Foraminiferal evidence for Cenomanian sequence stratigraphy and palaeoceanography of the Boulonnais (Paris Basin, northern France)
Identifieur interne : 001F09 ( Istex/Corpus ); précédent : 001F08; suivant : 001F10Foraminiferal evidence for Cenomanian sequence stratigraphy and palaeoceanography of the Boulonnais (Paris Basin, northern France)
Auteurs : Kai-Uwe Gr FeSource :
- Palaeogeography, Palaeoclimatology, Palaeoecology [ 0031-0182 ] ; 1999.
Abstract
A middle to upper Cenomanian chalk succession in the northwestern European Paris Basin (Escalles section) was investigated with respect to its sediment composition, biofacies, and foraminiferal content. Most planktic foraminifers exhibit a high-frequency cyclicity in their distribution pattern and show little relationship to the sequence stratigraphic subdivision. A few characteristic species of benthic foraminifers (Tritaxia pyramidata, Ataxophragmium compactum, Dorothia levis, and Gavelinella cenomana) are related in their frequency distribution to certain systems tracts. Other benthic foraminiferal species are more evenly distributed through the systems tracts. Cluster analysis and factor analysis allow the separation of three benthic foraminiferal biofacies domains, which exhibit a characteristic frequency distribution pattern with respect to sequence stratigraphy. Biofacies 1 is dominant in the highstand systems tract (HST), and biofacies 3 is characteristic for the transgressive systems tract (TST). Biofacies 2 is most abundant around the maximum flooding–downlap surface (mfs) and less abundant around the sequence boundary. Factor analysis shows that most of the variance in the data set is explained by variables related to plankton productivity. Variables related to changes in water depth and changes in sea-level have minor influence on the variance of the whole data set, but have some influence on the variance of the benthic foraminiferal data set. The different reaction of benthic and planktic foraminifers to relative sea-level changes is also recorded in the total number of foraminifers per gram sediment (foraminiferal number) and in the ratio between planktic and benthic foraminifers (p/b-ratio). The foraminiferal number is highest at the mfs and lowest at the sequence boundaries of the investigated depositional sequences. The p/b-ratio has no correlation with the sequence stratigraphic subdivision, but shows a high-frequency cyclicity. The abundance pattern of planktic foraminifers is controlled by changes in the productivity of calcareous plankton. The regular variation in calcareous plankton productivity leads to marl (low productivity)–chalk (high productivity) cycles that form conspicuous couplets in the section. The productivity cycles are also recorded in gamma-ray logs in the environmental setting of the Escalles section. In contrast, the abundance patterns of benthic foraminifers are more influenced by relative sea-level changes, changes in water depth, and variations in substrate composition. The stacking of probably precession-controlled development of couplets lead to a distinct 100,000-year cyclicity that does not match very well with published sequence stratigraphic subdivisions.
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DOI: 10.1016/S0031-0182(99)00080-2
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<record><TEI wicri:istexFullTextTei="biblStruct"><teiHeader><fileDesc><titleStmt><title>Foraminiferal evidence for Cenomanian sequence stratigraphy and palaeoceanography of the Boulonnais (Paris Basin, northern France)</title><author><name sortKey="Gr Fe, Kai Uwe" sort="Gr Fe, Kai Uwe" uniqKey="Gr Fe K" first="Kai-Uwe" last="Gr Fe">Kai-Uwe Gr Fe</name><affiliation><mods:affiliation>Department of Geosciences, University of Bremen, P.O. Box 33 04 40, D-28334 Bremen, Germany</mods:affiliation></affiliation></author></titleStmt><publicationStmt><idno type="wicri:source">ISTEX</idno><idno type="RBID">ISTEX:8E30D91F060704308F2F23D374A89A3E000207BE</idno><date when="1999" year="1999">1999</date><idno type="doi">10.1016/S0031-0182(99)00080-2</idno><idno type="url">https://api.istex.fr/document/8E30D91F060704308F2F23D374A89A3E000207BE/fulltext/pdf</idno><idno type="wicri:Area/Istex/Corpus">001F09</idno><idno type="wicri:explorRef" wicri:stream="Istex" wicri:step="Corpus" wicri:corpus="ISTEX">001F09</idno></publicationStmt><sourceDesc><biblStruct><analytic><title level="a">Foraminiferal evidence for Cenomanian sequence stratigraphy and palaeoceanography of the Boulonnais (Paris Basin, northern France)</title><author><name sortKey="Gr Fe, Kai Uwe" sort="Gr Fe, Kai Uwe" uniqKey="Gr Fe K" first="Kai-Uwe" last="Gr Fe">Kai-Uwe Gr Fe</name><affiliation><mods:affiliation>Department of Geosciences, University of Bremen, P.O. Box 33 04 40, D-28334 Bremen, Germany</mods:affiliation></affiliation></author></analytic><monogr></monogr><series><title level="j">Palaeogeography, Palaeoclimatology, Palaeoecology</title><title level="j" type="abbrev">PALAEO</title><idno type="ISSN">0031-0182</idno><imprint><publisher>ELSEVIER</publisher><date type="published" when="1999">1999</date><biblScope unit="volume">153</biblScope><biblScope unit="issue">1–4</biblScope><biblScope unit="page" from="41">41</biblScope><biblScope unit="page" to="70">70</biblScope></imprint><idno type="ISSN">0031-0182</idno></series><idno type="istex">8E30D91F060704308F2F23D374A89A3E000207BE</idno><idno type="DOI">10.1016/S0031-0182(99)00080-2</idno><idno type="PII">S0031-0182(99)00080-2</idno></biblStruct></sourceDesc><seriesStmt><idno type="ISSN">0031-0182</idno></seriesStmt></fileDesc><profileDesc><textClass></textClass><langUsage><language ident="en">en</language></langUsage></profileDesc></teiHeader><front><div type="abstract" xml:lang="en">A middle to upper Cenomanian chalk succession in the northwestern European Paris Basin (Escalles section) was investigated with respect to its sediment composition, biofacies, and foraminiferal content. Most planktic foraminifers exhibit a high-frequency cyclicity in their distribution pattern and show little relationship to the sequence stratigraphic subdivision. A few characteristic species of benthic foraminifers (Tritaxia pyramidata, Ataxophragmium compactum, Dorothia levis, and Gavelinella cenomana) are related in their frequency distribution to certain systems tracts. Other benthic foraminiferal species are more evenly distributed through the systems tracts. Cluster analysis and factor analysis allow the separation of three benthic foraminiferal biofacies domains, which exhibit a characteristic frequency distribution pattern with respect to sequence stratigraphy. Biofacies 1 is dominant in the highstand systems tract (HST), and biofacies 3 is characteristic for the transgressive systems tract (TST). Biofacies 2 is most abundant around the maximum flooding–downlap surface (mfs) and less abundant around the sequence boundary. Factor analysis shows that most of the variance in the data set is explained by variables related to plankton productivity. Variables related to changes in water depth and changes in sea-level have minor influence on the variance of the whole data set, but have some influence on the variance of the benthic foraminiferal data set. The different reaction of benthic and planktic foraminifers to relative sea-level changes is also recorded in the total number of foraminifers per gram sediment (foraminiferal number) and in the ratio between planktic and benthic foraminifers (p/b-ratio). The foraminiferal number is highest at the mfs and lowest at the sequence boundaries of the investigated depositional sequences. The p/b-ratio has no correlation with the sequence stratigraphic subdivision, but shows a high-frequency cyclicity. The abundance pattern of planktic foraminifers is controlled by changes in the productivity of calcareous plankton. The regular variation in calcareous plankton productivity leads to marl (low productivity)–chalk (high productivity) cycles that form conspicuous couplets in the section. The productivity cycles are also recorded in gamma-ray logs in the environmental setting of the Escalles section. In contrast, the abundance patterns of benthic foraminifers are more influenced by relative sea-level changes, changes in water depth, and variations in substrate composition. The stacking of probably precession-controlled development of couplets lead to a distinct 100,000-year cyclicity that does not match very well with published sequence stratigraphic subdivisions.</div></front></TEI><istex><corpusName>elsevier</corpusName><author><json:item><name>Kai-Uwe Gräfe</name><affiliations><json:string>Department of Geosciences, University of Bremen, P.O. Box 33 04 40, D-28334 Bremen, Germany</json:string></affiliations></json:item></author><subject><json:item><lang><json:string>eng</json:string></lang><value>Cretaceous</value></json:item><json:item><lang><json:string>eng</json:string></lang><value>Cenomanian</value></json:item><json:item><lang><json:string>eng</json:string></lang><value>sequence stratigraphy</value></json:item><json:item><lang><json:string>eng</json:string></lang><value>palaeoceanography</value></json:item><json:item><lang><json:string>eng</json:string></lang><value>foraminifers</value></json:item><json:item><lang><json:string>eng</json:string></lang><value>Paris Basin</value></json:item></subject><language><json:string>eng</json:string></language><originalGenre><json:string>Full-length article</json:string></originalGenre><abstract>A middle to upper Cenomanian chalk succession in the northwestern European Paris Basin (Escalles section) was investigated with respect to its sediment composition, biofacies, and foraminiferal content. Most planktic foraminifers exhibit a high-frequency cyclicity in their distribution pattern and show little relationship to the sequence stratigraphic subdivision. A few characteristic species of benthic foraminifers (Tritaxia pyramidata, Ataxophragmium compactum, Dorothia levis, and Gavelinella cenomana) are related in their frequency distribution to certain systems tracts. Other benthic foraminiferal species are more evenly distributed through the systems tracts. Cluster analysis and factor analysis allow the separation of three benthic foraminiferal biofacies domains, which exhibit a characteristic frequency distribution pattern with respect to sequence stratigraphy. Biofacies 1 is dominant in the highstand systems tract (HST), and biofacies 3 is characteristic for the transgressive systems tract (TST). Biofacies 2 is most abundant around the maximum flooding–downlap surface (mfs) and less abundant around the sequence boundary. Factor analysis shows that most of the variance in the data set is explained by variables related to plankton productivity. Variables related to changes in water depth and changes in sea-level have minor influence on the variance of the whole data set, but have some influence on the variance of the benthic foraminiferal data set. The different reaction of benthic and planktic foraminifers to relative sea-level changes is also recorded in the total number of foraminifers per gram sediment (foraminiferal number) and in the ratio between planktic and benthic foraminifers (p/b-ratio). The foraminiferal number is highest at the mfs and lowest at the sequence boundaries of the investigated depositional sequences. The p/b-ratio has no correlation with the sequence stratigraphic subdivision, but shows a high-frequency cyclicity. The abundance pattern of planktic foraminifers is controlled by changes in the productivity of calcareous plankton. The regular variation in calcareous plankton productivity leads to marl (low productivity)–chalk (high productivity) cycles that form conspicuous couplets in the section. The productivity cycles are also recorded in gamma-ray logs in the environmental setting of the Escalles section. In contrast, the abundance patterns of benthic foraminifers are more influenced by relative sea-level changes, changes in water depth, and variations in substrate composition. The stacking of probably precession-controlled development of couplets lead to a distinct 100,000-year cyclicity that does not match very well with published sequence stratigraphic subdivisions.</abstract><qualityIndicators><score>8</score><pdfVersion>1.2</pdfVersion><pdfPageSize>546 x 746 pts</pdfPageSize><refBibsNative>true</refBibsNative><keywordCount>6</keywordCount><abstractCharCount>2752</abstractCharCount><pdfWordCount>12613</pdfWordCount><pdfCharCount>91878</pdfCharCount><pdfPageCount>30</pdfPageCount><abstractWordCount>379</abstractWordCount></qualityIndicators><title>Foraminiferal evidence for Cenomanian sequence stratigraphy and palaeoceanography of the Boulonnais (Paris Basin, northern France)</title><pii><json:string>S0031-0182(99)00080-2</json:string></pii><refBibs><json:item><host><author></author></host></json:item><json:item><host><author></author></host></json:item><json:item><host><author></author></host></json:item><json:item><author><json:item><name>M.A. Arthur</name></json:item><json:item><name>D.J. 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Geol., Mem.</title></host><title>Evolution of the Arctic–North Atlantic and the Western Tethys</title></json:item><json:item><host><author></author></host></json:item></refBibs><genre><json:string>research-article</json:string></genre><host><volume>153</volume><pii><json:string>S0031-0182(00)X0065-X</json:string></pii><pages><last>70</last><first>41</first></pages><issn><json:string>0031-0182</json:string></issn><issue>1–4</issue><genre><json:string>journal</json:string></genre><language><json:string>unknown</json:string></language><title>Palaeogeography, Palaeoclimatology, Palaeoecology</title><publicationDate>1999</publicationDate></host><categories><wos><json:string>science</json:string><json:string>paleontology</json:string><json:string>geosciences, multidisciplinary</json:string><json:string>geography, physical</json:string></wos><scienceMetrix><json:string>natural sciences</json:string><json:string>earth & environmental sciences</json:string><json:string>paleontology</json:string></scienceMetrix></categories><publicationDate>1999</publicationDate><copyrightDate>1999</copyrightDate><doi><json:string>10.1016/S0031-0182(99)00080-2</json:string></doi><id>8E30D91F060704308F2F23D374A89A3E000207BE</id><score>0.42455107</score><fulltext><json:item><extension>pdf</extension><original>true</original><mimetype>application/pdf</mimetype><uri>https://api.istex.fr/document/8E30D91F060704308F2F23D374A89A3E000207BE/fulltext/pdf</uri></json:item><json:item><extension>zip</extension><original>false</original><mimetype>application/zip</mimetype><uri>https://api.istex.fr/document/8E30D91F060704308F2F23D374A89A3E000207BE/fulltext/zip</uri></json:item><istex:fulltextTEI uri="https://api.istex.fr/document/8E30D91F060704308F2F23D374A89A3E000207BE/fulltext/tei"><teiHeader><fileDesc><titleStmt><title level="a">Foraminiferal evidence for Cenomanian sequence stratigraphy and palaeoceanography of the Boulonnais (Paris Basin, northern France)</title></titleStmt><publicationStmt><authority>ISTEX</authority><publisher>ELSEVIER</publisher><availability><p>©1999 Elsevier Science B.V.</p></availability><date>1999</date></publicationStmt><notesStmt><note type="content">Fig. 1: Four major components that affect stratigraphic cycles in a basin. The component sediment supply is composed of three independent variables: siliciclastic supply, carbonate supply, and organic matter supply. Modified after Vail et al. (1987).</note><note type="content">Fig. 2: Sediment flux in a three-component system of carbonate (C), siliciclastics (S), and organic matter (OM) in Cenomanian chalks. The carbonate flux from calcareous plankton is the most important component (rectangle). Not to scale, ΔRSL = change in relative sea-level. Modified after Ricken (1993).</note><note type="content">Fig. 3: Palaeogeographic map of the Cenomanian to Turonian period of western Europe and North Africa. Modified after Ziegler (1988)and Philip et al. (1993). Abbreviations: AB = Alboran Basin; AKB = Alboran–Kabylian Block; AM = Armorican Massif; APF = Apulian Platform; BR = Briançonnais; CSH = Corsica–Sardinia High; EH = Ebro High; FC = Flemish Cap; GB = Grand Banks; IBM = Iberian Meseta; IM = Irish Massif; ISB = Ionian Sea Basin; J. = Julia Platform; LAT = Latium–Abruzzi Block; Luc.–Cam Lucania–Campania; MC = Massif Central; MM = Morocco Meseta; NFB = East Newfoundland Basin; OK = Orphan Knoll; PT = Porcupine Trough; RHB = Rockall–Hatton Bank; RM = Rhenish Massif; T = Trento Platform; TAB = Tagus Abyssal Plain; UGFZ = Ungawa Fracture Zone.</note><note type="content">Fig. 4: (a) Location plan of the investigated profile. (b) Outcrop sketch of the coastal cliff around Cap Blanc Nez with the location of the profiles that compose the Escalles section. The sections c.2 to c.7 were investigated by Robaszynski and Amédro (1980), the section CB was newly measured for this work. Section CB covers 42.2 to 76.7 m of the Escalles section (Fig. 5). CF = Crupes Formation (unit K, see Fig. 5). View from the coastline towards the land in the SE.</note><note type="content">Fig. 5: The Cenomanian part of the Escalles section, northern France. Biostratigraphic zonation and lithostratigraphy after Robaszynski and Amédro (1993). For comparison, two sequence stratigraphic interpretations are shown. The one of Robaszynski and Amédro (1993) is from the Escalles section, the one of Owen (1996)is from the nearby Folkestone/Dover section. Correlation of both sections after Robaszynski and Amédro (1986, fig. 16). Sub-Member 23 is the correlative equivalent of Jukes-Browne Bed 7 (Robaszynski and Amédro, 1986; Owen, 1996). Lithofacies, logging of the section, and ranges of planktic foraminifers between 0 and 42 m after Robaszynski and Amédro (1993), between 42 m and 81 m, this work. Abbreviations: A. = Albian; Tur. = Turonian; gesl. = geslinianum; Hvglt. = Helvetoglobotruncana; SF = Strouanne Formation; CF = Crupes Formation; GBN F. = Grand Blanc Nez Formation; SMW = Shelf Margin Wedge; TST = transgressive systems tract; HST = highstand systems tract; mfs = maximum flooding–downlap surface. For location of the section see Fig. 4.</note><note type="content">Fig. 6: The middle Cenomanian to upper Cenomanian part of the Escalles section (section CB, see Fig. 4b). The profile corresponds to 42.2 to 76.7 m of the section of Fig. 5. Stratigraphic subdivision after Robaszynski and Amédro (1993). Stratigraphic columns from left to right: division in substages; sequence stratigraphy after Robaszynski and Amédro (1993); formations; members; sub-members; couplets interpreted as precession cycles. Owen (1996)interpreted the top SMW-surface (arrow) as sequence boundary and the SMW below as part of the HST in the Folkestone–Dover section. Sub-Member 23 is the correlative equivalent of Jukes-Browne Bed 7 (Robaszynski and Amédro, 1986; Owen, 1996). Legend and abbreviations see Fig. 5. Location of the section see Fig. 4.</note><note type="content">Fig. 7: Foraminiferal number, some diversity parameters, and triangular plot after Stehli (1966)in the Escalles section (part CB, 42.2 to 76.7 m). Sequence stratigraphy after Robaszynski and Amédro (1993). Black arrow in Fig. 7a,b,d: top-SMW surface interpreted by Owen (1996)as sequence boundary and the SMW below as part of the HST in the Folkestone–Dover section. Legend and abbreviations for Fig. 7 see Fig. 5. (a) Total number of unfragmented foraminifers per gram sediment, 125 to 425 μm fraction. Meters of section see Figs. 5 and 6. (b) Number of benthic and planktic foraminiferal species, 125 to 425 μm fraction (Fig. 6). (c) Triangular plot of calcareous and agglutinated benthic foraminifers and of planktic foraminifers after Stehli (1966). (d) Shannon–Weaver diversity of foraminiferal samples; pi: percent of i-th species/100 (Murray, 1991).</note><note type="content">Fig. 8: Frequency distribution of five selected species and one genus of planktic foraminifers in the Escalles section (42.2 to 76.7 m). Percentage values are percents of total foraminiferal fauna based on census counts per gram sediment (Table 1). Meters refer to the section of Figs. 5 and 6, sequence stratigraphy after Robaszynski and Amédro (1993). Black arrow: top-SMW surface interpreted by Owen (1996)as sequence boundary and the SMW below as part of the HST in the Folkestone–Dover section. Legend and abbreviations see Fig. 5.</note><note type="content">Fig. 9: Water depth model and absolute sea-level model for the middle to upper Cenomanian of the Escalles section. The water depth model was calculated as average from two models: model WD1 was calculated with WD1=exp(3.58718+(0.03534×P)); P = number of planktic foraminifers in %, after Van Der Zwaan et al. (1990). Model WD2 was calculated as average of the water depth models of Lenticulina muensteri, Gavelinella cenomana, Gyroidinoides nitidus, and Praebulimina reussi (see Table 2). Absolute limit values for water depth of these species after Sikora and Olsson (1991). For the calculation of the absolute sea-level model see text. Sequence boundary (sb) and maximum flooding–downlap surface (mfs) after Robaszynski and Amédro (1993).</note><note type="content">Fig. 10: Frequency distribution of 10 species of benthic foraminifers in the Escalles section (42.2 to 76.7 m). Percentage values are percents of total foraminiferal fauna based on census counts per gram sediment (Table 1). Meters refer to the section of Figs. 5 and 6, sequence stratigraphy after Robaszynski and Amédro (1993). Black arrow: top-SMW surface interpreted by Owen (1996)as sequence boundary and the SMW below as part of the HST in the Folkestone–Dover section. Legend and abbreviations see Fig. 5.</note><note type="content">Fig. 11: (a) R-mode cluster analysis of the benthic foraminiferal fauna of the Escalles section (part CB, Fig. 6), complete linkage, distance measure: 1-Pearson-r. For explanation see text. Abbreviations: nitid = Gyroidinoides nitidus; gavce = Gavelinella cenomana; praeb = Praebulimina reussi and P. nannina; troc = Dorothia trochus; gaudry = Gaudryina (all species); ordi = Lenticulina ordinaris; cret = Pseudotextulariella cretosa; angl = Arenobulimina anglica; Lingu = Lingulogavelinella globosa; lag lageniids; plec Plectina mariae and P. cenomana; epo = Eponides cf. beisseli; vmuens = Verneuilina muensteri; gavba = Gavelinella gr. baltica; marg = Marginulinopsis; psi = Psilocitharella; muen = Lenticulina muensteri; nod = nodosariids; cym = Cymbalopora; fron = frondiculariids; lev = Dorothia levis; grad = Dorothia gradata; adv = Arenobulimina advena; pyr = Tritaxia pyramidata; comp = Ataxophragmium compactum; sara = Saracenaria jarvisi; anceps = Spiroplectammina anceps. The benthic foraminiferal fauna was grouped in eight clusters (stippled) and three biofacies domains, for discussion see text. (b) Varimax rotated factor analysis (principal axis factoring) of 27 input variables composed of benthic foraminiferal frequencies in the Escalles section (part CB, Fig. 6, Table 1). The calculation was done on five factors. For explanation see text. Abbreviations of input variables, see (a).</note><note type="content">Fig. 12: Frequency distribution of three biofacies domains of benthic foraminifers in the Escalles section (42.2 to 76.7 m). The biofacies domains are composed of clusters defined by the cluster analysis shown in Fig. 11a. Meters refer to the section of Figs. 5 and 6, sequence stratigraphy after Robaszynski and Amédro (1993). Black arrow: top-SMW surface interpreted by Owen (1996)as sequence boundary and the SMW below as part of the HST in the Folkestone–Dover section. Legend and abbreviations see Fig. 5.</note><note type="content">Fig. 13: Varimax rotated factor analysis (principal axis factoring) of 23 input variables from the Escalles section (part CB, Fig. 6). The calculation was done on six factors, explanation see text. Abbreviations of input variables: abssea = absolute sea-level model (Fig. 9); carb = carbonate content (Fig. 6); clay = clay content (Fig. 6); cocs = nannoplankton-proxy (Fig. 6); fortot = total number of foraminifers per gram sediment (Fig. 7a, Table 1); gamma = gamma-ray log (Fig. 6); meter = meters in section Escalles where samples were investigated; litho = lithofacies (Fig. 6), p/b = p/b-ratio (Fig. 6, Table 1); seqstr = sequence stratigraphic interpretation (Fig. 6); totpl = total number of planktic foraminifers per gram sediment (Table 1); wd = absolute values of water depth model (Fig. 9); bf1 to bf3 = benthic foraminiferal biofacies 1 to 3 (Fig. 12). (a) Plot of factor loadings of factor axes 1 and 2. For discussion see text. (b) Plot of factor loadings of factor axes 2 and 3. For discussion see text.</note><note type="content">Table 1: Census counts of foraminifers in the Escalles section (42.3 to 75.5 m) calculated per gram sediment and expressed as percentage of the whole, unfragmented foraminiferal fauna of the 125 to 425 μm fraction</note><note type="content">Table 2: Regression equations for each water depth model of the benthic foraminiferal species used in model WD2</note></notesStmt><sourceDesc><biblStruct type="inbook"><analytic><title level="a">Foraminiferal evidence for Cenomanian sequence stratigraphy and palaeoceanography of the Boulonnais (Paris Basin, northern France)</title><author xml:id="author-1"><persName><forename type="first">Kai-Uwe</forename><surname>Gräfe</surname></persName><note type="biography">Fax: +49 421 218 4451; E-mail: ugraefe@micropal.uni-bremen.de</note><affiliation>Department of Geosciences, University of Bremen, P.O. Box 33 04 40, D-28334 Bremen, Germany</affiliation></author></analytic><monogr><title level="j">Palaeogeography, Palaeoclimatology, Palaeoecology</title><title level="j" type="abbrev">PALAEO</title><idno type="pISSN">0031-0182</idno><idno type="PII">S0031-0182(00)X0065-X</idno><imprint><publisher>ELSEVIER</publisher><date type="published" when="1999"></date><biblScope unit="volume">153</biblScope><biblScope unit="issue">1–4</biblScope><biblScope unit="page" from="41">41</biblScope><biblScope unit="page" to="70">70</biblScope></imprint></monogr><idno type="istex">8E30D91F060704308F2F23D374A89A3E000207BE</idno><idno type="DOI">10.1016/S0031-0182(99)00080-2</idno><idno type="PII">S0031-0182(99)00080-2</idno></biblStruct></sourceDesc></fileDesc><profileDesc><creation><date>1999</date></creation><langUsage><language ident="en">en</language></langUsage><abstract xml:lang="en"><p>A middle to upper Cenomanian chalk succession in the northwestern European Paris Basin (Escalles section) was investigated with respect to its sediment composition, biofacies, and foraminiferal content. Most planktic foraminifers exhibit a high-frequency cyclicity in their distribution pattern and show little relationship to the sequence stratigraphic subdivision. A few characteristic species of benthic foraminifers (Tritaxia pyramidata, Ataxophragmium compactum, Dorothia levis, and Gavelinella cenomana) are related in their frequency distribution to certain systems tracts. Other benthic foraminiferal species are more evenly distributed through the systems tracts. Cluster analysis and factor analysis allow the separation of three benthic foraminiferal biofacies domains, which exhibit a characteristic frequency distribution pattern with respect to sequence stratigraphy. Biofacies 1 is dominant in the highstand systems tract (HST), and biofacies 3 is characteristic for the transgressive systems tract (TST). Biofacies 2 is most abundant around the maximum flooding–downlap surface (mfs) and less abundant around the sequence boundary. Factor analysis shows that most of the variance in the data set is explained by variables related to plankton productivity. Variables related to changes in water depth and changes in sea-level have minor influence on the variance of the whole data set, but have some influence on the variance of the benthic foraminiferal data set. The different reaction of benthic and planktic foraminifers to relative sea-level changes is also recorded in the total number of foraminifers per gram sediment (foraminiferal number) and in the ratio between planktic and benthic foraminifers (p/b-ratio). The foraminiferal number is highest at the mfs and lowest at the sequence boundaries of the investigated depositional sequences. The p/b-ratio has no correlation with the sequence stratigraphic subdivision, but shows a high-frequency cyclicity. The abundance pattern of planktic foraminifers is controlled by changes in the productivity of calcareous plankton. The regular variation in calcareous plankton productivity leads to marl (low productivity)–chalk (high productivity) cycles that form conspicuous couplets in the section. The productivity cycles are also recorded in gamma-ray logs in the environmental setting of the Escalles section. In contrast, the abundance patterns of benthic foraminifers are more influenced by relative sea-level changes, changes in water depth, and variations in substrate composition. The stacking of probably precession-controlled development of couplets lead to a distinct 100,000-year cyclicity that does not match very well with published sequence stratigraphic subdivisions.</p></abstract><textClass><keywords scheme="keyword"><list><head>Keywords</head><item><term>Cretaceous</term></item><item><term>Cenomanian</term></item><item><term>sequence stratigraphy</term></item><item><term>palaeoceanography</term></item><item><term>foraminifers</term></item><item><term>Paris Basin</term></item></list></keywords></textClass></profileDesc><revisionDesc><change when="1999">Published</change></revisionDesc></teiHeader></istex:fulltextTEI><json:item><extension>txt</extension><original>false</original><mimetype>text/plain</mimetype><uri>https://api.istex.fr/document/8E30D91F060704308F2F23D374A89A3E000207BE/fulltext/txt</uri></json:item></fulltext><metadata><istex:metadataXml wicri:clean="Elsevier, elements deleted: ce:floats; body; tail"><istex:xmlDeclaration>version="1.0" encoding="utf-8"</istex:xmlDeclaration><istex:docType PUBLIC="-//ES//DTD journal article DTD version 4.5.2//EN//XML" URI="art452.dtd" name="istex:docType"><istex:entity SYSTEM="gr1" NDATA="IMAGE" name="gr1"></istex:entity><istex:entity SYSTEM="gr2" NDATA="IMAGE" name="gr2"></istex:entity><istex:entity SYSTEM="gr3" NDATA="IMAGE" name="gr3"></istex:entity><istex:entity SYSTEM="gr4" NDATA="IMAGE" name="gr4"></istex:entity><istex:entity SYSTEM="gr5" NDATA="IMAGE" name="gr5"></istex:entity><istex:entity SYSTEM="gr6" NDATA="IMAGE" name="gr6"></istex:entity><istex:entity SYSTEM="gr7" NDATA="IMAGE" name="gr7"></istex:entity><istex:entity SYSTEM="gr8" NDATA="IMAGE" name="gr8"></istex:entity><istex:entity SYSTEM="gr9" NDATA="IMAGE" name="gr9"></istex:entity><istex:entity SYSTEM="gr10" NDATA="IMAGE" name="gr10"></istex:entity><istex:entity SYSTEM="gr11" NDATA="IMAGE" name="gr11"></istex:entity><istex:entity SYSTEM="gr12" NDATA="IMAGE" name="gr12"></istex:entity><istex:entity SYSTEM="gr13" NDATA="IMAGE" name="gr13"></istex:entity></istex:docType><istex:document><converted-article version="4.5.2" docsubtype="fla"><item-info><jid>PALAEO</jid><aid>2272</aid><ce:pii>S0031-0182(99)00080-2</ce:pii><ce:doi>10.1016/S0031-0182(99)00080-2</ce:doi><ce:copyright year="1999" type="full-transfer">Elsevier Science B.V.</ce:copyright></item-info><head><ce:title>Foraminiferal evidence for Cenomanian sequence stratigraphy and palaeoceanography of the Boulonnais (Paris Basin, northern France)</ce:title><ce:author-group><ce:author><ce:given-name>Kai-Uwe</ce:given-name><ce:surname>Gräfe</ce:surname><ce:cross-ref refid="CORR1">*</ce:cross-ref></ce:author><ce:affiliation><ce:textfn>Department of Geosciences, University of Bremen, P.O. Box 33 04 40, D-28334 Bremen, Germany</ce:textfn></ce:affiliation><ce:correspondence id="CORR1"><ce:label>*</ce:label><ce:text>Fax: +49 421 218 4451; E-mail: ugraefe@micropal.uni-bremen.de</ce:text></ce:correspondence></ce:author-group><ce:date-received day="3" month="2" year="1998"></ce:date-received><ce:date-accepted day="20" month="4" year="1999"></ce:date-accepted><ce:abstract><ce:section-title>Abstract</ce:section-title><ce:abstract-sec><ce:simple-para>A middle to upper Cenomanian chalk succession in the northwestern European Paris Basin (Escalles section) was investigated with respect to its sediment composition, biofacies, and foraminiferal content. Most planktic foraminifers exhibit a high-frequency cyclicity in their distribution pattern and show little relationship to the sequence stratigraphic subdivision. A few characteristic species of benthic foraminifers (<ce:italic>Tritaxia pyramidata</ce:italic>, <ce:italic>Ataxophragmium compactum</ce:italic>, <ce:italic>Dorothia levis</ce:italic>, and <ce:italic>Gavelinella cenomana</ce:italic>) are related in their frequency distribution to certain systems tracts. Other benthic foraminiferal species are more evenly distributed through the systems tracts. Cluster analysis and factor analysis allow the separation of three benthic foraminiferal biofacies domains, which exhibit a characteristic frequency distribution pattern with respect to sequence stratigraphy. Biofacies 1 is dominant in the highstand systems tract (HST), and biofacies 3 is characteristic for the transgressive systems tract (TST). Biofacies 2 is most abundant around the maximum flooding–downlap surface (mfs) and less abundant around the sequence boundary. Factor analysis shows that most of the variance in the data set is explained by variables related to plankton productivity. Variables related to changes in water depth and changes in sea-level have minor influence on the variance of the whole data set, but have some influence on the variance of the benthic foraminiferal data set. The different reaction of benthic and planktic foraminifers to relative sea-level changes is also recorded in the total number of foraminifers per gram sediment (foraminiferal number) and in the ratio between planktic and benthic foraminifers (p/b-ratio). The foraminiferal number is highest at the mfs and lowest at the sequence boundaries of the investigated depositional sequences. The p/b-ratio has no correlation with the sequence stratigraphic subdivision, but shows a high-frequency cyclicity. The abundance pattern of planktic foraminifers is controlled by changes in the productivity of calcareous plankton. The regular variation in calcareous plankton productivity leads to marl (low productivity)–chalk (high productivity) cycles that form conspicuous couplets in the section. The productivity cycles are also recorded in gamma-ray logs in the environmental setting of the Escalles section. In contrast, the abundance patterns of benthic foraminifers are more influenced by relative sea-level changes, changes in water depth, and variations in substrate composition. The stacking of probably precession-controlled development of couplets lead to a distinct 100,000-year cyclicity that does not match very well with published sequence stratigraphic subdivisions.</ce:simple-para></ce:abstract-sec></ce:abstract><ce:keywords class="keyword"><ce:section-title>Keywords</ce:section-title><ce:keyword><ce:text>Cretaceous</ce:text></ce:keyword><ce:keyword><ce:text>Cenomanian</ce:text></ce:keyword><ce:keyword><ce:text>sequence stratigraphy</ce:text></ce:keyword><ce:keyword><ce:text>palaeoceanography</ce:text></ce:keyword><ce:keyword><ce:text>foraminifers</ce:text></ce:keyword><ce:keyword><ce:text>Paris Basin</ce:text></ce:keyword></ce:keywords></head></converted-article></istex:document></istex:metadataXml><mods version="3.6"><titleInfo><title>Foraminiferal evidence for Cenomanian sequence stratigraphy and palaeoceanography of the Boulonnais (Paris Basin, northern France)</title></titleInfo><titleInfo type="alternative" contentType="CDATA"><title>Foraminiferal evidence for Cenomanian sequence stratigraphy and palaeoceanography of the Boulonnais (Paris Basin, northern France)</title></titleInfo><name type="personal"><namePart type="given">Kai-Uwe</namePart><namePart type="family">Gräfe</namePart><affiliation>Department of Geosciences, University of Bremen, P.O. Box 33 04 40, D-28334 Bremen, Germany</affiliation><description>Fax: +49 421 218 4451; E-mail: ugraefe@micropal.uni-bremen.de</description><role><roleTerm type="text">author</roleTerm></role></name><typeOfResource>text</typeOfResource><genre type="research-article" displayLabel="Full-length article"></genre><originInfo><publisher>ELSEVIER</publisher><dateIssued encoding="w3cdtf">1999</dateIssued><copyrightDate encoding="w3cdtf">1999</copyrightDate></originInfo><language><languageTerm type="code" authority="iso639-2b">eng</languageTerm><languageTerm type="code" authority="rfc3066">en</languageTerm></language><physicalDescription><internetMediaType>text/html</internetMediaType></physicalDescription><abstract lang="en">A middle to upper Cenomanian chalk succession in the northwestern European Paris Basin (Escalles section) was investigated with respect to its sediment composition, biofacies, and foraminiferal content. Most planktic foraminifers exhibit a high-frequency cyclicity in their distribution pattern and show little relationship to the sequence stratigraphic subdivision. A few characteristic species of benthic foraminifers (Tritaxia pyramidata, Ataxophragmium compactum, Dorothia levis, and Gavelinella cenomana) are related in their frequency distribution to certain systems tracts. Other benthic foraminiferal species are more evenly distributed through the systems tracts. Cluster analysis and factor analysis allow the separation of three benthic foraminiferal biofacies domains, which exhibit a characteristic frequency distribution pattern with respect to sequence stratigraphy. Biofacies 1 is dominant in the highstand systems tract (HST), and biofacies 3 is characteristic for the transgressive systems tract (TST). Biofacies 2 is most abundant around the maximum flooding–downlap surface (mfs) and less abundant around the sequence boundary. Factor analysis shows that most of the variance in the data set is explained by variables related to plankton productivity. Variables related to changes in water depth and changes in sea-level have minor influence on the variance of the whole data set, but have some influence on the variance of the benthic foraminiferal data set. The different reaction of benthic and planktic foraminifers to relative sea-level changes is also recorded in the total number of foraminifers per gram sediment (foraminiferal number) and in the ratio between planktic and benthic foraminifers (p/b-ratio). The foraminiferal number is highest at the mfs and lowest at the sequence boundaries of the investigated depositional sequences. The p/b-ratio has no correlation with the sequence stratigraphic subdivision, but shows a high-frequency cyclicity. The abundance pattern of planktic foraminifers is controlled by changes in the productivity of calcareous plankton. The regular variation in calcareous plankton productivity leads to marl (low productivity)–chalk (high productivity) cycles that form conspicuous couplets in the section. The productivity cycles are also recorded in gamma-ray logs in the environmental setting of the Escalles section. In contrast, the abundance patterns of benthic foraminifers are more influenced by relative sea-level changes, changes in water depth, and variations in substrate composition. The stacking of probably precession-controlled development of couplets lead to a distinct 100,000-year cyclicity that does not match very well with published sequence stratigraphic subdivisions.</abstract><note type="content">Fig. 1: Four major components that affect stratigraphic cycles in a basin. The component sediment supply is composed of three independent variables: siliciclastic supply, carbonate supply, and organic matter supply. Modified after Vail et al. (1987).</note><note type="content">Fig. 2: Sediment flux in a three-component system of carbonate (C), siliciclastics (S), and organic matter (OM) in Cenomanian chalks. The carbonate flux from calcareous plankton is the most important component (rectangle). Not to scale, ΔRSL = change in relative sea-level. Modified after Ricken (1993).</note><note type="content">Fig. 3: Palaeogeographic map of the Cenomanian to Turonian period of western Europe and North Africa. Modified after Ziegler (1988)and Philip et al. (1993). Abbreviations: AB = Alboran Basin; AKB = Alboran–Kabylian Block; AM = Armorican Massif; APF = Apulian Platform; BR = Briançonnais; CSH = Corsica–Sardinia High; EH = Ebro High; FC = Flemish Cap; GB = Grand Banks; IBM = Iberian Meseta; IM = Irish Massif; ISB = Ionian Sea Basin; J. = Julia Platform; LAT = Latium–Abruzzi Block; Luc.–Cam Lucania–Campania; MC = Massif Central; MM = Morocco Meseta; NFB = East Newfoundland Basin; OK = Orphan Knoll; PT = Porcupine Trough; RHB = Rockall–Hatton Bank; RM = Rhenish Massif; T = Trento Platform; TAB = Tagus Abyssal Plain; UGFZ = Ungawa Fracture Zone.</note><note type="content">Fig. 4: (a) Location plan of the investigated profile. (b) Outcrop sketch of the coastal cliff around Cap Blanc Nez with the location of the profiles that compose the Escalles section. The sections c.2 to c.7 were investigated by Robaszynski and Amédro (1980), the section CB was newly measured for this work. Section CB covers 42.2 to 76.7 m of the Escalles section (Fig. 5). CF = Crupes Formation (unit K, see Fig. 5). View from the coastline towards the land in the SE.</note><note type="content">Fig. 5: The Cenomanian part of the Escalles section, northern France. Biostratigraphic zonation and lithostratigraphy after Robaszynski and Amédro (1993). For comparison, two sequence stratigraphic interpretations are shown. The one of Robaszynski and Amédro (1993) is from the Escalles section, the one of Owen (1996)is from the nearby Folkestone/Dover section. Correlation of both sections after Robaszynski and Amédro (1986, fig. 16). Sub-Member 23 is the correlative equivalent of Jukes-Browne Bed 7 (Robaszynski and Amédro, 1986; Owen, 1996). Lithofacies, logging of the section, and ranges of planktic foraminifers between 0 and 42 m after Robaszynski and Amédro (1993), between 42 m and 81 m, this work. Abbreviations: A. = Albian; Tur. = Turonian; gesl. = geslinianum; Hvglt. = Helvetoglobotruncana; SF = Strouanne Formation; CF = Crupes Formation; GBN F. = Grand Blanc Nez Formation; SMW = Shelf Margin Wedge; TST = transgressive systems tract; HST = highstand systems tract; mfs = maximum flooding–downlap surface. For location of the section see Fig. 4.</note><note type="content">Fig. 6: The middle Cenomanian to upper Cenomanian part of the Escalles section (section CB, see Fig. 4b). The profile corresponds to 42.2 to 76.7 m of the section of Fig. 5. Stratigraphic subdivision after Robaszynski and Amédro (1993). Stratigraphic columns from left to right: division in substages; sequence stratigraphy after Robaszynski and Amédro (1993); formations; members; sub-members; couplets interpreted as precession cycles. Owen (1996)interpreted the top SMW-surface (arrow) as sequence boundary and the SMW below as part of the HST in the Folkestone–Dover section. Sub-Member 23 is the correlative equivalent of Jukes-Browne Bed 7 (Robaszynski and Amédro, 1986; Owen, 1996). Legend and abbreviations see Fig. 5. Location of the section see Fig. 4.</note><note type="content">Fig. 7: Foraminiferal number, some diversity parameters, and triangular plot after Stehli (1966)in the Escalles section (part CB, 42.2 to 76.7 m). Sequence stratigraphy after Robaszynski and Amédro (1993). Black arrow in Fig. 7a,b,d: top-SMW surface interpreted by Owen (1996)as sequence boundary and the SMW below as part of the HST in the Folkestone–Dover section. Legend and abbreviations for Fig. 7 see Fig. 5. (a) Total number of unfragmented foraminifers per gram sediment, 125 to 425 μm fraction. Meters of section see Figs. 5 and 6. (b) Number of benthic and planktic foraminiferal species, 125 to 425 μm fraction (Fig. 6). (c) Triangular plot of calcareous and agglutinated benthic foraminifers and of planktic foraminifers after Stehli (1966). (d) Shannon–Weaver diversity of foraminiferal samples; pi: percent of i-th species/100 (Murray, 1991).</note><note type="content">Fig. 8: Frequency distribution of five selected species and one genus of planktic foraminifers in the Escalles section (42.2 to 76.7 m). Percentage values are percents of total foraminiferal fauna based on census counts per gram sediment (Table 1). Meters refer to the section of Figs. 5 and 6, sequence stratigraphy after Robaszynski and Amédro (1993). Black arrow: top-SMW surface interpreted by Owen (1996)as sequence boundary and the SMW below as part of the HST in the Folkestone–Dover section. Legend and abbreviations see Fig. 5.</note><note type="content">Fig. 9: Water depth model and absolute sea-level model for the middle to upper Cenomanian of the Escalles section. The water depth model was calculated as average from two models: model WD1 was calculated with WD1=exp(3.58718+(0.03534×P)); P = number of planktic foraminifers in %, after Van Der Zwaan et al. (1990). Model WD2 was calculated as average of the water depth models of Lenticulina muensteri, Gavelinella cenomana, Gyroidinoides nitidus, and Praebulimina reussi (see Table 2). Absolute limit values for water depth of these species after Sikora and Olsson (1991). For the calculation of the absolute sea-level model see text. Sequence boundary (sb) and maximum flooding–downlap surface (mfs) after Robaszynski and Amédro (1993).</note><note type="content">Fig. 10: Frequency distribution of 10 species of benthic foraminifers in the Escalles section (42.2 to 76.7 m). Percentage values are percents of total foraminiferal fauna based on census counts per gram sediment (Table 1). Meters refer to the section of Figs. 5 and 6, sequence stratigraphy after Robaszynski and Amédro (1993). Black arrow: top-SMW surface interpreted by Owen (1996)as sequence boundary and the SMW below as part of the HST in the Folkestone–Dover section. Legend and abbreviations see Fig. 5.</note><note type="content">Fig. 11: (a) R-mode cluster analysis of the benthic foraminiferal fauna of the Escalles section (part CB, Fig. 6), complete linkage, distance measure: 1-Pearson-r. For explanation see text. Abbreviations: nitid = Gyroidinoides nitidus; gavce = Gavelinella cenomana; praeb = Praebulimina reussi and P. nannina; troc = Dorothia trochus; gaudry = Gaudryina (all species); ordi = Lenticulina ordinaris; cret = Pseudotextulariella cretosa; angl = Arenobulimina anglica; Lingu = Lingulogavelinella globosa; lag lageniids; plec Plectina mariae and P. cenomana; epo = Eponides cf. beisseli; vmuens = Verneuilina muensteri; gavba = Gavelinella gr. baltica; marg = Marginulinopsis; psi = Psilocitharella; muen = Lenticulina muensteri; nod = nodosariids; cym = Cymbalopora; fron = frondiculariids; lev = Dorothia levis; grad = Dorothia gradata; adv = Arenobulimina advena; pyr = Tritaxia pyramidata; comp = Ataxophragmium compactum; sara = Saracenaria jarvisi; anceps = Spiroplectammina anceps. The benthic foraminiferal fauna was grouped in eight clusters (stippled) and three biofacies domains, for discussion see text. (b) Varimax rotated factor analysis (principal axis factoring) of 27 input variables composed of benthic foraminiferal frequencies in the Escalles section (part CB, Fig. 6, Table 1). The calculation was done on five factors. For explanation see text. Abbreviations of input variables, see (a).</note><note type="content">Fig. 12: Frequency distribution of three biofacies domains of benthic foraminifers in the Escalles section (42.2 to 76.7 m). The biofacies domains are composed of clusters defined by the cluster analysis shown in Fig. 11a. Meters refer to the section of Figs. 5 and 6, sequence stratigraphy after Robaszynski and Amédro (1993). Black arrow: top-SMW surface interpreted by Owen (1996)as sequence boundary and the SMW below as part of the HST in the Folkestone–Dover section. Legend and abbreviations see Fig. 5.</note><note type="content">Fig. 13: Varimax rotated factor analysis (principal axis factoring) of 23 input variables from the Escalles section (part CB, Fig. 6). The calculation was done on six factors, explanation see text. Abbreviations of input variables: abssea = absolute sea-level model (Fig. 9); carb = carbonate content (Fig. 6); clay = clay content (Fig. 6); cocs = nannoplankton-proxy (Fig. 6); fortot = total number of foraminifers per gram sediment (Fig. 7a, Table 1); gamma = gamma-ray log (Fig. 6); meter = meters in section Escalles where samples were investigated; litho = lithofacies (Fig. 6), p/b = p/b-ratio (Fig. 6, Table 1); seqstr = sequence stratigraphic interpretation (Fig. 6); totpl = total number of planktic foraminifers per gram sediment (Table 1); wd = absolute values of water depth model (Fig. 9); bf1 to bf3 = benthic foraminiferal biofacies 1 to 3 (Fig. 12). (a) Plot of factor loadings of factor axes 1 and 2. For discussion see text. (b) Plot of factor loadings of factor axes 2 and 3. For discussion see text.</note><note type="content">Table 1: Census counts of foraminifers in the Escalles section (42.3 to 75.5 m) calculated per gram sediment and expressed as percentage of the whole, unfragmented foraminiferal fauna of the 125 to 425 μm fraction</note><note type="content">Table 2: Regression equations for each water depth model of the benthic foraminiferal species used in model WD2</note><subject><genre>Keywords</genre><topic>Cretaceous</topic><topic>Cenomanian</topic><topic>sequence stratigraphy</topic><topic>palaeoceanography</topic><topic>foraminifers</topic><topic>Paris Basin</topic></subject><relatedItem type="host"><titleInfo><title>Palaeogeography, Palaeoclimatology, Palaeoecology</title></titleInfo><titleInfo type="abbreviated"><title>PALAEO</title></titleInfo><genre type="journal">journal</genre><originInfo><dateIssued encoding="w3cdtf">19990915</dateIssued></originInfo><identifier type="ISSN">0031-0182</identifier><identifier type="PII">S0031-0182(00)X0065-X</identifier><part><date>19990915</date><detail type="volume"><number>153</number><caption>vol.</caption></detail><detail type="issue"><number>1–4</number><caption>no.</caption></detail><extent unit="issue pages"><start>1</start><end>360</end></extent><extent unit="pages"><start>41</start><end>70</end></extent></part></relatedItem><identifier type="istex">8E30D91F060704308F2F23D374A89A3E000207BE</identifier><identifier type="DOI">10.1016/S0031-0182(99)00080-2</identifier><identifier type="PII">S0031-0182(99)00080-2</identifier><accessCondition type="use and reproduction" contentType="copyright">©1999 Elsevier Science B.V.</accessCondition><recordInfo><recordContentSource>ELSEVIER</recordContentSource><recordOrigin>Elsevier Science B.V., ©1999</recordOrigin></recordInfo></mods></metadata><serie></serie></istex></record>Pour manipuler ce document sous Unix (Dilib)
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