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Późnokredowa tektoniczno-sedymentacyjna ewolucja północnej Polski : opracowanie na podstawie regionalnych danych sejsmicznych

Stachowska Aleksandra, Krzywiec Piotr

Przegląd Geologiczny

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2024

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Vol. 72, nr 6

270--279

EN

Seismostratigraphic interpretation of the Cretaceous succession of northern Poland was based on regional geo-seismic transects, consisting, mostly, of unique, high-resolution, regional seismic profiles of the Poland SPANTMseismic survey, calibrated by geophysical, stratigraphic and lithological data from several deep boreholes. The upper Albian - Upper Cretaceous succession was divided into 5 seismostratigraphic units. The seismic facies have also been characterized. So far, the interpretation ofthe regional architecture ofthe Upper Cretaceous sedimentary cover of the East European Craton was commonly based on the classic, layer-cake model, assuming simple correlations of stratigraphic units between boreholes. The regional geophysical profiles from the Poland SPANTMsurvey revealed, however, a more complex picture. Within the upper Albian - Upper Cretaceous succession, two major units have been identified that are divided by regional mid-Upper Cretaceous unconformity. Within this succession, numerous clinoforms and erosional incisions have been recognized that are incompatible with the formerly applied layer-cake model. Two systems of contour currents (N-S and NW-SE) were identified as active during the deposition of mostly syn-inversion Upper Cretaceous succession. A new tectono-sedimentary model of the Late Cretaceous evolution of the shelf basin of northern Poland has been proposed that, which tentatively, linked depositional processes with the progressive lithospheric buckling during mid-Late Cretaceous sub-Hercynian tectonic movements.

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Depositional architecture of the Upper Cretaceous succession in central Poland (Grudziądz-Polik area) based on regional seismic data

Stachowska Aleksandra, Krzywiec Piotr

Geological Quarterly

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2021

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Vol. 65, No. 2

art. no. 21

EN

Interpretation of the regional high-resolution seismic data of the PolandSPANTM survey in the Grudziądz-Polik area revealed a new depositional architecture of the Upper Cretaceous succession that differs substantially from the previously assumed layer-cake model, commonly applied to Permian-Mesozoic sequences. A previously unrecognized regional unconformity, dividing the Upper Cretaceous succession into two units characterized by very different internal geometries, was identified and mapped. The lower unit, with a generally layer-cake internal pattern, is overlain by an upper unit composed of a regionally low-angle succession that pinches out toward the south. This newly revealed regional pattern remained unrecognized in previous regional compilations based on borehole data, which suggested that a layer-cake depositional architecture prevailed throughout the entire Upper Cretaceous. This new image of Upper Cretaceous depositional patterns has far-reaching consequences for understanding of the evolution of the Polish Basin in the Late Cretaceous, including its subsidence and burial history, deposition, and tectonic development. A re-evaluation of the chronostratigraphy of the Upper Cretaceous of the Polish Basin is needed to temporally constrain the succession of sedimentary and tectonic events revealed here.

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Rozwój sedymentacji dewońskiej w basenie łysogórsko-radomskim i lubelskim

Narkiewicz M., Narkiewicz K., Turnau E.

Prace Państwowego Instytutu Geologicznego

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2011

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T.196

289--318

PL

Basen łysogórsko-radomski (BŁR) ograniczony był od południa synsedymentacyjnym uskokiem świętokrzyskim o głębokich założeniach skorupowych. Od NE graniczył z basenem lubelskim (BL) wzdłuż wąskiej strefy czytelnej w środkowodewońskim rozkładzie sedymentacji. Jej głębsze założenia stanowił prawdopodobnie uskok podłoża w osiowej części elewacji radomsko-kraśnickiej, wpływający na sedymentację przynajmniej od emsu późnego. BL łączył się od SE z basenem lwowskim, który od wschodu był ograniczony przez lądowy masyw w rejonie tarczy ukraińskiej. Wczesnodewoński etap rozwoju basenów (lochkow–środkowy ems) został zapoczątkowany w sylurze późnym osadami otwartego szelfu, które w lochkowie środkowym i późnym przeszły w osady perylitoralne, przykryte (częściowo niezgodnie ?) grubą serią aluwialną. W etapie środkowodewońskim (późny ems-wczesny fran) szybkie tempo sedymentacji facji węglanowo-terygenicznych otwartego zbiornika BŁR było uwarunkowane przez pogrążanie się bloków podłoża. Natomiast w warunkach stabilnego podłoża BL niewielką przestrzeń akomodacji dla osadów płytkiego szelfu i platformy węglanowej kształtowały głównie transgresje eustatyczne. W etapie środkowo–późnofrańskim, na tę ostatnią tendencję nałożył się puls subsydencji związany z początkiem ryftowania w rowie Prypeci. Etap fameński zaznaczył się powstaniem depocentrum w centralnym segmencie BL i akumulacją niemal 2 km węglanowo-ilastych osadów głębokiego basenu szelfowego i otwartego szelfu, przechodzących ku górze w progradujące ku SW systemy przybrzeżnomorskie i lądowe. Depocentrum utworzyło się w układzie pull-apart między strefą Kocka a uskokiem Ursynowa–Kazimierza, równocześnie z główną fazą ryftowania basenu Prypeci.

EN

Łysogóry-Radom Basin (ŁRB) is bounded in the south by the deeply-rooted Holy Cross Fault. To NE it passes into the Lublin Basin (LB) along a narrow zone clearly reflected in the Middle Devonian depositional pattern. It was probably related to a basement fault along the axial part of the Radom–Kraśnik Elevation affecting deposition at least since the late Emsian onwards. BL continued to the Lviv Basin in SE, which was bordered from the east by the continental Ukrainian Massif. The Early Devonian stage of the basins development started in the latest Silurian with an open-shelf sedimentation passing in the middle to late Lochkovian into marginal marine clastics. This is (partly unconformably) overlain by a thick alluvial complex. Between late Emsian and early Frasnian rapid sedimentation of carbonate-terrigenous open marine facies in the ŁRB was controlled by basement blocks subsidence. On the other hand, under stable cratonic conditions of the BL much smaller accomodation space was generated mainly by eustatic transgressions allowing a mostly shallow-shelf and carbonate platform development. In the Middle Frasnian this pattern was overprinted by a subsidence pulse related to the initial Pripyat Graben rifting. The Famennian stage was marked by a depocentre development in the central LB segment, and an accumulation of nearly 2 km of sediments, starting with carbonate-shaly deposits of a shelf basin and open shelf, passing upwards into marginal-marine and continental systems prograding SW-wards. The depocentre formed in a pull-apartregime between the Kock and Ursynów–Kazimierz faults, parallel with the main phase of the Pripyat Graben rifting.

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Litostratygrafia, systemy depozycyjne i cykle transgresywno-regresywne dewonu basenu lubelskiego

Narkiewicz M.

Prace Państwowego Instytutu Geologicznego

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2011

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T.196

53--146

PL

W wyniku analizy 19 kluczowych profili wiertniczych, wspartej reinterpretacją materiałów publikowanych, zmodyfikowano i uzupełniono dotychczasowy formalny podział litostratygraficzny dewonu środkowego i górnego, obejmując nim cały basen lubelski. Wydzielono 6 nowych oraz zrewidowano 6 wcześniej wydzielonych formacji i ogniw. Jednostki litostratygraficzne przypisano do systemów depozycyjnych: od aluwialnego, przybrzeżnych systemów morsko-lądowych, przez platformę węglanową, płytki szelf, lagunę ewaporacyjną, po głębszy szelf i basen szelfowy. Wyróżniono 11 cykli transgresywno-regresywnych odpowiadających rangą sekwencjom trzeciego rzędu. Architektura depozycyjna odzwierciedla cztery etapy rozwoju basenu. Etap wczesnodewoński odpowiada jednemu megacyklowi T-R, złożonemu niemal wyłącznie z osadów terygenicznych, od ilasto-mulistych otwartomorskich po aluwialne systemy warunkowane tektoniczną ruchliwością bloków podłoża. Na etap środkowodewoński–wczesnofrański składa się 7 niegrubych cykli T-R rejestrujących znaczną zmienność w sukcesji środowisk depozycyjnych. Płytsze środowiska występują w SE i NE części basenu, erozja przeważa w części NW. Z etapem środkowo–późnofrańskim (3 cykle T-R) wiąże się wzrost tempa sedymentacji uwarunkowany przez puls subsydencji tektonicznej, przewaga węglanowych systemów otwartomorskich i największy zasięg zbiornika. Etap fameński, odpowiadający pojedynczemu cyklowi T-R, charakteryzuje się największymi miąższościami osadów i najsilniejszymi gradientami facjalnymi. Zaznaczył się wówczas rozwój wyraźnego depocentrum, a następnie aktywizacja tektoniczna wzdłuż obrzeżenia NE. Basen dewoński dzieli się na segmenty poprzeczne: komarowski (SE), lubelski (centralny) i stężycki (NW). Pierwszy charakteryzuje się rozwojem systemów proksymalnych, w tym lądowych, ale przy znacznej subsydencji. Drugi reprezentuje maksymalną subsydencję i najbardziej głębokowodne facje, natomiast trzeci – wyklinowanie osadów i/lub facje płytkomorskie w strefie obrzeża basenu, zwłaszcza w środkowym dewonie i franie.

EN

Previous lithostratigraphic sudivision of the Middle and Upper Devonian has been supplemented, modified and extended over the entire Lublin Basin in SE Poland as a result of investigations of 19 key borehole sections and reinterpretation of published data. Six new members have been defined, whereas six other units of a formation or member rank have been revised. The lithostratigraphic units have been ascribed to depositional systems ranging from alluvial and marginal marine to a carbonate platform, shallow restricted shelf, evaporative lagoon, to open-marine carbonate-shaly shelf and deeper shaly-carbonate shelf basin. The systems have been attributed to 11 transgressive-regressive (T-R) cycles corresponding to3rd order depositional sequences. The depositional architecture reflects four stages of a basin development. The Early Devonian stage corresponds to a single T-R megacycle, comprising terrigeneous sediments from open marine shaly basin to alluvial systems con-trolled partly by synsedimentary block movements. The Middle Devonian to Early Frasnian stage comprises 7 T-R cycles with a total thickness <400 m and displaying considerable depositional facies variability. Generally, shallower-water environments extended in SE and NE parts of the basin, whereas erosion prevailed in its NW segment. The Middle–Late Frasnian stage (3 T-R cycles) is characterized by initially increased depositional rates connected with a pulse of tectonic subsidence, predominance of open-marine carbonate systems, and a maximum basin extent. The Famennian developmental stage, corresponding to a single T-R cycle, is exceptional due to a maximum sediment-thickness and strong lateral facies and thickness gradients related to a distinct depocentre development, followed by increased activity of a tectonic zone in NE. The Devonian basin can be divided into three transversal segments: Komarów (SE), Lublin (central), and Stężyca (NW). The first one is characterized by a largest proportion of shallow-marine and alluvial facies, and a considerable total subsidence. The central segment represents a maximum subsidence and deepest marine facies, whereas the NW one –reductions of sediment-thickness and/or shallower-water facies near the basin margin, particularly in the Middle Devonian and Frasnian.

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Sequence stratigraphy of Carboniferous paralic deposits in the Lublin Basin (SE Poland)

Waksmundzka M.

Acta Geologica Polonica

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2010

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Vol. 60, no. 4

557-597

EN

Based on lithofacies analysis of clastic, clay and carbonate rocks, wireline logs and sequence stratigraphy, sixteen depositional sequences have been distinguished in the paralic Carboniferous succession of the Lublin Basin from the Visean to the base of Westphalian B. The facies evolution and depositional architecture of the deposits belonging to three types of depositional systems tracts, i.e. lowstand (LST), transgressive (TST) and highstand (HST) have been reconstructed. The sequences are bounded by type 1 basal unconformities formed during subaerial erosion following relative sea-level fall and lowstand. This erosion, that in some cases reached down to the LST deposits of the underlying sequences, mainly affected the HST deposits. Relative sea-level rise controlling the base level of the rivers during lowstand was the basic factor influencing facies development, cyclicity and thickness of fluvial deposits, as well as the vertical and lateral transformation of rivers in theparalic Carboniferous succession. Vertical transition of high- to low-energy fluvial environments can be observed within the LST. The LST deposits typically occur in incised shelf valleys and in non-incised fluvial systems. Within the LST of sequences 2 and 4 to 10 commonly occur medium and large systems of simple incised valleys that developed in a coastal-plain system. The LST of sequences 11 to 15 comprises large systems of compound incised valleys that developed in a piedmont system. Relative sealevel rise in the late lowstand, sea-level oscillations during transgression and highstand and the volume of sediment supply were the main factors influencing facies development, cyclicity, thickness and lateral distribution of the deltaic deposits, shallow-shelf shales and limestones. Within the TST commonly occur coarsening-upward and non-gradational cyclothems that correspond to parasequences and were formed in the distal parts of the inner-shelf delta lobes. In the HST, the most commontypes are coarsening-upward cyclothems developed during the progradation of innershelf delta lobes and small lake deltas, as well as non-gradational cyclothems formed in lakes on a delta plain without influence of delta lobes. The transgression of sequence 7 probably had the widest extent of all the sequences in the paralic Carboniferous succession of the Lublin Basin. It was presumably much wider to the N, NE and NW than the presently accepted boundaries of the basin. Based on analysis of three curves of relative sea-level changes in the paralic Carboniferous succession of the Lublin Basin and the transgressive-regressive curve for the Carboniferous of Western Europe, the sequences distinguished have been correlated with the chronostratigraphic scheme for the Carboniferous System. The diachronous commencement of sedimentation has been confirmed and evaluated. The lack of deposits of sequence 5 in the eastern part of the basin suggests the presence of a stratigraphicgap encompassing the upper Brigantian. The position and range of stratigraphic gaps present elsewhere in the basin has also been indicated. In the north-westernmost and easternmost parts of the study area the gap has the widest range, encompassing the upper Arnsbergian to lower Marsdenian strata. The mid-Carboniferous boundary between the Mississippian and Pennsylvanian has been located at the base of sequence 8.

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Depositional architecture of the Zabrze Beds (Namurian B) within the Main Anticline of the Upper Silesia Coal Basin, Poland

Kędzior A.

Studia Geologica Polonica

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2008

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Vol. 129

131-156

EN

The Zabrze Beds (Namurian B) constitute a part of the flexural Variscan foredeep Upper Silesia Coal Basin (USCB) infill. On the Main Anticline area this unit starts the continental stage of the basin development. The Zabrze Beds were deposited on an extensive alluvial plain probably constructed by meandering river systems. The fluvial sediments were accumulated both within channels and on overbank areas. The thick (<5 m) sandstone bodies are considered as the channel fills and usually form extensive sheets whose width/thickness ratio exceeds 15. The thinner sandstone bodies, fine-grained sediments and phytogenic material were deposited on the overbank areas. The thickness of the Zabrze Beds on the Main Anticline area decreases eastward from ~250 m down to 3 m over a distance of 35 km. The thickness and number of the sandstone bodies diminish eastward with the thickness of the whole unit. The thickest bodies occur in the western part of the studied area, attaining 60 m, whereas in the eastern part they rarely exceed 30 m. As a rule, the thick sandstone bodies are laterally extensive approaching up to 10 km. Subordinately appear isolated bodies that are usually thinner. In those areas where the coarse-grained sediments are in the minority the inter- connectedness ratio is relatively low. The deposition of the thick sandstone bodies is related to stabilization of the river banks with accompanied balanced aggradations of the overbank areas, or is result of superposition of several generations of channel fills. The coal seams are numerous in the Zabrze Beds despite the small thickness of this unit. The growth of successive generations with extended eastward areas reflects increasing positive accommodation space created mainly by flexural bending of the basin substratum. The thirteen coal seams that have been identified within the Zabrze Beds, occur in different classes of thickness. Except thick (<3 m) and very thick (up to 24 m) seams, the laterally extensive and continuous coal seams are present thin (>0.3 m) and often lenticular in shape. The zones where the coal seam increase in thickness have been observed and they were the result of coalescence or the superposition of successively younger generation peat bogs. The characteristic feature of the succession of coal seams is the eastward increase of their lateral extend. The va- rious types of coal seam splitting have been observed. These phenomena were caused by lateral migration of the channel belts and growth of the crevasse splays, or by action of synsedimentary faults.