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1

Ammonite biostratigraphy in the Polish Jura sections (central Poland) as a clue for recognition of the uniform base of the Kimmeridgian Stage

Wierzbowski A., Matyja B.

Volumina Jurassica

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2014

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Vol. 12, no. 1

45--98

EN

The ammonite succession in the stratigraphical interval from the Bifurcatus Zone, through the Hypselum Zone, up to the lower part of the Bimammatum Zone corresponding to a large part of the Submediterranean Upper Oxfordian is studied in several sections of the Polish Jura in central Poland. The sections have yielded numerous ammonites of Submediterranean–Mediterranean affinity, but also, some of Boreal and Subboreal character. The co-occurrence of ammonites of different bioprovinces makes possible the correlation between the different zonal schemes – especially between the Subboreal/Boreal zonations and the Submediterranean/Mediterranean zonation. The correlation shows that the boundary of the Pseudocordata and Baylei zones (Subboreal) and its equivalent – the boundary of the Rosenkrantzi and Bauhini zones (Boreal), currently proposed as the primary standard of the Oxfordian-Kimmeridgian boundary within its GSSP at Staffin Bay (Isle of Skye, Scotland), runs in the Submediterranean/Mediterranean Upper Oxfordian near the base of the Bimammatum Zone. This discovery removes the main obstacle against the formal recognition of the Staffin Bay section as representing the uniform base of the Kimmeridgian Stage in the World and its GSSP. The ammonite taxa recognized are commented on and/or described, and suggestions on their taxonomical and phylogenetical relations are given in the palaeontological part of the study. A new taxon is established: Microbiplices anglicus vieluniensis subsp. nov.

2

Stratigraphy and microfacies of the Jurassic and lowermost Cretaceous of the Veliky Kamenets section (Pieniny Klippen Belt, Carpathians, Western Ukraine)

Rehakova D., Matyja B., Wierzbowski A., Schlogl J., Krobicki M., Barski M.

Volumina Jurassica

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2011

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Vol. 9, no. 1

61-104

EN

The Veliky Kamenets section in the eastern part of the Pieniny Klippen Belt in the Ukrainian Carpathians shows a well exposed, 83 m thick succession composed of Jurassic and lowermost Cretaceous (Berriasian) deposits. The terrigenous part of the section includes: gravels with a sandy matrix (unit 1A), massive grey-green sandstones (unit 1B) and shales with intercalations of siltstones/sandstones and oyster/gastropod lumachelles (unit 2). Organic-walled dinoflagellates document the Toarcian-Aalenian age of the siliciclastic deposits of unit 2. The carbonate part of the succession embraces: stromatactis mud-mounds interfingering with crinoidal limestones (unit 3A), lower nodular limestones (unit 3B), cherty limestones (unit 3C), upper nodular limestones (unit 3D), pink pelitic limestones (unit 3E), limestones with a volcanogenic bed (unit 5) and limestone breccia limestones (unit 6). This succession has yielded abundant ammonites from the Bathonian, Oxfordian and Kimmeridgian (with a stratigraphical hiatus covering the Callovian and Lower Oxfordian), as well as calcareous dinoflagellates (from the Upper Oxfordian towards the top of the succession), and calpionellids (in the Tithonian and Berriasian). Detailed stratigraphical study of the succession based both on ammonites and microfossils has resulted in the recognition of biostratigraphical units and their correlation with the chronostratigraphical scale.The microfacies recognized in the pelagic part of the succession include: the “filament” (Bositra) microfacies (Bathonian), the planktonic foraminifer microfacies (Oxfordian), the Saccocoma microfacies (Kimmeridgian to Upper Tithonian), and the calpionellid microfacies (Upper Tithonian–Berriasian). The volcanogenic rocks (lava flows and volcanic ash) appear in the topmost part of the succession (units 4 to 6) and this volcanic event is very precisely located in the Elliptica-Simplex chrons of the Middle and Late Berriasian.

3

Metrologiczne i eksploatacyjne aspekty pomiaru poziomu metodą radarową i ultradźwiękową

Banaczyk E., Błotnicki W., Kozyra A., Matyja B., Waluś S.

Pomiary Automatyka Kontrola

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2010

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R. 56, nr 8

659-862

PL

Istnieje wiele kryteriów podziału metod pomiaru poziomu. W referacie przestawiono najbardziej ogólny podział na metody bezpośrednie i pośrednie. Wyprowadzono model matematyczny pomiaru objętości materiału sypkiego, który tworzy stożek nasypowy, przy zastosowaniu poziomomierza radarowego z falowodem i obliczono błędy metody takiego pomiaru. Na podstawie badań laboratoryjnych oraz danych literaturowych dokonano porównania przepływomierzy ultradźwiękowych z radarowymi z falowodem. Korzystając z doświadczeń laboratoryjnych i danych literaturowych z obiektów polowych podano wskazówki odnośnie doboru poziomomierza.

EN

The paper presents the division of level measurement methods taking into account various criteria: principle of operation, contact with the process material, open or closed tank and art of measure-ment: direct and indirect. The mathematical model of measurement of volume of solid in the tank by radar level meter with wave-guide for some typical situations is introduced. It enables volume of material calculation on the base of the result of actual level measurement and the information of previous level. Also the method error as a function of distance between the probe and tank axis and the function of the mound cone angle is calculated. Introducing special algorithm of volume calculation or using two probes for level measurements can give decreasing of systematic error of volume calculation. On the base of laboratory tests and literature data from field objects the comparative analysis of ultrasonic level meter and radar level meter with wave-guide is introduced. Some guidelines for choosing proper level meter for various measurement conditions are presented.

4

The oceanic "Metis Geotectonic Event" (Callovian/Oxfordian) and its implications for the peri-Tethyan area of Poland

Matyja B., Wierzbowski A.

Volumina Jurassica

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2006

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Vol. 4, no. 1

60-61

EN

Condensed deposits of the Middle/Upper Callovian and/or lowermost Oxfordian are spread over vast areas of peri-Tethyan Europe from Portugal, and Spain through France, Switzerland, Germany, Poland, to Romania. A number of hypotheses for the origin of these deposits have been presented. Melendez et al. (1983) suggested that they originated due to the rise of CCD in relation to increased igneous activity. Other proposed explanations include: an extra-terrestrial event (Brochwicz-Lewifski et al. 1989) and erosional events and related taphonomic reworking of fossils during long episodes of subaerial exposure (Aurell et al. 1991). Palaeomagnetic data from the Pieniny Klippen Belt (Carpathians) of southwestern Ukraine (Lewandowski et al. 2005), and western Slovakia (Lewandowski et al. 2006) indicate that during Middle Callovian - Early Oxfordian time span a relatively fast opening of the oceanic domain took place in the outer part of the Tethys. This newly open basin (possibly corresponding to the Magura Basin in the Carpathian domain) attained 1100-1400 km in width. The rocks that formed during the Middle Callovian - Early Oxfordian in the epi-platform area of Poland bear witness to this geotectonic event. It is highly probable that the total spatial range of the geo-tectonic event within the Tethys (cf. Lewandowski et al. 2006) has been much greater, however, which indicates that the obtained results can be applied to the whole peri-Tethyan Europe. Thus, to distinguish this phenomenon independently of which particular part of the Tethys it affected, we propose to name it the "Metis Geotectonic Event"(Metis in Greek mythology was the Oceanid, and the daughter of Tethys). The appearance of condensed deposits in the epi-platform area of Poland (Giżejewska & Wieczorek 1974; Dembicz & Praszkier 2003, and other papers cited therein) remains in close time relation with recognized extension in the Tethyan domain. The short time interval of the extension (about 5 Ma) plus a large-scale displacement could have resulted in a sudden change in deposition from shallow-marine to pelagic environment, as well as in chemical corrosion of earlier accumulated carbonates. This change of deposition was controlled by relative sea-level rise as well as by upwelling of cold oceanic waters into the epi-platform area. This interpretation is consistent with recognized isotopic thermometry results indicating drastic cooling of sea water at lower middle latitudes (Dromart et al. 2003). The development of the sponge megafacies covering the peri-Tethyan part of the Late Jurassic shelf of Europe remains in close relationship with discussed phenomena. These deposits showed during Oxfordian similar spatial distribution as older condensed deposits, and represent the non-actualistic deep environment of the Late Jurassic shelf (Matyja & Pisera 1991; Matyja & Wierzbowski 1996).

5

Palaeomagnetism of the Pieniny Klippen Belt (Carpathians): evidence for low-latitude origin and palaeogeographic dispersion of the Upper Jurassic carbonates

Lewandowski M., Aubrecht R., Krobicki M., Matyja B., Reháková D., Schlögl J., Sidorczuk M., Wierzbowski A.

Volumina Jurassica

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2006

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Vol. 4, no. 1

56-58

EN

Palaeomagnetic studies on the Middle and Upper Jurassic carbonates were recently carried out along the Pieniny Klippen Belt from Ukraine (Veliky Kamenets, Lewandowski et al. 2005), through Poland to Western Slovakia (Fig. 1A). More than 200 oriented cores and hand samples were collected from lithologies considered representative for the Czorsztyn Succession (Birkenmajer 1976, 1986), cropping out from the East to the West of PKB in Slovakia. Laboratory work aiming at recognizing the natural remanent magnetization structure, involving thermal and alternating field demagnetizations, magnetic measurements using 2G SQUID magnetometer and employing principal component analysis revealed a multicomponent nature of NRM (Fig. 1B-C). Rock magnetic studies have shown that Ti-poor magnetite is the main magnetic carrier of NRM. In turn, EMS and SEM analysis confirmed the presence of magnetite grains of both detrital and autigenic origin (Fig. 1E-F). Low coercivity/unblocking temperature components are considered post-tectonic and genetically interpreted as an orogeny-related overprint. An overall direction is proximal to the Tertiary directions from cratonic Europe, pointing to only minor individual block rotations after the Pieniny Klippen Belt was formed (Fig. 1). Characteristic, high blocking temperature components (ChRM) show dual-polarity distribution (reversal test statistically positive at B and C levels) and are considered primary. Palaeomagnetic declinations differ among the localities, testifying tectonic rotations of individual blocks after acquisition of ChRMs, supposedly exerted due to transform faults systems, active during Late Jurassic-Cretaceous time. Palaeomagnetic inclinations for the Oxfordian point to palaeolatitude positions ranging from (assuming North) 28° in Veliky Kamenets (Ukraine, see Lewandowski et al. 2005), 17° at Kyjov Pusté Pole, 12° at Milpoš, and 9° in Babina (all in Slovakia), an average error of the oval of 95% confidence being 8° (Fig. 1D). Interestingly, the Milpoš section yielded ca. 10° inclination shift between Bajocian and Oxfordian rocks, indicating southward migration of the host basin in the time concerned. This conclusion is in line with the data obtained for the Kamenets section (Lewandowski et al. 2005). On the other hand, Callovian radiolarites of Butkov, the Inner Carpatians unit situated today in the vicinity of Babina, yielded palaeolatitudes of ca. 22°. It is worth also to note that palaeomagnetic studies of the uppermost Jurassic carbonates from the Brodno Klippe of the Kysuca (equivalent of Branisko) Succession (Houša et al. 1999) also point to low latitudes of deposition. These new data evidence wide palaeogeographic separation of currently neighbouring sedimentary rocks and their host basins in Late Jurassic time, the southernmost of them being in the proximity of Northern Africa. This outcome suggests that Pieniny Klippen Belt is composed of Tethyan microblocks (terrains), witnessing an evolution of Jurassic basins at relatively distant areas of the Tethys domain. Alternatively, the latitudinal dimension of the Czorsztyn Ridge, the host structural unit for the Czorsztyn Succession, would have been 2000±900 km during mid-Oxfordian time.

6

Jurassic - lowermost Cretaceous successions at Priborzhavskoye (Pieniny Klippen Belt, SW Ukraine) and their palaeogeographic importance

Krobicki M., Matyja B., Wierzbowski A.

Volumina Jurassica

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2006

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Vol. 4, no. 1

53-54

EN

The large quarries at Priborzhavskoye show thick and fairly complete sequences of the Jurassic and Lower Cretaceous deposits representing two different palaeogeographic successions. The bulk of the deposits in the quarries covers a sequence of dark siliciclastic dominated deposits of the Gresten-like facies (Hettangian - Lower Sinemurian) followed by spotty limestones and marls of the Fleckenkalk/Fleckenmergel-type (Sinemurian-Pliensbachian); these are capped by thin carbonate deposits indicating a reduced sedimentation rate and rich in ammonites (uppermost Pliensbachian to Aalenian), and overlain by thick-bedded massive crinoidal limestones of the Smolegowa Limestone Formation (Bajocian). The younger deposits of the sequence are micritic ammonite-brachiopod coquinas and the youngest are micritic limestones rich in ammonites (Tithonian-Berriasian) with an omission surface on the top where phosphatic stromatolites occur (these limestones are in tectonic contact with the discussed crinoidal limestones). All these deposits are tectonically overturned and overthrusted by rocks of an upper tectonic unit representing a different succession. The latter consists of thin-bedded crinoidal limestones with multicoloured cherts, overlain by red nodular limestones with ammonites (uppermost Bajocian to Kimmeridgian/Tithonian), and thin-bedded white and greenish Maiolica-type micritic limestones (Tithonian-Berriasian). The presumable position of the two sequences of deposits corresponding to different palaeogeographic successions may be considered mainly based on the character of coeval crinoidal limestones found in both successions: a shallower ones represented by massive crinoidal limestones (Smolegowa Limestone Formation) with condensed deposits at their base, and deeper ones represented by thin bedded crinoidal limestones with cherts. Although some similarity of the shallower succession from Priborzhavskoye, to the typical Czorsztyn Succession from the western part of the Pieniny Klippen Belt (Poland, Slovakia) may be indicated, there exist marked differences. The most important difference is the occurrence in the Priborzhavskoye of highly condensed pelagic deposits at the base of the crinoidal limestones of the Smolegowa Limestone Formation, covering the time interval from the latest Pliensbachian to Aalenian. In the Czorsztyn Succession of Poland and Slovakia the deposits underlying the Smolegowa Limestone Formation are developed as dark clays, marls and limestones of the Fleckenmergel/Fleckenkalk-type, and the hiatus at the base of the crinoidal limestones corresponds to a part of the Lower Bajocian. Conversely, the deeper-water succession from Priborzhavskoye showing the presence of thin-bedded crinoidal limestones, Ammonitico Rosso deposits of the Ammonitico Rosso marneux type, and thin-bedded of the Maiolica-type limestones has no direct counterparts in the western part of the Pieniny Klippen Belt; the typical "transitional" and basin successions in the latter area show the presence of radiolarites which are totally absent in the discussed succession at Priborzhavskoye. The ridge to basin pelagic facies pattern recognized at Priborzhavskoye although similar to that from western parts of the Pieniny Klippen Basin differs thus in several features. The indicated differences between the Priborzhavskoye area and more western parts of the Pieniny Klippen Basin could be related to an earlier (latest Pliensbachian-Aalenian) uplift of the Priborzhavskoye area than of the Czorsztyn Ridge, in the territory of Slovakia and Poland (Early Bajocian). These could result from either (1) diachronous uplifting of the Czorsztyn Ridge which included the shallower succession of the Priborzhavskoye area, or (2) a more southeastern, independent position of the studied succession within the Pieniny Klippen Basin, than that of the Czorsztyn Ridge regarded usually as confined to the northwestern border of the basin.

7

Fast palaeogeographic changes of the Pieniny Klippen Basin from palaeomagnetic data of the Bajocian-Berriasian section in the Veliky Kamenets (Carpatians, West Ukraine)

Lewandowski M., Krobicki M., Matyja B., Wierzbowski A., Sidorczuk M.

Volumina Jurassica

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2006

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Vol. 4, no. 1

58-59

EN

A 40 m thick carbonate succession of the Bajocian to Berriasian age from the Veliky Kamenets quarry (Novoselica area, Pieniny Klippen Belt, Ukraine) resembles both the Czorsztyn and Niedzica successions of the Pieniny Klippen Belt, traditionally considered ridge slope-related deposits. 176 individually oriented cores have been collected for palaeomagnetic purpose from the bottom to the top of the sequence, with sampling density dependent on inferred sedimentation rates. Unblocking temperature spectra and results of the Lowrie test, as well as electron microscope analyses, point to a Ti-poor magnetite as a main magnetic carrier. Thermal demagnetization revealed two main components of the natural remanent magnetization (NRM). A low-blocking temperature component S of normal polarity is considered of post-tectonic, probably thermoviscous origin due to overheating by Neogene volcanics. A stable, high-blocking temperature NRM component P shows dual polarity distribution and is considered primary. Since two significant sedimentary gaps occur at 422 cm and 860 cm (the main hiatus - H) from the base, the latter comprising the Late Callovian - Early Oxfordian time span (6-8 Ma), the pattern of magnetic reversals presented in this study can not be considered complete. A palaeolatitude of 41° ±5° is calculated for the mid-Jurassic part below H, similar to that expected for the European Craton at the Kamenets locality. The mid-Oxfordian limestone, directly overlying H, has palaeolatitudes around 28° ±6°. This implies a relatively fast opening of the oceanic domain to the North of the Kamenets block. Palaeomagnetic declinations suggest 100° counterclockwise rotation of the whole section before the Neogene.

8

Biostratigraphy of the Upper Jurassic – lowermost Cretaceous succession at Veliky Kamenets (Pieniny Klippen Belt, Carpathians, SW Ukraine)

Rehakova D., Krobicki M., Matyja B., Wierzbowski A.

Volumina Jurassica

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2006

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Vol. 4, no. 1

207-208

EN

The Veliky Kamenets quarry is an essential locality in stratigraphical and palaeomagnetical studies of the Jurassic and lowermost Cretaceous in eastern part of the Pieniny Klippen Belt. The carbonate succession, about 40 m thick, has been subdivided into 6 major lithostratigraphical units (A, B, C, D, DE and E) which biostratigraphy was based mainly on the ammonite fauna (Lewandowski et al. 2005); these deposits are overlain by about 13 m thick complex unit of carbonates (fossiliferous limestones and calcareous sedimentary breccias composed mainly of micritic limestone clasts) alternating with volcanogenic rocks (basalt lava flows, and pyroclastic deposits). The studied succession yielded abundant and well preserved microfossils which enable detailed stratigraphical interpretation of the deposits in question. The lowest part of the Upper Jurassic succession (upper part of unit B) is represented by lower Ammonitico Rosso limestones rich in planktonic foraminifers Globuligerina. The ammonites are indicative of the Plicatilis Zone and Transversarium/or Bifurcatus Zone of Middle, and possibly lowermost Upper Oxfordian, whereas calcareous dinoflagellates found at the top of the unit indicate the Parvula Zone of the Upper Oxfordian. The overlying cherty limestones (unit C) yielded the Kimmeridgian ammonites found in their uppermost part; the deposits of the unit are rich in rests of planktonic crinoids Saccocoma. The younger ammonite assemblage coming from the lower part of the upper Ammonitico Rosso unit (unit D) is indicative of the Acanthicum Zone of the Upper Kimmeridgian. These deposits are characterized by Saccocoma-Globochaete microfacies, and yielded calcareous dinocysts indicative of the Moluccana Zone of the Kimmeridgian. The Kimmeridgian/Tithonian boundary runs in the middle of the discussed Ammonitico Rosso unit (unit D) as evidenced by occurrence of calcareous dinocyst Carpistomiosphaera tithonica. The upper part of the unit yielded calpionellids and calcareous dinocysts indicative of the Praetintinnopsella Zone located at the turn of the Middle and Upper Tithonian. The topmost part of the unit, as well as the lower part of overlying partly nodular micritic limestones (unit E/D) yielded already calpionellids and calcareous dinocysts indicative of the Crassicolaria Zone of the Upper Tithonian. The deposits are dominated by the Crassicolaria-Globochaete microfacies. The Jurassic/Cretacous boundary runs in the middle of the partly nodular micritic limestone unit (D/E). Here appears assemblage dominated by spherical forms of Calpionella alpina indicating the lowermost part of the Calpionella Zone of the Lower Berriasian. This zone ranges up at least to the upper part of massive micritic limestones (unit E) where the calpionellids of the Ferasini Subzone have been recognized. The microfacies of the Globochaete-Calpionella type, locally enriched in radiolarians prevail. The carbonates of the topmost part of the succession covering the basalt lava flows, as well as limestones alternating with pyroclastic layers yielded calpionellids of the Calpionellopsis Zone of the Upper Berriasian indicating both the Simplex Subzone, and the Oblonga Subzone. The breccias contain i.a. the clasts of the Upper Tithonian micritic limestones with calpionellids of the Crassicolaria Zone and of volcanic rocks. The carbonates correspond to the ?ysa Limestone Fm., including the Walentowa Breccia Member of this formation (see Birkenmajer 1977).

9

Bathonian ammonites from the Polish Tatras

Galacz A., Matyja B.

Volumina Jurassica

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2006

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Vol. 4, no. 1

162-162

EN

In the sedimentary sequence of the Polish High Tatras, thin limestone beds with Middle Jurassic, mainly Bathonian fossils have been reported. The best known of these occurrences is that of Wielka Âwistówka Cirques in the Mi´tusia Valley with extremely rich ammonite fauna which became famous for the classic monographs of Passendorfer in 1935 and 1938. The fauna occurs in a condensed bed overlying with considerable hiatus the Middle Triassic shallow-water carbonates, and is covered by Upper Jurassic pelagic limestone. The 8-12 cm thick bed yielded nautiloids, belemnites, ammonites and brachiopods in great profusion, and less commonly other molluscs (bivalves and gastropods). The revision of the ammonite fauna in the collections of Passendorfer indicated that most of the forms is typical of the higher Middle Bathonian Bremeri Zone, with the rich representation of the zonal index and other diagnostic forms, e.g. Prohecticoceras ochraceum, Bullatimorphites eszterensis. Within the perisphinctids, Procerites is dominant and Wagnericeras is rarer which could indicate the lower part of the Bremeri Zone. As interesting rarities, Phlycticeras, Oecoptychius, Thraxites, etc. also appear. However, the collections contain some macrocephalitids and rare Hecticoceras suggesting the presence of the Lower Callovian. While preservational differences cannot be seen between the Bathonian and Callovian fossils, and the recent state of the Wielka Âwistówka exposure did not show this, the best explanation is to suppose an occurrence of a thin, intermittent Callovian layer in between the Bathonian and Upper Jurassic beds as the source of these stratigraphically younger ammonites in the collections. The ammonite fauna is dominated by suborder Ammonitina (66.6%) of which nearly half belongs to the Perisphinctidae, and phylloceratids are represented 32%. This is a faunal composition very close to those from other Bathonian condensed ammonite beds occurring in the Carpathian-Pannon region (e.g. Swinitza in the Southern Carpathians, Villány in South Hungary).

10

A potential stratotype for the Oxfordian/Kimmeridgian boundary: Staffin Bay, Isle of Skye, UK

Wierzbowski A., Coe A., Hounslow M., Matyja B., Ogg J., Page K., Wierzbowski H., Wright J.

Volumina Jurassica

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2006

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Vol. 4, no. 1

17-33

EN

A coastal exposure of the Staffin Shale Formation at Flodigarry, Staffin Bay, Isle of Skye, Scotland, UK fulfils the criteria for definition as the Global Stratotype Section and Point (GSSP) for the base of the Kimmeridgian Stage (Upper Jurassic). This marine shale succession was deposited during a long-term transgression, and is part of a complete, relatively well-expanded stratigraphic succession. A rich fauna of ammonites above and below the Oxfordian/Kimmeridgian boundary allows recognition of the Evoluta Subzone (Pseudocordata Zone) and Rosenkrantzi Subzone (Rosenkrantzi Zone) of the Subboreal and Boreal uppermost Oxfordian, and the Densicostata Subzone (Baylei Zone) and the Bauhini Zone of the Subboreal and Boreal lowermost Kimmeridgian). A suitable level for the boundary is thus marked by the replacement of the Subboreal Ringsteadia (M)/Microbiplices (m) by Pictonia (M)/Prorasenia (m), and by the first appearance of Boreal Amoeboceras (Plasmatites). Detailed study of the microfossils reveals an excellent dinoflagellate succession. A variety of stratigraphically important dinoflagellates are found, the assemblages being intermediate in character between Boreal and Subboreal ones. The magnetostratigraphic data, though rather troublesome to extract, shows a polarity pattern which can be confidently correlated to other UK boundary sections. The upper boundary of a normal magnetozone falls at, or very near, the proposed Oxfordian/Kimmeridgian boundary. The 87Sr/86Sr ratio at the boundary, based on an analysis of belemnites, lies between 0,70689 and 0,70697, averaging 0.70693. Matching worldwide trends, no distinct change in the ratio is seen across the boundary. A lack of variations in the carbon isotope composition of belemnites across the Oxfordian/Kimmeridgian boundary does not indicate perturbation in the global carbon cycle. However, high ?13C values and their scatter suggest the influence of local fractionation affecting isotope composition of dissolved inorganic carbon (DIC) in the partly isolated Boreal sea. A fall in the belemnite ?18O values in the Upper Oxfordian and Lower Kimmeridgian compared to the Mid Oxfordian suggests a slight rise in seawater temperature.

11

Paleogeografia pienińskiego basenu skałkowego: środkowojurajsko-wczesnokredowa ewolucja na podstawie badań paleomagnetycznych sekwencji Kamenca (Ukraina Zakarpacka)

Lewandowski M., Krobicki M., Matyja B., Wierzbowski A.

Volumina Jurassica

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2003

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Vol. 1, no. 1

29-34

12

Następstwo amonitów dolnego i środkowego oksfordu w profilu kamieniołomu w Ogrodzieńcu i ich znaczenie biogeograficzne

Matyja B., Głowniak E.

Volumina Jurassica

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2003

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Vol. 1, no. 1

53-58

13

Biostratygrafia amonitowa formacji częstochowskich iłów rudonośnych (najwyższy bajos - górny baton) z odsłonięć w Częstochowie

Matyja B., Wierzbowski A.

Volumina Jurassica

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2003

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Vol. 1, no. 1

3-6

14

Boreal and Subborreal ammonites in the Submediterranean uppermost Oxfordian in the Bielawy section (northern Poland) and their correlation value

Matyja B., Wierzbowski A.

Acta Geologica Polonica

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2002

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Vol. 52, nr 4

411-421

EN

The youngest deposits exposed in the Bielawy Quarry (Kujawy area, northern Poland) yielded both Submediterranean ammonites, making possible recognition of the uppermost Submediterranean Oxfordian, and Subboreal-Boreal ammonites, indicative of some parts of the Subboreal/Boreal lowermost Kimmeridgian. This makes possible closer correlation of the different zonal schemes that appear to be important in discussion of the uniform Oxfordian/Kimmeridgian boundary and recognition of its GSSP. The upper part of the Submediterranean Planula Subzone yields Boreal Amoeboceras of the Plasmatites group, indicative of the Boreal Bauhini Zone. Moreover, the lowermost part of the Submediterranean Galar Subzone corresponding to the wenzeli horizon yields Boreal Amoeboceras of the Amoebites group (such as Amoeboceras bayi BIRKELUND & CALLOMON), indicative of the lowermost part of the Boreal Kitchini Zone, as well as late representatives of the genus Pictonia, described here as Pictonia kuiaviensis sp. nov., allowing correlation with the upper part of the Subboreal Baylei Zone.

15

Biological response of ammonites to changing environmental conditions : an example of Boreal Amoeboceras invasions into Submediterranean Province during Late Oxfordian

Matyja B., Wierzbowski A.

Acta Geologica Polonica

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2000

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Vol. 50, no. 1

45-54

EN

Amoeboceras faunas constituting the typical element of the Boreal Province occur abundantly in two Amoeboceras layers in the Submediterranean Province ammonite succession of the Upper Oxfordian of Central Poland. When compared with those from the home-area of ammonites of the genus Amoeboceras, these invasive forms in the Submediterranean Province differ in their smaller shell-sizes, in the lack of differentiation of the shells into separate size-related morphs, and in the crowding of septa for up to one and a half whorls of thelast part of the phragmocone. The densely-spaced septa appear at the beginning of the fifth whorl, after the "normally" septate inner whorls. This fits well with the beginning of the sexual cycle postulated for the phyletically related genus Quenstedtoceras. Such a long section of phragmocone with densely-spaced septa, indicating a prolonged period of low rate of shell growth, may be related to the attainment of a long period of sexual maturity due to environmental conditions untypical for Boreal forms.

16

Ammonites and stratigraphy of the uppermost Bajocian and Lower Bathonian between Częstochowa and Wieluń, Central Poland

Matyja B., Wierzbowski A.

Acta Geologica Polonica

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2000

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Vol. 50, no. 2

191-209

EN

A detailed biostratigraphical study of the black clays and siltstones with ironstone nodules of the Ore Bearing Częstochowa Clay Formation in the brick-pits at Częstochowa and Wieluń resulted in recognition of the following standard ammonite zones and subzones: the Parkinsoni and Bomfordi subzones of the Parkinsoni Zone of the uppermost Bajocian; the Convergens, Macrescens and Yeovilensis subzones of the Zigzag Zone, and the Tenuiplicatus Zone of the Lower Bathonian. The ammonite faunas are of Submediterranean character, although markedly impoverished when compared with those of the most classic areas of the province. This impoverishment is especially well seen in the uppermost Bajocian - lowermost Bathonian part of the succession, where the only numerous ammonites are these of the genus Parkinsonia, together with rare representatives of Cadomites; and in theuppermost part of the Lower Bathonian, where representatives of the corresponding macro- and microconchs- Asphinctites tenuiplicatus (BRAUNS), and Polysphinctites secundus (WETZEL) - predominate. In the palaeontological part of the paper 14 species belonging to the genera Oxycerites, Parkinsonia, Cadomites, Wagnericeras, Asphinctites and Polysphinctites are descibed. Of these, particular attention is paid to a form referred to as Parkinsonia (Parkinsonia) aff. dorni ARKELL from the uppermost Bajocian, represented by several specimens of various growth stages, which may be tentatively compared with the poorly diagnostic small, incomplete type-specimens of P. dorni.