The great transgressions of the Late Cretaceous

Hancock, Jake M.; Kauffman, Erle G.

doi:10.1144/gsjgs.136.2.0175

Cited by 409 publications

(150 citation statements)

References 18 publications

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“…15) is correlated with the step towards more positive δ 13 C values above the East Cliff Event, culminating in the White Fall Event, above. A widespread Coniacian transgressive maximum (Hancock & Kauffman, 1979;Hancock, 2000) correlates with a broad δ 13 C maximum between the White Fall and Kingsdown events. Early and Late Santonian transgressions (Sahagian et al 1996;Miller et al 2003Miller et al , 2004 correspond to the Horseshoe Bay and Santonian/Campanian boundary positive carbon-isotope events (Fig.…”

Section: A Eustatic Sea-levelmentioning

confidence: 99%

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: A Eustatic Sea-levelmentioning

confidence: 99%

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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“…The early Albian (Lower Cretaceous) also saw at least three flooding events. From the Turonian to the Santonian (90-85 Ma), there was a period of stability when average global temperatures and sea levels stabilized before starting to fall again at the beginning of the Campanian (84-74 Ma) (Frakes 1986;Hancock & Kauffman 1979). The late Maastrichtian (66 Ma) was marked by a significant cooling of the oceans and the Cretaceous-Tertiary (K-T) event was accompanied by a sudden drop in the eustatic sea level and global temperatures.…”

Section: The Palaeoecological Context Of Diatom Originsmentioning

confidence: 99%

Evolution of the diatoms: insights from fossil, biological and molecular data

2006

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Molecular sequence analyses have yielded many important insights into diatom evolution, but there have been few attempts to relate these to the extensive fossil record of diatoms, probably because of unfamiliarity with the data available, which are scattered widely through the geological literature. We review the main features of molecular phylogenies and concentrate on the correspondence between these and the fossil record; we also review the evolution of major morphological, cytological and life cycle characteristics, and possible diatom origins. The first physical remains of diatoms are from the Jurassic, and well-preserved, diverse floras are available from the Lower Cretaceous. Though these are unequivocally identifiable as centric diatoms, none except a possible Stephanopyxis can be unequivocally linked to lineages of extant diatoms, although it is almost certain that members of the Coscinodiscophyceae (radial centrics) and Mediophyceae (polar centrics) were present; some display curious morphological features that hint at an unorthodox cell division mechanism and life cycle. It seems most likely that the earliest diatoms were marine, but recently discovered fossil deposits hint that episodes of terrestrial colonization may have occurred in the Mesozoic, though the main invasion of freshwaters appears to have been delayed until the Cenozoic. By the Upper Cretaceous, many lineages are present that can be convincingly related to extant diatom taxa. Pennate diatoms appear in the late Cretaceous and raphid diatoms in the Palaeocene, though molecular phylogenies imply that raphid diatoms did in fact evolve considerably earlier. Recent evidence shows that diatoms are substantially underclassified at the species level, with many semicryptic or cryptic species to be recognized; however, there is little prospect of being able to discriminate between such taxa in fossil material.

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“…If the aquifer followed a simple Gheyben-Hertzberg principle, it would require approximately 40-45 m of freshwater above sea level to drive the base of the aquifer as deep as these talus deposits (about 1700 m). Eustatic sea-level falls of tens to hundreds of meters occurred repeatedly throughout the mid and Late Cretaceous (Hancock and Kauffman, 1979;Vail et al, 1977, fig. 6).…”

Section: Freshwater Alterationmentioning

confidence: 99%

Alternative Diagenetic Models for Cretaceous Talus Deposits, Deep Sea Drilling Project Site 536, Gulf of Mexico

Halley¹,

Pierson²,

Schlager³

1984

Initial Reports of the Deep Sea Drilling Project

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Talus deposits recovered from Site 536 show evidence of aragonite dissolution, secondary porosity development, and calcite cementation. Although freshwater diagenesis could account for the petrographic features of the altered talus deposits, it does not uniquely account for isotopic or trace-element characteristics. Also, the hydrologic setting required for freshwater alteration is not easily demonstrated for the Campeche Bank. A mixing-zone model does not account for the available trace-element data, but does require somewhat less drastic assumptions about the size of the freshwater lens. Although a seawater (bottom-water) alteration model requires no hydrologic difficulties, unusual circumstances are required to account for the geochemical characteristics of the talus deposits using this model.

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The great transgressions of the Late Cretaceous

Cited by 409 publications

References 18 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)

Evolution of the diatoms: insights from fossil, biological and molecular data

Alternative Diagenetic Models for Cretaceous Talus Deposits, Deep Sea Drilling Project Site 536, Gulf of Mexico

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The great transgressions of the Late Cretaceous

Cited by 409 publications

References 18 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)

Evolution of the diatoms: insights from fossil, biological and molecular data

Alternative Diagenetic Models for Cretaceous Talus Deposits, Deep Sea Drilling Project Site 536, Gulf of Mexico

Contact Info

Product

Resources

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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)

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