Cenozoic and Cretaceous Biochronology of Planktonic Foraminifera and Calcareous Nannofossils

Anthonissen, D. Erik; Ogg, James G.

doi:10.1016/b978-0-444-59425-9.15003-6

Cited by 86 publications

(106 citation statements)

References 53 publications

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“…In addition to this definition based on sequence stratigraphy, paleoclimate and biostratigraphy, the Styrian tectonic phase documented by a strong uplift and the subsequent deepening led to the first Badenian transgression (Hohenegger et al 2009). Therefore, we place the Karpatian/Badenian boundary at 16.303 Ma, the top of C5Cn.2n (ATNTS 2012, Hilgen et al 2012) near the beginning of the Praeorbulina lineage (16.38 Ma; Wade et al 2011;Anthonissen & Ogg 2012); this confirms the original definition by Papp & Cicha (1978). This boundary definition and age, as defined by magnetostratigraphy, was also used by Kováč et al & OszczypkoClowes (2012) and Hohenegger & Wagreich (2012).…”

Section: Karpatian/badenian Boundarysupporting

confidence: 70%

“…We chose this age because it best approximates the base of plankton Zone M6, the Orbulina suturalis LOZ (Wade et al 2011) at 15.10 Ma, the calcareous nannoplankton boundary NN4/NN5 (Martini 1971;Anthonissen & Ogg 2012) positioned at 14.91 Ma, and to the Lan2/Ser1 sequence boundary at ca. 14.8 Ma ).…”

Section: Early Badenianmentioning

confidence: 99%

“…Strauss et al 2006;Schreilechner & Sachsenhofer 2007). The sequence boundaries of Hardenbol et al (1998) have to be newly calibrated due to the recently refined timing of the Neogene (Hilgen et al 2012;Anthonissen & Ogg 2012); as a result, they have not been used directly as geochronological constraints in our new subdivision of the Badenian based on biostratigraphy and magnetostratigraphy data from classic areas such as the Vienna Basin.…”

Section: Methodsmentioning

confidence: 99%

“…The beginning of the Early Badenian, here dated at 16.303 Ma, corresponds roughly to the base of foraminiferal plankton Zone M5, the Praeorbulina sicana LOZ (Wade et al 2011;Anthonissen & Ogg 2012). The Bur5/Lan1 sequence boundary estimated at ca.…”

Section: Early Badenianmentioning

confidence: 99%

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Timing of the Middle Miocene Badenian Stage of the Central Paratethys

Hohenegger

Ćorić

Wagreich

2014

Geologica Carpathica

132

101

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Abstract:A new and precisely defined chronometric subdivision of the Badenian (Middle Miocene, regional stage of Central Paratethys) is proposed. This uses global events, mainly geomagnetic polarity reversals as correlated chronometric boundaries, supported by climatic and sea-level changes in addition to isotope events and biostratigraphic data. The Karpatian/ Badenian boundary lies at 16.303 Ma, at the top of Chron C5Cn.2n, which is near the base of the Praeorbulina sicana Lowest-occurrence Zone (LOZ). The Badenian/Sarmatian boundary is placed at the top of polarity Chron C5Ar.2n, thus at 12.829 Ma. In relation to three sea level cycles TB 2.3, TB 2.4 and TB 2.5 and astronomically confirmed data, the Badenian can be divided into three parts of nearly equivalent duration. The Early Badenian as newly defined here ranges from 16.303 to 15.032 Ma (top of polarity Chron C5Bn.2n). The younger boundary correlates roughly to the base of the planktonic foraminifera Orbulina suturalis LOZ at 15.10 Ma, the HO (Highest Occurrence) of the nannofossil Helicosphaera ampliaperta at 14.91 Ma (NN4/NN5 boundary) and the Lan2/Ser1 sequence boundary at 14.80 Ma. The subsequent Mid Badenian ranges from 15.032 Ma to 13.82 Ma; the latter datum correlates with the base of the Serravallian, characterized by a strong global cooling event reflected in the oxygen isotope event Mi3b. The main part of cycle TB 2.4 falls into the Mid Badenian, which can be subdivided by a short cooling event at 14.24 Ma during the Middle Miocene Climate Transition (14.70 to 13.82 Ma). The HCO (Highest common occurrence) of the nannofossil Helicosphaera waltrans at 14.357 Ma supports this division, also seen in the tropical plankton Zones M6 Orbulina suturalis LOZ and M7 Fohsella peripheroacuta LOZ that correspond roughly to the lower and upper Lagenidae zones in the Vienna Basin, respectively. The Late Badenian is delimited in time at the base to 13.82 Ma by the Langhian/Serravallian boundary and at the top by the top of polarity Chron C5Ar.2n at 12.829 Ma. The Mediterranean Langhian/Serravallian boundary can be equated with the Mid/Late Badenian boundary at 13.82 Ma. However, the Karpatian/Badenian boundary at 16.303 Ma, a significant event easily recognizable in biostratigraphy, paleoclimate evolution and sequence stratigraphy, cannot be equated with the proposed global Burdigalian/Langhian, and thus Early/Middle Miocene boundary, at 15.974 Ma.

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Section: Karpatian/badenian Boundarysupporting

confidence: 70%

Section: Early Badenianmentioning

confidence: 99%

Section: Methodsmentioning

confidence: 99%

Section: Early Badenianmentioning

confidence: 99%

See 2 more Smart Citations

Timing of the Middle Miocene Badenian Stage of the Central Paratethys

Hohenegger

Ćorić

Wagreich

2014

Geologica Carpathica

132

101

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“…Chrono-biostratigraphy of the late Miocene -early Pliocene calcareous nannoplankton and inferred ages for studied sections in the Çanakkale region (Melinte-Dobrinescu et al, 2009). Chronology and calcareous nannoplankton biostratigraphy refer to Berggren et al (1995), Raffi et al (2006) and Anthonissen et al (2012). Dark and light grey strips represent the commonly accepted two steps of the MSC (Clauzon et al, 1996).…”

Section: Details) This Implies a Latest Tortonian To Early Messinianmentioning

confidence: 99%

Crustal Strain in the Marmara Pull‐Apart Region Associated With the Propagation Process of the North Anatolian Fault

et al. 2018

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Key Points:• Structural map and geological cross-section of the Ganos-Gelibolu fold system in the Dardanelles region.• Timing, amount of shortening associated to the propagation of the North Anatolian Fault deduced from mapping and critical revision of the stratigraphy.• Reconstruction of the westward propagation of the NAF in the Dardanelles region. AbstractPropagation processes of plate-scale faults through continental lithosphere are poorly documented. The North Anatolian fault (NAF) is a continental right-lateral transform with striking evidence for propagation processes in the Marmara Sea pull-apart region. Earlier work [Armijo et al., 1999] suggests that in the Dardanelles, where the principal, northern branch of that fault (NNAF) enters into the Aegean: (1) a fold-thrust system has progressively developed above the NNAF fault tip, at the WSW corner of the Marmara Sea pull-apart. The main anticline formed there was sheared and its SW half laterally offset by ~70 km to the SW; (2) the timing of structure development appears correlated with sea-level changes associated with the Messinian Salinity Crisis (MSC). Our new description of the Dardanelles (or Ganos-Gelibolu) fold-thrust system is based on structural mapping, field observations and calcareous nannoplankton analyses to date key sedimentary units. Our results provide tight constraints on the main pulse of folding associated with propagation of the tip of the NNAF: it took place in the late Miocene to earliest Pliocene (5.60 to 5.04 Ma), before deposition of undeformed Pliocene marine sediments. The folding is mostly coeval with the MSC and accommodated several kilometers of shortening at the fault tip. After full propagation of the NNAF up to the surface, the folded structure was sheared and right-laterally offset, with an average 14 mm/yr of slip-rate during the past ~5 Myrs. A reconstruction of tectonic evolution suggests a flower structure nucleating and taking root at the tip of the fault.

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Latest Cretaceous climatic and environmental change in the South Atlantic region

et al. 2017

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Latest Maastrichtian climate change caused by Deccan volcanism has been invoked as a cause of mass extinction at the Cretaceous‐Paleogene (K‐Pg) boundary (~66.0 Ma). Yet late Maastrichtian climate and ecological changes are poorly documented, in particular on the Southern Hemisphere. Here we present upper Maastrichtian‐lower Danian climate and biotic records from the Bajada del Jagüel (BJ) shelf site (Neuquén Basin, Argentina), employing the TEX86 paleothermometer, marine palynology (dinoflagellate cysts), and micropaleontology (foraminifera). These records are correlated to the astronomically tuned Ocean Drilling Program Site 1262 (Walvis Ridge). Collectively, we use these records to assess climatic and ecological effects of Deccan volcanism in the Southern Atlantic region. Both the TEX86‐based sea surface temperature (SST) record at BJ and the bulk carbonate δ18O‐based SST record of Site 1262 show a latest Maastrichtian warming of ~2.5–4°C, at 450 to 150 kyr before the K‐Pg boundary, coinciding with the a large Deccan outpouring phase. Benthic foraminiferal and dinocyst assemblage changes indicate that this warming resulted in enhanced runoff and stratification of the water column, likely resulting from more humid climate conditions in the Neuquén Basin. These climate conditions could have been caused by an expanding and strengthening thermal low over the South American continent. Biotic changes in response to late Maastrichtian environmental changes are rather limited, when compared to the major turnovers observed at many K‐Pg boundary sites worldwide. This suggests that environmental perturbations during the latest Maastrichtian warming event were less severe than those following the K‐Pg boundary impact.

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Cenozoic and Cretaceous Biochronology of Planktonic Foraminifera and Calcareous Nannofossils

Cited by 86 publications

References 53 publications

Timing of the Middle Miocene Badenian Stage of the Central Paratethys

Timing of the Middle Miocene Badenian Stage of the Central Paratethys

Crustal Strain in the Marmara Pull‐Apart Region Associated With the Propagation Process of the North Anatolian Fault

Latest Cretaceous climatic and environmental change in the South Atlantic region

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