Chapter A5 Langhian, serravallian, and tortonian historical stratotypes

Rio, Domenico; Cita, M.B.; Iaccarino, S.; Gelati, R.; Gnaccolini, Mario

doi:10.1016/s0920-5446(06)80009-9

Cited by 21 publications

(30 citation statements)

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“…We further arrived at an age of 11.8 Ma for the top of the Serravallian stratotype in the Serravalle Scrivia section by linear extrapolation of the sedimentation rate between the Sphenolithus heteromorphus LO (13.5 Ma, Rio et al, 1997) and the Calcidiscus premacintyrei (12.3 Ma, Rio et al, 1997). This admittedly rough age estimate indicates that there is gap between the top of the Serravallian stratotype and the base of the Tortonian stratotype as previously suggested by Rio et al (1997) among others.…”

Section: Serravallian=tortonian Boundarysupporting

confidence: 66%

“…This admittedly rough age estimate indicates that there is gap between the top of the Serravallian stratotype and the base of the Tortonian stratotype as previously suggested by Rio et al (1997) among others. These observations potentially render all bio-events in the interval between 11.8 and 10.554 Ma suitable for delimiting the S=T boundary.…”

Section: Serravallian=tortonian Boundarysupporting

confidence: 54%

“…The Serravallian=Tortonian (S=T) boundary is not yet formally defined but is commonly placed at or close to the N. acostaensis FO because this bio-event has previously been reportedas the first evolutionary appearance -from the basal part of the Tortonian historical stratotype section of Rio Mazzapiedi-Castellania (Cita and Premoli Silva, 1968), which is assigned to nannofossil zone NN9 on the basis of the presence of the zonal marker D. hamatus (Mazzei, 1977). These zonal assignments are conflicting, however, with the common practice to place the N15=N16 boundary at or close to the base of NN8 (see Rio et al, 1997), while our data from Gibliscemi even indicate that the N. acostaensis FO actually falls within zone NN7 in the Mediterranean as previously suggested by Foresi et al (1998). This indicates that the so-called N. acostaensis FO at Rio Mazzapiedi-Castellania does not represent the true first occurrence of this species, as recently confirmed by the presence of rare N. acostaensis in the top part of the Serravalle Sandstones immediately below the base of the Tortonian stratotype (Miculan, 1997;Foresi et al, 1998).…”

Section: Serravallian=tortonian Boundarycontrasting

confidence: 52%

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Integrated stratigraphy and astronomical calibration of the Serravallian/Tortonian boundary section at Monte Gibliscemi (Sicily, Italy)

Hilgen

Krijgsman²,

Raffi

et al. 2000

Marine Micropaleontology

118

148

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Results are presented of an integrated stratigraphic (calcareous plankton biostratigraphy, cyclostratigraphy and magnetostratigraphy) study of the Serravallian=Tortonian (S=T) boundary section of Monte Gibliscemi (Sicily, Italy). Astronomical calibration of the sedimentary cycles provides absolute ages for calcareous plankton bio-events in the interval between 9.8 and 12.1 Ma. The first occurrence (FO) of Neogloboquadrina acostaensis, usually taken to delimit the S=T boundary, is dated astronomically at 11.781 Ma, pre-dating the migratory arrival of the species at low latitudes in the Atlantic by almost 2 million years. In contrast to delayed low-latitude arrival of N. acostaensis, Paragloborotalia mayeri shows a delayed low-latitude extinction of slightly more than 0.7 million years with respect to the Mediterranean (last occurrence (LO) at 10.49 Ma at Ceara Rise; LO at 11.205 Ma in the Mediterranean). The Discoaster hamatus FO, dated at 10.150 Ma, is clearly delayed with respect to the open ocean. The ages of D. kugleri first and last common occurrence (FCO and LCO), Catinaster coalitus FO, Coccolithus miopelagicus last (regular) occurrence (L(R)O) and the D. hamatus=neohamatus cross-over, however, are in good to excellent agreement with astronomically tuned ages for the same events at Ceara Rise (tropical Atlantic), suggesting that both independently established timescales are consistent with one another. The lack of a reliable magnetostratigraphy hampers a direct comparison with the geomagnetic polarity timescale of Cande and Kent (1995; CK95), but ages of calcareous nannofossil events suggests that CK95 is significantly younger over the studied time interval. Approximate astronomical ages for the polarity reversals were obtained by exporting astronomical ages of selected nannofossil events from Ceara Rise (and the Mediterranean) to eastern equatorial Pacific ODP Leg 138 Site 845, which has a reliable magnetostratigraphy.Our data from the Rio Mazzapiedi-Castellania section reveal that the base of the Tortonian stratotype corresponds almost exactly with the first regular occurrence (FRO) of N. acostaensis s.s. as defined in the present study, dated at 10.554 Ma. An extrapolated age of 11.8 Ma calculated for the top of the Serravallian stratotype indicates that there is a gap between the top of the Serravallian and the base of the Tortonian stratotype, potentially rendering all bio-events in the interval between 11.8 and 10.554 Ma suitable for delimiting the S=T boundary. Despite the tectonic deformation and the lack of a magnetostratigraphy, Gibliscemi remains a candidate to define the S=T boundary by means of the Tortonian global boundary stratotype section and point (GSSP). © 2000 Elsevier Science B.V. All rights reserved.Ł Corresponding author. E-mail: fhilgen@geo.uu.nl 0377-8398/00/$ -see front matter © 2000 Elsevier Science B.V. All rights reserved. PII: S 0 3 7 7 -8 3 9 8 ( 0 0 ) 0 0 0 0 8 -6 182 F.J. Hilgen et al. / Marine Micropaleontology 38 (2000)

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Section: Serravallian=tortonian Boundarysupporting

confidence: 66%

Section: Serravallian=tortonian Boundarysupporting

confidence: 54%

Section: Serravallian=tortonian Boundarycontrasting

confidence: 52%

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Integrated stratigraphy and astronomical calibration of the Serravallian/Tortonian boundary section at Monte Gibliscemi (Sicily, Italy)

Hilgen

Krijgsman²,

Raffi

et al. 2000

Marine Micropaleontology

118

148

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“…This proposal was put forward because the onset of the extremely rare, but highly variable index fossil Praeorbulina sicana (Jenkins et al 1981;Rio et al 1997) is blurred in almost all sections to be considered for the Langhian GSSP ). Although the top of polarity Chron C5Cn.1n is a distinct boundary in magnetostratigraphy, its calibration by biostratigraphic markers is problematic if the Globigerinoides-Praeorbulina lineage is not taken into consideration.…”

Section: Karpatian/badenian Boundarymentioning

confidence: 99%

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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“…Taxonomy, additional useful bioevents and their paleomagnetic position and biochronological calibration are based on Theodoridis (1984), Perch-Nielsen (1985), Martini & Müller (1986), Driever (1988), Flores et al (1992), Young et al (1994), Berggren et al (1995), Schackleton at al. (1995), Sprovieri et al (1996), Rio et al (1997), Negri & Villa (2000), Van Couvering et al (2000), Lourens et al (2004), Raffi et al (2003Raffi et al ( , 2006 and Morigi et al (2007).…”

Section: Studied Materials -Methodsmentioning

confidence: 99%