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Badania stratygraficzne powłok antykorozyjnych mostu Zwierzynieckiego we Wrocławiu

Chmielewski Andrzej, Rabiega Józef, Olczyk Piotr

Inżynieria i Budownictwo

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2023

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R. 79, nr 3-4

119--124

PL

Most Zwierzyniecki nad Starą Odrą we Wrocławiu jest użytkowany już od 125 lat. Od jesieni 2021 r. obiekt przechodził remont w zakresie wymiany pomostu na chodnikach oraz zabezpieczeń antykorozyjnych konstrukcji stalowej. Jednym z założeń prowadzonych prac było wykonanie badań stratygraficznych w celu ustalenia pierwotnej kolorystyki mostu, aby po remoncie stalowe przęsło mostu otrzymało swoje oryginalne barwy.

EN

The article presents the condition of a building temporarily out of service without adequate protection against the influence of environmental factors. The survey of the facility revealed a number of damage to the supporting structure elements. The results of non-destructive tests and laboratory tests confirmed the impact of long-term shutdown of operation on the degradation of the structure and allowed for conclusions about the possibility of return ing it to use.

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Fine-resolution pollen-based evidences of farming and forest development, South-Eastern Estonia

Niinemets E., Saarse L.

Polish Journal of Ecology

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2007

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Vol. 55, nr 2

283-296

EN

The pollen stratigraphical and lithological data obtained from Lake Lasva, southern Estonia, are summarized. The land-use and vegetation history during the last 6300 years in an agricultural area with dense prehistoric setting is discussed. A high sedimentation rate and laminated structure of lake deposits enabled high-resolution palaeobotanical study of a 985 cm long core. Accelerator mass spectrometry [^14]C dates show good linearity and fit well with varve counts. Up to ca 2900 years BP, birch, pine, spruce and broad-leaved species, later mostly birch, pine and alder, grew in that area. The first weak signs of human impact were traced at 6300 years BP. Human activities were more pronounced be.tween 5400-5100 and 3800-3500 years ago, due to the foundation of Neolithic settlements not far from the lake. The first attempt of small-scale tillage, detected from the first finds of Triticum pollen, followed by a long-term gap, dates back to 5100 years BP. Crop cultivation (Cannabis, Hordeum, Triticum and Secale) became the main means of subsistence not until the Iron Age at about 1600-1400 years ago, but extensive arable farming started to develop 800 years ago, after the German crusaders invaded the area. Pollen dia.grams display several setbacks in arable farming, mostly caused by crop failure due to climate de-terioration and decrease in the population caused by famines, wars and epidemics.

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Integrated stratigraphy of the upper Lower - lower Middle Cenomanian of northern Germany and southern England

Wilmsen M.

Acta Geologica Polonica

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2007

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Vol. 57, no. 3

263-279

EN

A high-resolution stratigraphic calibration of the upper Lower (upper Mantelliceras dixoni Zone) and lower Middle Cenomanian (Cunningtoniceras inerme Zone and lower Acanthoceras rhotomagense Zone) based on an integrated analysis of macrofossil biostratigraphy, event, cyclo-, stable-isotope and sequence stratigraphy of northern German and southern England key sections is presented. Classic event stratigraphy has a good potential in refining biostratigraphic correlations as most of the classic bioevents are isochronous within the integrated stratigraphy. Many lithological event beds such as marker marls can be incorporated into the cyclo- and sequence stratigraphic framework, explaining their significance in interregional correlation. The best stratigraphic resolution provides the cyclostratigraphy based on the typical Cenomanian marl-limestone couplets and their stacking pattern, inferred to reflect orbital forcing of the Milankovitch frequency band: detailed bed-by-bed correlation of couplets (precession cycle, ca. 20 kyr) allows a stratigraphic calibration within [similar to]10 kyr time slices. Conspicuous marker marl beds embrace bundles of [similar to]five couplets and are related to the short eccentricity (100 kyr) cycle. However, for the upper Lower Cenomanian (dixoni Zone) it appears that the existing couplet scale is incomplete. Sequence stratigraphic analysis demonstrates that the investigated interval comprises the maximum flooding and highstand interval of an Early Cenomanian sequence, capped by a significant late dixoni Zone sequence boundary, followed by uppermost Lower to Middle Cenomanian lowstand and transgressive deposits grading into a Middle Cenomanian maximum flooding zone ("calcimetry break"). Carbon stable-isotope values are stable around 2[per mil] vs. V-PDB within the mid- and late dixoni Zone,related to equilibrium conditions during maximum flooding and highstand conditions of sea-level. The latest Early to earliest Middle Cenomanian sea-level fall and lowstand was accompanied by a negative [delta] [^13]C excursion of ca. 0.4[per mil] in couplets B34-B40 (Lower-Middle Cenomanian boundary isotope Event, LMCE, new name) followed by a rise of 0.4.0.6[per mil] [delta] [^13]C in couplets B41-C2 during the early transgressive systems tract (Middle Cenomanian [delta] [^13]C excursion MCE 1). These observations support the interpretation that the [delta] [^13]C signal is a good proxy for (eustatic) sea-level changes. The LMCE is suggested as a proxy marker for the base of the Middle Cenomanian Substage.

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Sukcesja osadowa miocenu w rejonie zrębu Ryszkowej Woli (obszar Sieniawa-Rudka), zapadlisko przedkarpackie: wyniki facjalnej i stratygraficznej interpretacji danych wiertniczych oraz sejsmiki 3D

Mastalerz K., Wysocka A., Krzywiec P., Kasiński J., Aleksandrowski P., Papiernik B., Ryzner-Siupik B., Siupik J.

Przegląd Geologiczny

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2006

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Vol. 54, nr 4

333-342

EN

TThe Polish Carpathian Foredeep Basin (PCFB) is the northern compartment of a foreland basin system that surrounds the Carpathian orogenic belt. The axis of the eastern part of the PCFB plunges gently towards SE, where the Miocene basin-fill succession exceeds 2000 metres in thickness. The Miocene succession developed in shallow marine ramp settings and is subdivided into 3 lithostratigraphic units: sub-evaporitic (onshore-to-nearshore), evaporitic, and supra-evaporitic (offshore-to-estuarine). The upper unit includes a siliciclastic series (Upper Badenian–Sarmatian), which constitutes the main segment of the succession. It displays an asymmetric, shallowing-up trend, expressed by the following sequence: hemipelagic-turbiditic-deltaic-low-energy nearshore-to-estuarine facies associations. Sediment accummulation in the basin has been significantly overprinted by higher-frequency cyclicity and encloses several genetic stratigraphic sequences bounded by MFS surfaces. An early phase of the basin development was characterised by high-rate subsidence and slow-rate sedimentation (hemipelagic facies). The turbiditic facies association identified within the Sieniawa–Rudka area resulted from southward progradation of a submarine fan/prodeltaic depositional system, mainly fed from the northern and north–western continental margins of the basin. An overall SE–ward palaeoslope inclination controlled the main phase of the deltaic progradation, which had gradually replaced the turbiditic systems. The late deltaic phase was characterised by ENE palaeotransport directions. The final phase of the basin filling took place in shallow-water, low-energy, nearshore-to-estuarine environments. In the early stage of the basin development, a complex system of NW–SE elongated basement pop-ups and flower structures in the Miocene succession were produced by reactivation and inversion of Mesozoic basement faults. The growth of these positive structures modified local subsidence patterns and affected the organisation of depositional systems of the siliciclastic series. A narrow elevation of the RyszkowaWola High (RWH) gradually grew above one of the pop-up structures. Complex structural-stratigraphic hydrocarbon traps developed along the RWH, due to interaction between the growth of local faults and the development of the successive depositional systems. Tidally-modified delta-top and estuarine facies are the most common hydrocarbon hosts within individual sequences of the „deltaic” segment of the succession..

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Analiza stratygraficzna utworów miocenu przedgórza Karpat na podstawie funkcji błędów predykcji dla profilowań geofizyki otworowej

Jarzyna J., Gręplowski Z.

Prace Instytutu Nafty i Gazu

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2006

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nr 137

419-426

PL

Obliczono funkcje PEFA (Prediction Error Filter Analysis) i INPEFA (INtegrated PEFA), powstające poprzez porównywanie wartości pomierzonych z obliczonymi (przewidywanymi), z wykorzystaniem funkcji błędów predykcji. Krzywa PEFA jest wskaźnikiem zmienności wyniku pomiaru z punku na punkt, natomiast krzywa INPEFA ilustruje trend zmian na wykresie profilowania. Funkcje PEFA i INPEFA obliczono korzystając z programu CycloLog 3.1 dla wybranych profilowań geofizyki otworowej z otworów rejonu Księżpola i Markowic w zapadlisku przedkarpackim. Wyniki uzyskane dla mioceńskich cienkowarstwowych formacji piaskowcowo-mułowcowo-iłowcowych dają możliwość analizy warunków ciągłości sedymentacji, zmiany na wykresach wskazują na punkty nagłych zmian w środowisku powstawania skał. Stanowią dodatkową informację możliwą do wykorzystania przy korelacji międzyotworowej na podstawie profilowań geofizyki otworowej. Mogą być przydatne przy identyfikacji horyzontów sejsmicznych.

EN

PEFA (Prediction Error Filter Analysis) and INPEFA (INtegrated PEFA) functions were calculated on the basis of differences between measured and predicted logs. PEFA log is an indicator of changes in the measured log from depth to depth, INPEFA curve illustrates trend of changes in the raw log. PEFA and INPEFA were obtained using CycloLog 3.1 for selected wells in Księżpol and Markowice fields in the Carpathian Foredeep. Results for the Miocene thinly-bedded sandstone-claystone-mudstone formations enable analysis of a continuity of sedimentation conditions and show places (depths) of rapid changes in rock sedimentation environment. These results provide additional information useful in cross-wells correlation on the basis of logs. They may be also applied in seismic data analysis.

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Stratygrafia dewońsko-karbońskiej serii węglanowej w rejonie Rajbrotu i Tarnawy

Matyja H., Tomaś A., Lipiec M., Turnau E.

Prace Państwowego Instytutu Geologicznego

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2001

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T. 174

33--60

PL

Zintegrowane badania biostratygraficzne, polegające na równoczesnym badaniu tych samych profilów przy pomocy konodontów, otwornic i palinomorf, aczkolwiek nie dały w pełni satysfakcjonujących wyników, pozwoliły na datowanie granic jednostek litostratygraficznych wyróżnionych przez Narkiewicza (2001), na dość wiarygodną wzajemną korelację profilów, przynajmniej na poziomie chronostratygraficznym, na oszacowanie rozmiaru lokalnych luk erozyjnych, a w przyszłości stać się mogą podstawą do szerszych korelacji na skalę regionalną. Początek sedymentacji węglanowych osadów dewońskich przypada w analizowanym obszarze na przełom wczesnego i środkowego dewonu, na pogranicze emsu i eiflu. W obrębie serii węglanowej stwierdzono obecność niewielkiej miąższości osadów środkowego dewonu, prawdopodobnie franu (jego obecności można się jedynie domyślać na podstawie położenia w profilach, brak jest natomiast, jak na razie, datowań biostratygraficznych), relatywnie dużej miąższości datowanych osadów famenu oraz turneju i wizenu: hastaru i iworu, prawdopodobnie również czadu i arundu, a także dobrze datowanego holkeru. Granica między dewonem a karbonem przebiega w obrębie jednej jednostki litostratygraficznej, kompleksu wapieni gruzłowych i ziarnistych, ale jej natura — ciągłość sedymentacji między dewonem a karbonem z objawami spłycenia, jak to ma miejsce w części profilów na świecie, czy też luka erozyjna — pozostaje nadal nieznana. Sedymentacja osadów węglanowych karbonu trwała w badanym obszarze od końca emsu lub początku eiflu aż do wizenu, co najmniej po holker, natomiast sedymentacja osadów klastycznych rozpoczęła się być może już w asbie, a na pewno w namurze, prawdopodobnie w arnsbergu—w dobie triangulus-knoxi (TK), jak wynika z badań Trzepierczyńskiej (2001). Obserwowana luka o tektoniczno-erozyjnym charakterze obejmuje więc późny wizen, asb i brigant. W żadnym z badanych trzech profilów nie znaleziono osadów tego wieku, natomiast w najwyższych partiach serii węglanowej w profilu Tarnawa 1, wydatowanych na podstawie otwornic jako wyższy turnej — iwor, zona Tournayella (Cf2), znalezione zostały w odwróconym porządku stratygraficznym, w niewielkim stopniu wymieszane, zespoły miospor identyfikujące wspomniane brakujące piętra najwyższej części wizenu, niżej miospory dolnej części brigantu (zona VF), wyżej asbu (zony TC i NM). W dolnych partiach osadów klastycznych w profilu Tarnawa 1, datowanych jako namur (prawdopodobnie arnsberg), notowane są również liczne i zróżnicowane taksonomicznie miospory, reprezentujące poziomy TC i NM asbu oraz poziom VF brigantu. Taki zapis stratygraficzny na pograniczu serii węglanowej i klastycznej w profilu Tarnawa 1 sugeruje dość skomplikowany scenariusz procesów i zdarzeń geologicznych, jakie mogły mieć miejsce w tym niewielkim obszarze pod koniec wizenu i na początku namuru: (1) depozycję osadów węglanowych prawdopodobnie aż po holker; (2) śródwizeński epizod tektoniczno-erozyjny, w wyniku którego usuwane mogły być węglanowe osady holkeru, arundu, czadu i części iworu; (3) prawdopodobnie depozycję niewielkiej miąższości klastycznych osadów asbu, brigantu i pendleju; (4) późnowizeński epizod tektoniczno-erozyjny, w wyniku którego usuwane być mogły sukcesywnie klastyczne osady pendleju, brigantu i asbu i (5)uruchomienie sedymentacji w namurze - prawdopodobnie w Arnsbergu.

EN

The subdivision in lithostratigraphical units presently used (Narkiewicz 2001) is schematically shown on Figure 4. Biostratigraphy of the Devonian and Carboniferous in the Tarnawa-Rajbrot area has been established using conodonts and foraminifers and palynomorphs. The three microfossil groups used in conjunction can facilitate better precision in dating and correlating of sequences. Unfortunately, for most of the Devonian and Lower Carboniferous limestone succession, the miospores recovered tend to be too much oxidized and poorly preserved to be useful. They are routinely used in the siliciclastic part of the sequence. Unfortunately, the biostratigraphic evidence is too much incomplete to firmly establish the boundary between the lithostratigraphic units as well as between the Devonian and Carboniferous successions (see Figure 4). Marly dolostones and limestones with bioturbations (DWMB) spans the Middle Devonian, limestones, dolomicrites and dolosparites (WDD) include part of the Middle Devonian, probably Frasnian and part of the Famennian. Nodular and grained limestones unit (WGZ) include the uppermost part of Famennian and part of the Tournaisian (up to the isosticha-Upper crenulata conodont Zone). The Devonian-Carboniferous boundary runs within this lithostratigraphic units but its nature remains unknown. Marly horizon (PM) spans the uppermost isosticha-Upper crenulata-Lower typicus conodont zones (Tournaisian - Ivorian), grained limestones (WZ) include upper part of the Tournaisian (Ivorian to Arundian), and upper limestones and marls unit (WGM) belong to the Viséan (Holkerian, Cf5 foraminifer Zone). Using the integrated results of conodont, foraminifer and palinomorph studies it is possible to conclude that the limestone succession spans the Middle and Upper Devonian, Tournaisian and much of the Viséan, up to the Holkerian. The siliciclastic sedimentation starts certainly at the begining of the Namurian (see Trzepierczyńska, 2001), maybe earlier (during the ?Asbian). There is a significant hiatus at the erosional boundary between the carbonate and clastic sequences which may span the late Asbian and Brigantian. Deposits of this age have been found in none of the three borehole sections. The uppermost t parts of the carbonate series of the Tarnawa 1 borehole, dated by foraminifers as the Upper Tournaisian Ivorian, Tournayella Zone, yielded miospore assemblages, which point to the above-mentioned missing stages of the uppermost Viséan, but occurring in a reverse stratigraphic order (lower in the sections younger miospores of the Brigantian VF zone, above in the section older miospores of the Asbian TC and NM zones). In the lower parts of the clastic sequence of the Tarnawa 1 borehole, dated as the Namurian (probably Arnsbergian), abundant and taxonomically diverse miospores representing the Asbian TC and NM, as well as Brigantian VF Zone, were also found. Such a stratigraphic record of the carbonate/clastic transition zone from the Tarnawa 1 borehole section suggests a fairly complicated succession of events, that may have taken place over this small area at the end of Viséan and beginning of the Namurian: (1) carbonate sedimentation, probably until the Holkerian (by analogy to the Rajbrot 2 borehole section); (2) Mid-Viséantectonic-erosional event that may have caused the removal of the Holkerian, Arundian, Chadian and a part of Ivorian deposits; (3) probable deposition of small thickness Asbian, Brigantian and Pendleian clastics; (4) Late-Viséan tectonic-erosional event which might have resulted in the removal of Pendleian, Brigantian and Asbian clastics; (5) renewal of deposition in the Namurian, probably Arnsbergian. Ivorian to Arundian), and upper limestones and marls unit (WGM) belong to the Viséan (Holkerian, Cf5 foraminifer Zone). Using the integrated results of conodont, foraminifer and palinomorph studies it is possible to conclude that the limestone succession spans the Middle and Upper Devonian, Tournaisian and much of the Viséan, up to the Holkerian. The siliciclastic sedimentation starts certainly at the begining of the Namurian (see Trzepierczyńska, 2001), maybe earlier (during the ?Asbian). There is a significant hiatus at the erosional boundary between the carbonate and clastic sequences which may span the late Asbian and Brigantian. Deposits of this age have been found in none of the three borehole sections. The uppermost tparts of the carbonate series of theTarnawa 1 borehole, dated by foraminifers as the Upper Tournaisian Ivorian, Tournayella Zone, yielded miospore assemblages, which point to the above-mentioned missing stages of the uppermost Viséan, but occurring in a reverse stratigraphic order (lower in the sections younger miospores of the Brigantian VF zone, above in the section older miospores of the Asbian TC and NM zones). In the lower parts of the clastic sequence of the Tarnawa 1 borehole, dated as the Namurian (probably Arnsbergian), abundant and taxonomically diverse miospores representing the Asbian TC and NM, as well as Brigantian VF Zone, were also found. Such a stratigraphic record of the carbonate/clastic transition zone from the Tarnawa 1 borehole section suggests a fairly complicated succession of events, that may have taken place over this small area at the end of Viséan and beginning of the Namurian: (1) carbonate sedimentation, probably until the Holkerian (by analogy to the Rajbrot 2 borehole section); (2) Mid-Viséantectonic-erosional event that may have caused the removal of the Holkerian, Arundian, Chadian and a part of Ivorian deposits; (3) probable deposition of small thickness Asbian, Brigantian and Pendleian clastics; (4) Late-Viséan tectonic-erosional event which might have resulted in the removal of Pendleian, Brigantian and Asbian clastics; (5) renewal of deposition in the Namurian, probably Arnsbergian.