The Santonian-Campanian reversed polarity magnetozone and the Late Cretaceous magnetostratigraphical time-scale

Pechersky, D. M.; Naidin, D. P.; Molostovsky, Edward A.

doi:10.1016/0195-6671(83)90039-3

Cited by 8 publications

(8 citation statements)

References 12 publications

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“…Although generally believed to be of planktic or nektonic habit, strong arguments can be advanced to support a benthic mode of life for these ainoids (Milsom et al, 1994). The earlier species Coast, USA (Mississippi; Stephenson and Monroe, 1940;Texas;Marks, 1952), Europe (England, Northern Ireland, France, Germany; Sieverts, 1927), the former Soviet Union (Ukraine, Crimea, Middle Urals, Caucasus, Kopet Dagh, Turkmenistan;Pechersky et al, 1983;Klikushin, 1983), southern India (Stoliczka, 1872), Africa (Algeria; Peron, 1898;Madagascar;Besairie, 1936) and Western Australia (Perth Basin; Withers, 1924;Feldtmann, 1963;Carnarvon Basin;Clarke and Teichert, 1948).…”

Section: The Crinoids Uintacrinus and Marsupitesmentioning

confidence: 99%

“…This was subsequently traced widely in the (former) Soviet Union in marine sediments to Central Asia, Transcaspia, the Lesser Caucasus, the Russian Platform and Sakhalin. At Tuarkyr, in Turkmenia, the reversed zone is some 50m thick and includes Upper Santonian beds with Mnrsupites testudinarius, and Lower Campanian strata with the echinoid Ofaster (Pechersky et al, 1983).…”

Section: Magnetochron 33rmentioning

confidence: 99%

“…In southern England the base of 33r is situated considerably lower in the underlying Uintacnnus socialis Zone. In Turkmenia, the reversal is known to include the Marsupites testudinarius Zone (Pechersky et al, 1983). Two possible reasons for this discrepancy are: (i) G. eleoata is significantly diachronous in its appearance between Europe and the Gulf…”

Section: Gubbio Italymentioning

confidence: 99%

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Definition and global correlation of the Santonian‐Campanian boundary

et al. 1995

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Review of biostratigraphical evidence from different regions shows that criteria used by workers on various marine fossil groups to define the Santonian‐Campanian boundary differ considerably in relative age and position. Probably the most widely recognizable of these criteria is the extinction of the distinctive crinoid Marsupites testudinarius (North America, Europe, Asia, north Africa, Australia), which, coincides exactly with two separate definitions of the boundary ‐ appearances of the ammonite Placenticeras bidorsatum and the belemnite Gonioteuthis granulataquadrata ‐ and may also coincide with a third ‐ entry of the planktic foraminiferan Globotruncana elevata. A comparison of evidence from upper Santonian and lower Campanian successions in widely separated regions allows us to place a series of important biostratigraphical markers in correct order. Defining the boundary at the extinction of M. testudinarius corresponds to a 87Sr/86Sr of 0.707479, and a small positive excursion in δ13C. The base of magnetochron 33R, generally considered to coincide with, or fall just above the base of the Campanian, is shown to lie within the upper Santonian Uintacrinus socialis Zone.

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Section: The Crinoids Uintacrinus and Marsupitesmentioning

confidence: 99%

Section: Magnetochron 33rmentioning

confidence: 99%

Section: Gubbio Italymentioning

confidence: 99%

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Definition and global correlation of the Santonian‐Campanian boundary

et al. 1995

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“…14). In England, the Chron 34n/33r boundary occurs a short distance above the base of the Upper Santonian in the lower Uintacrinus Zone Montgomery et al 1998), consistent with its position in Russia (Pechersky, Naidin & Molotovsky, 1983). In Italy, the reversal has generally been regarded as occurring immediately above the base of the Campanian Alvarez & Lowrie, 1978;Cresta, Monechi & Parisi, 1989;Premoli Silva & Sliter, 1995).…”

Section: A Boreal-tethyan Carbon-isotope Correlationmentioning

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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“…However, the data available are not sufficient to judge about fine details. It should be emphasized that the growth of paleointensity and, especially, the abrupt growth of the paleointensity variations, began from the time of about 80 Ma, this time marking the upper boundary of the Jalal hyperchron mainly of normal geomagnetic polarity (relatively stable state of the geomagnetic field) and a transition to the hyperchron of the frequent reversals (unstable state of the field) [Pechersky et al, 1983] (Figure 1a). …”

Section: Paleointensitymentioning

confidence: 99%

The Mesozoic-Cenozoic boundary: Paleomagnetic characteristic

Pechersky¹,

Garbuzenko²

2005

Russ. J. Earth Sci.

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Abstract. The purpose of this paper is to consider the behavior of the geomagnetic field in the vicinity of the Mesozoic-Cenozoic (Mz-Kz) boundary, in particular, of the paleointensity and polarity of the field, the frequency of geomagnetic polarity reversals, the total magnitude of the field direction variations, and the behavior of the magnetic susceptibility of oceanic sediments in the vicinity of the Mz-Kz boundary. As to these paleomagnetic events, worthy of mention is the change in the variation conditions at the Mesozoic-Cenozoic boundary. It is global growth of the average variation magnitude from 8• -8.5• in the Late Cretaceous to 11.5• in the Early Cenozoic. The global character of this event suggests a general change in the generation of the geomagnetic field direction variations in the vicinity of the Mz-Kz boundary. A change in the Earth core conditions, causing the reversals of the geomagnetic field, began at ∼80 Ma, that is, notably earlier than the Mz-Kz boundary, and, hence, was not associated directly with this boundary, nor with the generation of variations in the geomagnetic field direction. Some local changes in the variations of the magnetic field direction were associated with the formation of plumes near the core-mantle boundary, yet, the plumes have originated 20-40 million years prior to the Mz-Kz boundary. As follows from the examination of sequences of oceanic sediments (DSDP and ODP data), the Mz-Kz boundary is often, but not necessarily, marked by a peak of magnetic susceptibility (κ-peak), i.e. that is not a characteristic feature of the Mz-Kz boundary. The accumulation of magnetic materials in the sediments lasted from a few dozens of thousand years (more common estimates) to hundreds of thousand years. And, where this interval is observed, it does include the Mz-Kz biostratigraphic boundary, except for very rare cases. The Mz-Kz biostratigraphic boundary is always restricted to the C29r chron, but its position varies as a function of its paleolatitude, amounting to about 0.7 Myr. The highest κ-peak values are close to the epicenters of active plumes, but high κ-peaks have been found far from the plumes.

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The Santonian-Campanian reversed polarity magnetozone and the Late Cretaceous magnetostratigraphical time-scale

Cited by 8 publications

References 12 publications

Definition and global correlation of the Santonian‐Campanian boundary

Definition and global correlation of the Santonian‐Campanian boundary

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

The Mesozoic-Cenozoic boundary: Paleomagnetic characteristic

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The Santonian-Campanian reversed polarity magnetozone and the Late Cretaceous magnetostratigraphical time-scale

Cited by 8 publications

References 12 publications

Definition and global correlation of the Santonian‐Campanian boundary

Definition and global correlation of the Santonian‐Campanian boundary

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

The Mesozoic-Cenozoic boundary: Paleomagnetic characteristic

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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)