The stratigraphy of the Actinocamax plenus Subzone (Turonian) in the Anglo-Paris Basin

Jefferies, R. P. S.

doi:10.1016/s0016-7878(63)80011-5

Cited by 188 publications

(139 citation statements)

References 7 publications

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“…1), affords the thickest Cenomanian/Turonian boundary section in the AngloParis Basin (Jefferies, 1962(Jefferies, , 1963Gale et al 1993Gale et al , 2005Paul et al 1999). The macrofossil (Mortimore, 1986;Gale et al 1993Gale et al , 2000Gale et al , 2005 and microfossil (Paul et al 1999;Keller et al 2001) biostratigraphy of the section has been documented in detail, and Paul et al (1999) have published high-resolution (5-10 cm sample spacing) δ 13 C and δ 18 O curves for a 24 m section incorporating the Cenomanian/Turonian boundary.…”

Section: H Eastbourne East Sussex (Cenomanian/turonian Boundary Imentioning

confidence: 99%

“…This locality offers the most expanded stage boundary section in the chalk facies of NW Europe (Paul et al 1999) and is widely used as a reference section for stable-isotope studies. Plenus Marl bed numbers (Jefferies, 1963) are in white. Key macrofossil datum levels (Table 1) is defined (Bengtson, 1996;Kennedy, Walaszczyk & Cobban, 2000) as the base of Bed 86 at Pueblo ( The stratigraphy of the Plenus Marl was described in detail by Jefferies (1962Jefferies ( , 1963, who used a combination of lithological and faunal criteria to define eight beds (numbered 1-8, Fig.…”

Section: A11 Cenomanian/turonian Boundary Eventmentioning

confidence: 99%

“…5) that could be correlated throughout the Anglo-Paris Basin and beyond. The Plenus Marl is everywhere underlain by a strongly burrowed erosion surface at the top of the Grey Chalk, the sub-Plenus erosion surface, and is directly overlain by white nodular chalks formerly referred to the Melbourn Rock (Jefferies, 1963;Mortimore, 1986). In expanded basinal successions, such as that at Eastbourne (Fig.…”

Section: A11 Cenomanian/turonian Boundary Eventmentioning

confidence: 99%

“…The most detailed isotope record is available for carbonate (δ 13 C carb ) analysed in bulk sediments collected from Gun Gardens at Eastbourne, East Sussex (Paul et al 1999). The Eastbourne δ 13 C profile (thick black line, far left) shows three carbon-isotope peaks (dark grey shaded horizons) within the overall positive excursion (pale grey shaded interval): (a) near the base, within Plenus Marls Beds 2-3 of Jefferies (1962Jefferies ( , 1963; (b) in the middle, spanning the Plenus Marl/Ballard Cliff Member boundary (cf. Gale, 1996); and (c) at the top of the excursion, around Meads Marls 5-6 (MM5, MM6) of Mortimore (1986).…”

Section: A11 Cenomanian/turonian Boundary Eventmentioning

confidence: 99%

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Secular variation in Late Cretaceous carbon isotopes: a new δ¹³C carbonate reference curve for the Cenomanian–Campanian (99.6–70.6 Ma)

et al. 2006

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-Carbon stable-isotope variation through the Cenomanian-Santonian stages is characterized using data for 1769 bulk pelagic carbonate samples collected from seven Chalk successions in England. The sections show consistent stratigraphic trends and δ 13 C values that provide a basis for highresolution correlation. Positive and negative δ 13 C excursions and inflection points on the isotope profiles are used to define 72 isotope events. Key markers are provided by positive δ 13 C excursions of up to + 2 ‰: the Albian/Cenomanian Boundary Event; Mid-Cenomanian Event I; the Cenomanian/Turonian Boundary Event; the Bridgewick, Hitch Wood and Navigation events of Late Turonian age; and the Santonian/Campanian Boundary Event. Isotope events are isochronous within a framework provided by macrofossil datum levels and bentonite horizons. An age-calibrated composite δ 13 C reference curve and an isotope event stratigraphy are constructed using data from the English Chalk. The isotope stratigraphy is applied to successions in Germany, France, Spain and Italy. Correlation with pelagic sections at Gubbio, central Italy, demonstrates general agreement between biostratigraphic and chemostratigraphic criteria in the Cenomanian-Turonian stages, confirming established relationships between Tethyan planktonic foraminiferal and Boreal macrofossil biozonations. Correlation of the Coniacian-Santonian stages is less clear cut: magnetostratigraphic evidence for placing the base of Chron 33r near the base of the Upper Santonian is in good agreement with the carbon-isotope correlation, but generates significant anomalies regarding the placement of the Santonian and Campanian stage boundaries with respect to Tethyan planktonic foraminiferal and nannofossil zones. Isotope stratigraphy offers a more reliable criterion for detailed correlation of Cenomanian-Santonian strata than biostratigraphy. With the addition of Campanian δ 13 C data from one of the English sections, a composite Cenomanian-Campanian age-calibrated reference curve is presented that can be utilized in future chemostratigraphic studies.The Cenomanian-Campanian carbon-isotope curve is remarkably similar in shape to supposedly eustatic sea-level curves: increasing δ 13 C values accompanying sea-level rise associated with transgression, and falling δ 13 C values characterizing sea-level fall and regression. The correlation between carbon isotopes and sea-level is explained by variations in epicontinental sea area affecting organic-matter burial fluxes: increasing shallow sea-floor area and increased accommodation space accompanying sea-level rise allowed more efficient burial of marine organic matter, with the preferential removal of 12 C from the marine carbon reservoir. During sea-level fall, reduced seafloor area, marine erosion of previously deposited sediments, and exposure of basin margins led to reduced organiccarbon burial fluxes and oxidation of previously deposited organic matter, causing falling δ 13 C values. Additionally, drowning of carbonate platforms during...

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Section: H Eastbourne East Sussex (Cenomanian/turonian Boundary Imentioning

confidence: 99%

Section: A11 Cenomanian/turonian Boundary Eventmentioning

confidence: 99%

Section: A11 Cenomanian/turonian Boundary Eventmentioning

confidence: 99%

Section: A11 Cenomanian/turonian Boundary Eventmentioning

confidence: 99%

See 2 more Smart Citations

Secular variation in Late Cretaceous carbon isotopes: a new δ¹³C carbonate reference curve for the Cenomanian–Campanian (99.6–70.6 Ma)

et al. 2006

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“…In the Turonian type area, elements of the Sciponoceras gracile assemblage have been reported from the Craie marneuse at the base of the Turonian in the Fretevou section (Rawson and others, 1978). In northern France and southeastern England, the lower part of the Sciponoceras gracile zone includes the Actinocamax plenus marls (Metoicoceras geslinianum and M. gourdoni zones of Jefferies, 1962) Clinch, Ga.…”

Section: Cenomanian-turonian European Stage Boundarymentioning

confidence: 99%

Upper Cretaceous subsurface stratigraphy and structure of coastal Georgia and South Carolina

Valentine¹

1982

Professional Paper

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Spatial extent and degree of oxygen depletion in the deep proto‐North Atlantic basin during Oceanic Anoxic Event 2

Helmond

Baroni

Sluijs

et al. 2014

Geochem Geophys Geosyst

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Massive organic matter burial due to widespread ocean anoxia across the Cenomanian/Turonian boundary event (94 Ma) resulted in a major perturbation of the global carbon cycle: the so-called Oceanic Anoxic Event 2 (OAE2). The characteristics and spatial distribution of the OAE2 deposits that formed in the deep basin of the proto-North Atlantic remain poorly described, however. Here we present proxy data of redox sensitive (trace) elements (e.g., Mo, Fe/Al, C org /P tot , and Mn) for OAE2 sediments from five Deep Sea Drilling Project and Ocean Drilling Program sites located in the deep proto-North Atlantic basin. Our results highlight that bottom waters in the entire deep proto-North Atlantic were anoxic during most of OAE2. Furthermore, regressions of Mo with total organic carbon content (TOC), previously shown to document the degree of water mass restriction, confirm that the water circulation in the proto-North Atlantic basin was severely restricted during OAE2. Comparison of these values to Mo/TOC ratios in the present-day Black Sea suggests a renewal frequency of the deep proto-North Atlantic water mass of between 0.5 and 4 ka, compared to a maximum of 200 years for the present-day northern Atlantic. The Plenus Cold Event, a cooler episode during the early stages of OAE2 hypothesized to be caused by declining pCO 2 due to extensive burial of organic matter, appears to have led to temporary re-oxygenation of the bottom water in the deep proto-North Atlantic basin during OAE2.

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The stratigraphy of the Actinocamax plenus Subzone (Turonian) in the Anglo-Paris Basin

Cited by 188 publications

References 7 publications

Secular variation in Late Cretaceous carbon isotopes: a new δ¹³C carbonate reference curve for the Cenomanian–Campanian (99.6–70.6 Ma)

Secular variation in Late Cretaceous carbon isotopes: a new δ¹³C carbonate reference curve for the Cenomanian–Campanian (99.6–70.6 Ma)

Upper Cretaceous subsurface stratigraphy and structure of coastal Georgia and South Carolina

Spatial extent and degree of oxygen depletion in the deep proto‐North Atlantic basin during Oceanic Anoxic Event 2

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The stratigraphy of the Actinocamax plenus Subzone (Turonian) in the Anglo-Paris Basin

Cited by 188 publications

References 7 publications

Secular variation in Late Cretaceous carbon isotopes: a new δ13C carbonate reference curve for the Cenomanian–Campanian (99.6–70.6 Ma)

Secular variation in Late Cretaceous carbon isotopes: a new δ13C carbonate reference curve for the Cenomanian–Campanian (99.6–70.6 Ma)

Upper Cretaceous subsurface stratigraphy and structure of coastal Georgia and South Carolina

Spatial extent and degree of oxygen depletion in the deep proto‐North Atlantic basin during Oceanic Anoxic Event 2

Contact Info

Product

Resources

About

Secular variation in Late Cretaceous carbon isotopes: a new δ¹³C carbonate reference curve for the Cenomanian–Campanian (99.6–70.6 Ma)

Secular variation in Late Cretaceous carbon isotopes: a new δ¹³C carbonate reference curve for the Cenomanian–Campanian (99.6–70.6 Ma)