early Coniacian) of the Black Hills region of South Dakota and Wyoming. The oldest unit, the Pool Creek Member, represents marine shoreface depositional environments and contains a selachian assemblage composed predominantly of pelagic predators (Carcharias, Cretodus, Cretolamna, Cretoxyrhina, Johnlongia, Scapanorhynchus, Squalicorax). Rocks from the lower part of the overlying Turner Sandy Member represent shallow-water environments influenced by wave-generated and tidal currents. Moderately diverse elasmobranch assemblages recovered from these rocks contain a preponderance of benthic taxa (Cantioscyllium, Chiloscyllium, Ischyrhiza, Pseudohypolophus, Ptychodus, Ptychotrygon, Rhinobatos, Sclerorhynchus). Only one taxon, Ptychodus latissimus, has thus far been recovered from the Sage Breaks Shale Member, which was deposited in an offshore, shelf-depth, open marine environment.
The upper Cretaceous deposits of the Opole Trough contain rare but relatively diverse shark teeth, mainly from ptychodontid sharks (Ptychodus latissimus Agassiz, 1843, Ptychodus polygyrus Agassiz, 1843 and Ptychodus mammillaris Agassiz, 1843), Anacoracidae (Squalicorax sp.), Mitsukurinidae (Scapanorhynchus raphiodon (Agassiz, 1843)), Alopiidae (Paranomotodon angustidens (Reuss 1845)) and Cretoxyrhinidae. Paranomotodon angustidens has not previously been reported from the Opole Trough. The selachians from the Opole Basin can be divided into two trophic groups: bottom-dwelling ptychodontid sharks with a diet consisting of shelly invertebrates, and pelagic Lamniformes, which were active predators feeding on fast-swimming fish and reptiles. The morphology of the teeth, signs of abrasion and the analysis of the invertebrate assemblage from the Opole Cretaceous suggest that the ptychodontids fed on inoceramid bivalves, while the lamniform sharks fed mostly on fish. Lamniformes live in all marine environments, and their remains are numerous in all the lithostratigraphic units of the Upper Cretaceous in the Opole Trough. The teeth of deep-water ptychodontid sharks are only abundant in the middle part of the Middle Turonian sediments. Nearshore shark remains are extremely rare in the Cretaceous deposits of the Opole Trough. This indicates that the Middle Turonian (middle I. lamarcki Zone) represents the deepest environment of the Opole Cenomanian and Turonian.
Surface collecting and bulk sampling techniques have yielded a diverse selachian assemblage from the upper part of the Belle Fourche Shale in the Black Hills region of South Dakota and Wyoming. Taxa include Hybodus sp., Ptychodus occidentalis, Squatina sp., Squalicorax sp. cf S. curvatus, S. volgensis, Cretodus semiplicatus, Cretoxyrhina mantelli, Carcharias amonensis, C. saskatchewanensis, C. tenuiplicatus, and the enigmatic Cretomanta canadensis. Associated ammonites indicate a late middle Cenomanian age for the fossils. All but Hybodus, Cretodus, and C. amonensis represent earliest occurrences in the Black Hills, and this is the oldest North American occurence of C. canadensis. The Belle Fourche Shale was deposited during a major transgression during the middle Cenomanian. The majority of the fossils, representing the most diverse assemblage, occur in thin calcarenites. These rocks and the associated shark taxa indicate a fairly shallow-water, nearshore marine environment. This suggests that, although the seaway was in a transgressive phase, minor regressive events took place during the late middle Cenomanian.
Several specimens of the Late Cretaceous lamniform shark, Cretoxyrhina mantelli (Agassiz), from the Niobrara Chalk of Kansas suggest that the shark fed on teleosts, mosasaurs, and possibly plesiosaurs. These animals are active vertebrates, so C. mantelli probably occupied the apex of the food chain in the Late Cretaceous seas. This top predator, however, was probably scavenged frequently by anacoracid sharks. Carcharodon carcharias (great white shark) and carcharhinid sharks are considered as the modem guild counterparts for Cretoxyrhina mantelli and anacoracids, respectively.
TRÖGER, K.-A. 2004. Cenomanian through Lower Coniacian events in the Upper Cretaceous of Saxony, Germany. Acta Geologica Polonica, 54 (4), 629-638. Warszawa. The event sequence recognised in the Cenomanian through basal Coniacian (Late Cretaceous) of the Elbe Valley is com- pared with the event stratigraphic scheme worked out in NW Germany. The following events, recognised originally in Lower Saxony, and subsequently in other Cretaceous areas of north-western Europe, were found in Saxony: Schloenbachia / virgatus eustatoevent (Lower Cenomanian); Chondrites ecoevent, Puzosia eustatoevent and plenus eustatoevent (Upper Cenomanian); hattini ecoevent, Mytiloides ecoevents, hercynicus ecoevent, Hyphantoceras ecoevent, Didymotis ecoevents and waltersdorfensis ecoevent (Turonian); erectus ecoevent, hannovrensis ecoevent, and incostans ecoevent (Lower Coniacian). Both the oxic/anoxic Cenomanian/Turonian boundary event and the facies change at the base of the Metoicoceras geslinianum Zone are recognisable. With the exception of the Mytiloides ecoevents, recorded in all facies types, all the events are well developed only in the marly-silty facies. Local events, specific to the Cretaceous of Saxony are: the Late Cenomanian Pennrich event, known from the Sudetic area, and the Middle Turonian rhynchonellid events, occur- ring in sandy and transitional facies between Pirna and Bad Schandau.
Bibliogr. s. 52-54. - Angl. souhrny kapitol na konci kn