◄ Carnets Geol. 14 (6) ►
Contents
[Introduction] [The isotope C7 segment] [Division of the segment C7 in the Prebetic
Domain, Spain]
[Intra-Furcata Negative Excursion (IFNE): Definition]
[Probable expressions of the "IFNE" in the Old World] [(...) in the New World]
[Conclusions] [Bibliographic references]
and ... [Appendix]
Posgrado en Ciencias de la Tierra, Departamento de
Paleontología, Instituto de Geología, Universidad Nacional Autónoma de
México, Ciudad Universitaria, Delegación Coyoacán, 04510 México, D.F. (Mexico)
Departamento de Paleontología, Instituto de Geología, Universidad Nacional Autónoma de
México, Ciudad Universitaria, Delegación Coyoacán, 04510 México, D.F. (Mexico)
Departamento de Estratigrafía y Paleontología, Facultad de
Ciencias, Universidad de Granada Avenida Fuentenueva s/n, 18002 Granada (Spain)
Departamento de Paleontología, Instituto de Geología, Universidad Nacional Autónoma de
México, Ciudad Universitaria, Delegación Coyoacán, 04510 México, D.F. (Mexico)
Manuscript online since May 8, 2014
[Editor:
Michel ; copy editor: Bruno ;
language editor: Phil ]
In this work we discuss a proposed updated division of the C7 isotope segment of et al. (1998). The new standard division of the segment C7 is based on a revision of published Barremian-Aptian carbon isotope curves from stratigraphic sections of the Prebetic Domain in Spain. It includes four distinct isotopic subunits labeled C7a to C7d, with a characteristic negative carbon isotope excursion at the base of the segment and which correlates with the Dufrenoyia furcata ammonite Zone. The negative excursion is recognized on a regional extent, and the term Intra-Furcata Negative Excursion (IFNE) is proposed to identify it. We provide possible sites correlatable with the IFNE in both the Old and New worlds, which suggest its potential use as an even global chemostratigraphic marker for the Aptian record.
Aptian; C7 segment; negative carbon isotope excursion; Dufrenoyia furcata Zone.
F., J.A., M. & R. (2014).- A negative carbon isotope excursion within the Dufrenoyia furcata Zone: proposal for a new episode for chemo-stratigraphic correlation in the Aptian.- Carnets de Géologie [Notebooks on Geology], Brest, vol. 14, nº 6, p. 129-137.
Une excursion négative de la courbe isotopique du carbone au sein de la Zone à Dufrenoyia furcata : proposition pour un nouvel épisode permettant la corrélation chimiostratigraphique dans l'Aptien.- Dans ce travail nous proposons une mise à jour de la subdivision du segment isotopique C7 de et al. (1998). Ce nouveau standard est fondé sur une révision des courbes isotopiques du carbone publiées pour le Barrémo-Aptien à partir de coupes stratigraphiques du domaine prébétique en Espagne. Le segment C7 inclut quatre sous-unités isotopiques distinctes répertoriées C7a à C7d et est caractérisé à sa base par une excursion isotopique négative qui est corrélée avec la Zone d'ammonites à Dufrenoyia furcata. Cette excursion négative est reconnue à l'échelon régional, et le terme Excursion Négative Intra-Furcata (ENIF) est proposé pour sa dénomination. Nous proposons d'autres sites, à la fois dans l'Ancien et le Nouveau Monde, qui paraissent révéler cette ENIF, ce qui suggère ses potentialités comme marqueur chimiostratigraphique global pour l'Aptien.
Aptien ; segment C7 ; excursion négative des isotopes du carbone ; Zone à Dufrenoyia furcata.
The carbon isotope segments of et al. (1998) describe long-term trends linked to different disturbances in the global carbon cycle during the Late Barremian-Aptian interval. They derived from high-resolution studies of carbon isotope stratigraphy from sections at the western and eastern margins of the Alpine Tethys. From C1 to C8, each segment is characterized by a distinctive pattern of variation in the inorganic (δ13Ccarb) and organic carbon (δ13Corg) isotope curve. Their recognition in several paleogeographic domains worldwide has provided evidence of their reliability as a well-established standard pattern for the carbon isotope curve and attests to their use as a valuable tool for correlations between different stratigraphic sections ( et al., 1999; et al., 2003; et al., 2005; et al., 2008; et al., 2009; et al., 2009; et al., 2010; et al., 2011; et al., 2012). Among the different isotope segments, greatest emphasis has been given to segments C3 to C6 because they characterized the most prominent shift in the C-isotope curve during the early Aptian, the Oceanic Anoxic Event 1a (OAE 1a, Selli event, ~120 Ma) ( & , 1976; , 1980, 1999; et al., 1990). So far the other segments have received less attention, but conspicuous fluctuations within their temporal pattern also have the potential to be used as chemostratigraphic markers. Characterizing in detail these minor but significant episodes allow us to improve the chemostratigraphic and chronologic resolution of the original segments ( et al., 1998).
In this paper we focus on segment C7 ( et al., 1998), and we attempt to identify particular characteristics of useful minor isotopic trends that can be recognized in different stratigraphic sections. We propose a new division of segment C7 into discrete sub-units based on similar isochronous behavior of δ13C values within this segment, as provided in different published European sections. We also provide evidence to demonstrate that the most significant sub-unit within C7 is characterized by a negative δ13C shift that we propose should be considered as a new and important element of correlation for the lower Aptian record. We also aim to motivate future research that may further reveal the minor isotopic shift discussed in this study in order to increase its known record and verify its potential as a tool for spatio-temporal correlations.
The C7 isotope segment ( et al.,
1998) the longest of all segments, corresponds to the maximum positive δ13C excursion of the
lower Aptian record, and is known as the Cismon event ( & ,
1991; et al.,
1998). Based on the planktonic foraminifera biozones used by et al.
(1998) from Cismon core reference section in Italy
(Fig. 1 
), C7 spans from the upper part of the Globigerinelloides blowi through the entire Leupoldina cabri Zone (Fig.
2.A ). However, at the same section, et al.
(1999) constrained this segment mostly to the Leupoldina cabri Zone and stated that its uppermost part falls within the Globigerinelloides ferreolensis Zone (Fig.
2.B ). Despite the overall high δ13C values that originally defined segment C7 ( et al.,
1998), the actual pattern includes minor, relatively abrupt negative to positive excursions. Numerous investigations have addressed the issue of these minor carbon isotopic variations and divided segment C7 into discrete sub-segments or zones that emphasize the value of these isotopic trends as suitable correlation patterns. In this respect, a detailed δ13Ccarb analysis in sections from the Vocontian Basin, Southeast France ( et al.,
2004) allowed the splitting of segment C7 into three units labeled Ap7, Ap8 and Ap9 at Serre Chaitieu section
(Fig. 1 ). Furthermore, since Ap7 consisted of a prominent positive δ13Ccarb excursion that included distinct lower magnitude variations, et al.
(2004) also subdivided unit Ap7 into four sub-units
(Fig. 2.D ). According to this scheme, sub-unit Ap7b is located within the uppermost part of the planktonic foraminifera L. cabri Zone and encloses the lowest δ13C values in the lower part of segment C7.
Click on thumbnail to enlarge the image.
Figure 1: Map showing location of stratigraphic sections mentioned in this contribution in a paleogeografical reconstruction at 120 Ma (, 2010; © Ron , Colorado Plateau Geosystems). 1-Cismon core section, Italy ( et al., 1998; et al., 1999); 2-Serre Chaitieu section, Vocontian Basin, France ( et al., 2004), 3- Cassis-La Bédoule section, France ( et al., 1998), 4-Prebetic Domain sections, Spain ( et al., 2012, this study); 5- Djebel Serdj section, Tunisia ( et al., 2008), 6-Igaratza section, Basque-Cantabrian Basin, Spain ( et al., 2009), 7-Santa Rosa section, Mexico ( et al., 2008), 8-Permanente Quarry section, USA ( et al., 2008), 9- Curití section, Colombia ( et al., 2013).
Subsequently, et al.
(2012) studied the Aptian δ13C signal at Ocean Drilling Program Site 765C, Leg 123, off the northwestern margin of Australia. They found differences with the scheme proposed by et al.
(1998), especially with respect to the values in the segment C7. They divided the segment C7 of site 765C into two zones which also found on a composite section with better sampling resolution and conformed with δ13Ccarb data from the Cismon core section ( et al.,
1999) and the Vocontian Basin ( et al.,
2004) (Fig.
2.C ). In this section, Zone C7a represents increasing values and correlates with the
lower Aptian highest positive δ13C excursion of et al.
(1998). This zone is equivalent to the lower and middle part of the C7 segment of
et al. (1999), which is the upper part of the C6 segment of et al.
(2004). Zone C7b of the composite section is equivalent to a period of high δ13C variation not clearly distinct in the Cismon core section, and corresponds to the uppermost part of the C7 segment of
et al. (1999) and to the unit Ap7 of et al.
(2004). The latter correlation reduced the upper extent of
's segment C7 and made it more coherent with the original age-calibration of the segments defined by et al.
(1998) (see in
Fig. 2 ). Based on the pattern of δ13C values of et al.
(2004) and ammonite biostratigraphy data analysis, et al.
(2012) even proposed that only sub-units Ap7a to Ap7c defined by et al.
(2004) correspond to segment C7.
The main issue with these proposed subdivisions for segment C7 ( et al., 2004; et al., 2012) is that they are based in each case only on the carbon isotopic record of a single section, and the sub-units cannot be clearly recognized in other stratigraphic sections; therefore, their potential as chemostratigraphic tools remains unproven and may only have a local value.
Click on thumbnail to enlarge the image.
Figure 2: The C7 isotope segment of et al. (1998) and et al. (1999) and the subsequent divisions of et al. (2004) and et al. (2012). Dashed lines are used for correlation. Scale bar in A, B and D indicates distance interval in meters (m), whereas in C represents time interval in million years (Myr).
The present study uses δ13Ccarb values within segment C7 from different published stratigraphic sections of the Prebetic
Domain in Spain, including the L'Alcoraia, Racó Ample and Cau sections ( et al.,
2012)
(Figs. 1 and
3 ). Carbon isotope determinations were carried out with reproducibility better than 0.03‰. All these sections have been calibrated by means of ammonite biostratigraphy ( et al.,
2012), and the Cau section has also been correlated with planktonic foraminifera zonation ( et al.,
2003).
Since segment C7 shows a similar pattern in all these sections, we divided it into four distinct isotopic trends labeled C7a to C7d, from bottom to top
(Fig. 3 ). While sub-unit C7a is represented by somewhat variable but overall constant values, the sub-unit C7b consists of a conspicuous negative excursion followed by a positive shift (sub-unit C7c). Finally, uniform to slightly increasing values characterize sub-unit C7d. These sub-units are identified in sections from the Prebetic Domain but are not clearly correlatable with the sub-units defined by et al.
(2004) or et al.
(2012).
All the sections shown in et al.
(2012) include the well-defined negative excursion of sub-unit C7b, which corresponds to the lowest carbon isotope data within segment C7. This negative shift has an amplitude of about 0.7‰ in the L'Alcoraia section, 1.2‰ in the Racó Ample section and close to 1‰ in the Cau section
(Fig. 3 ). This sub-unit occurs within the middle to upper part of the Leupoldina cabri Zone. A more consistent biostratigraphic position for this δ13C sub-unit is achieved if it is correlated with established Mediterranean ammonite zones. As shown in
Figure 3 , the negative inflection equivalent to subunit C7b consistently occurs in the Dufrenoyia furcata Zone. Taking into account the subzones of the Dufrenoyia furcata Zone showed in et al.
(2012) for the Cau and Racó Ample sections, it seems that the lower part of the zone is condensed and consequently
this sub-unit is located about the middle part of the zone. The fact that this negative carbon isotope excursion is defined by a single point is significant. This may be a result low sedimentation rate in an outer-ramp environment where these sections were deposited (,
1998; , 2004;et al.,
2008). Since this negative inflection is not linked to a significant lithologic change nor is it coeval with an oxygen isotope shift (see
Appendix 1), it can be considered as a primary carbon isotope signal. Diagenetic overprinting can be also excluded, given the presence of this negative carbon isotope excursion, with a similar value and biostratigraphic position, in geographically distant stratigraphic sections.
The δ13Ccarb values of segment C7 of the three sections from the Prebetic
Domain (Fig.
3 ) reveal that the negative carbon isotope excursion represented by sub-unit C7b appears in the same chemo- and bio-stratigraphic position and displays a similar drop in carbon isotope values at each location. Hence, this excursion appears to represent a constant chemostratigraphic marker with regional significance. This characteristic carbon isotope trend is here named the Intra-Furcata Negative Excursion (IFNE), which is defined as a negative carbon isotope excursion with the lowest values within segment C7, and can be correlated with the middle part of the Dufrenoyia furcata ammonite Zone (Fig. 3 ). Regarding planktonic foraminifera biozones, the IFNE can be recognized within the middle to the upper part of the Leupoldina cabri Zone. However, considering inconsistency regarding the definition of the base of this planktonic foraminifera biozone (,
1959; & ,
2004), such correlation for the IFNE is less accurate.
Click on thumbnail to enlarge the image.
Figure 3: Carbon-isotope stratigraphy of sections in the Prebetic Domain: Cau, Racó Ample and L'Alcoraia sections. Proposed sub-units for dividing the segment C7 are shown. Sections are correlated (dashed line) using the negative carbon isotope excursion represented by the sub-unit C7b (IFNE). For all sections scale bar is 10 m.
Although more studies are needed, it is likely that the IFNE appears elsewhere beyond the Prebetic
Domain (Fig.
4.A ) because a comparable negative variation also occurs in other stratigraphic sections in Old World. The Cassis-La Bédoule Stratotype section in southeast France ( et al.,
1998) is such an example, as a negative shift in the δ13Ccarb curve (~1.2‰) is recorded within the planktonic foraminifera L. cabri Zone, and is correlatable with the Dufrenoyia furcata Zone
(e.g., et al., 2006; et al.,
2012) (Fig.
4.B ). In the Vocontian
Basin, a negative carbon isotope excursion similar to IFNE has been documented by et al.
(2004) (Ap7b=~1.5‰). This correlation is very reliable because Ap7b has been related to the Niveau Blanc ( et al.,
2004), which is a significant reference level observed in most sections of the Vocontian Basin, and its upper part has been associated with the lower part of the Dufrenoyia furcata Zone (,
2005). This biochronologic correlation is also in agreement with the reconstructed carbon isotope segments of et al.
(1998) in the Vocontian Basin, as shown in Figure IX of et al.
(2012) (Fig.
4.C ). Another comparable negative carbon isotope shift that may be equivalent to the IFNE is reported in the Aptian outcrops of the Djebel Serdj area, north-central Tunisia ( et al.,
2008). It consists of a δ13Ccarb negative variation of ~2.5‰ within the L. cabri Zone (Fig.
4.D ).
In the Basque-Cantabrian Basin (Spain), at Igaratza section, et al.
(2009) documented a pronounced negative δ13Ccarb spike predating the Aparein level and within the Dufrenoyia furcata Zone. Since according to et al.
(2009) this negative carbon isotope excursion overlies the segment C8 and records a variation of about ~4.1‰, we consider that this does not correspond to the IFNE. Instead, it is more likely that the carbon isotope drop of ~1‰ to the middle part of the segment C7 correlates with the IFNE (Fig.
4.E ). A firm correlation is not possible due to the fact that this drop is included in the Deshayesites deshayesi - Dufrenoyia furcata transition Zone. All mentioned sections in this
chapter are located in
Figure 1 .
Click on thumbnail to enlarge the image.
Figure 4: Different stratigraphic sections in the Old World which exhibit a negative carbon isotope excursion similar to the IFNE. Cau section of the Prebetic Domain is shown for comparison. Dashed line correlates the stratigraphic sections using IFNE as a characteristic chemostratigraphic marker. Ammonite biozones plotted for the Cassis-La Bédoule ( et al., 1998) and the Serre Chaitieu (Vocontian Basin) sections ( et al., 2004) correspond to the interpretation of et al. (2012). Planktonic foraminifera zones of the Djebel Serdj section are also depicted ( et al., 2008). The segment C7 of the Vocontian Basin is also in agreement with et al. (2012). The Igaratza section [reference section of the Aparein level of et al. (2009)] is shown for comparison with the IFNE.
A cursory review of the literature reveals that fewer published data are available for the New World regarding the Aptian interval; however, carbon isotope data from some sites show isotopic trends that could correspond to the IFNE. The δ13Corg curve of the Santa Rosa section in northeastern Mexico displays a negative carbon isotope excursion of ~2.0‰ toward the base of segment C7 in the La Peña Formation, within the L. cabri planktonic foraminifera Zone ( et al.,
2008). Since ammonite data are not available for the Santa Rosa section, we cannot determine whether or not this carbon isotopic drop is related to the Mexican ammonite zone equivalent to the European Dufrenoyia furcata Zone. In the USA, a decrease of 0.4‰ in carbon isotope composition of organic matter is reported at the base of the segment C7 of the La Calera limestone exposed at the Permanente Quarry in California ( et al.,
2008). A lack of biostratigraphic data along with the carbon isotope data prevents us from further constraining the age of this negative excursion. In Colombia, the δ13Corg curve of the Curití section shows a pronounced negative inflection in the lowermost part of the segment C7 that reaches ~2.0‰ ( et al.,
2013) and is also compatible with the IFNE. All mentioned sections in this
chapter are located in
Figure 1 .
A review of the δ13Ccarb curve in three different stratigraphic sections of the Prebetic Domain in Spain reveals a consistent pattern that allows us to propose a quadripartite division of the segment C7 of et al. (1998). We divided segment C7 into distinct isotopic trends labeled, from bottom to top, C7a, C7b, C7c and C7d. The most conspicuous of these subdivisions corresponds to sub-unit 7b and consists of a negative carbon isotope excursion, with the lowest values within the lower middle part of segment C7. Since its record is chronologically linked to the Dufrenoyia furcata Zone, this isotope trend is here named the Intra-Furcata Negative Excursion (IFNE).
The chemostratigraphic record of the IFNE does not seem to be limited to the Prebetic Domain in Spain. We provide several plausible sites in both the Old and New worlds where a comparable negative carbon isotope excursion may be equivalent to the IFNE. Although additional research is needed, we wish to highlight the possible use of the IFNE as a new chemostratigraphic marker that has the potential to provide a more robust chronologic framework for the lower Aptian record.
The authors are grateful to Drs Karl , Florentin and Peter for the careful review and the helpful comments and suggestions that significantly improved the original manuscript. Special thanks also are due to Michel and Bruno for their constructive editing. We are very grateful to the Language Editor, Phil , for his corrections which allowed significant improvements to the manuscript.
M.A., H.J., H.C. & S.O. (1990).- Stratigraphy, geochemistry and paleoceanography of organic carbon-rich Cretaceous sequences. In: R.N. & B. (eds.), Cretaceous resources, events and rhythms-background and plans for research.- Kluwer Academic Publications, Dordrecht, p. 75-119.
R.C. (2010).- Paleogeographic maps.- Colorado Plateau Geosystems, Phoenix, AZ. URL: http://cpgeosystems.com/
T., J.A., R., P.W., K. & E. (2010).- Sedimentary evolution of an Aptian syn-rift carbonate system (Maestrat Basin, E Spain): effects of accommodation and environmental change.- Geologica Acta, Barcelona, vol. 8, p. 249-280.
H.B. (1959).- Planktonic foraminifera from the Cretaceous of Trinidad, B.W.I.- Bulletin of American Paleontology, New York, vol. 39, 257-277.
T.J., E., B., W.V., C.L. & J. (1999).- The record of global change in mid-Cretaceous (Barremian-Albian) sections from the Sierra Madre, northeastern Mexico.- Journal of Foraminiferal Research, Washington, vol. 29, nº 4, p. 418-308.
J.M. (1998).- Las plataformas del Valanginiense superior-Albiense superior en el Prebético de Alicante.- Ph.D. thesis, Universidad de Granada, 464 p.
J.M., G.A. de, P.A. & J.M. (2008).- Development of carbonate platforms on an extensional (rifted) margin: the Valanginian-Albian record of the Prebetic of Alicante (SE Spain).- Cretaceous Research, London, vol. 29, p. 848-860.
N., R.L., A. & U.G. (2012).- Early Aptian carbon and sulphur isotope signatures at ODP Site 765.- Isotopes in Environmental and Health Studies, Leipzig-Halle, vol. 48, nº 1, p. 180-194.
Y. (2005).- Biostratigraphie, évolution et renouvellements des ammonites de l'Aptien supérieur (Gargasien) du bassin vocontien (Sud-Est de la France).- Ph.D. thesis, Université Claude Bernard, Lyon, 302 p.
E., J.E.T., M., C., R., B., I., A., G. & S. (1999).- Integrated stratigraphy of the Cismon Apticore (southern Alps, Italy); a "reference section" for the Barremian-Aptian interval at low latitudes.- The Journal of Foraminiferal Research, Lawrence, vol. 29, nº 4, p. 371-391.
T., F.J-M.R. & F. (2013).- Geochemistry, palaeoenvironments and timing of Aptian organic-rich beds of the Paja Formation (Curití, Eastern Cordillera, Colombia). In: A.-V., M.C. & J. (eds.), Isotopic studies in Cretaceous research.- Geological Society, London, Special Publication, vol. 382, p. 31-48.
J., H.J., N., M.I. & P.A. (2009).- The early Aptian of Aralar (northern Spain): stratigraphy, sedimentology, ammonite biozonation, and OAE1.- Cretaceous Research, London, vol. 30, nº 2, p. 434-464.
G.A. de (2004).- Bioestratigrafía y eventos del Cretácico Inferior en las Zonas Externas de la Cordillera Bética.- Universidad de Jaén, 658 p.
G.A. de, J.M., o R., P.A. & M. (2003).- Lower Aptian carbon isotope stratigraphy from a distal carbonate shelf setting: the Cau section, Prebetic zone, SE Spain.- Palæogeography, Palæoclimatology, Palæoecology, Amsterdam, vol. 200, p. 207-219.
M., M. & J. (2008).- Microfacies, biostratigraphy, and geochemistry of the hemipelagic Barremian-Aptian in north-central Tunisia: Influence of the OAE 1a on the southern Tethys margin.- Palæogeography, Palæoclimatology, Palæoecology, Amsterdam, vol. 261, p. 246-260.
J.O., P., O., H. & C. (2004).- High-resolution carbon isotope records of the Aptian to lower Albian from SE France and the Mazagan Plateau (DSDP Site 545): a stratigraphic tool for paleoceanographic and paleobiologic reconstruction.- Earth and Planetary Science Letters, Amsterdam, vol. 218, p. 149-161.
H.C. (1980).- Cretaceous anoxic events: From continents to oceans.- Journal of the Geological Society, London, vol. 137, nº 2, p. 171-188.
H.C. (1999).- Mesozoic anoxic events and palaeoclimate.- Zentralblatt für Geologie und Paläontologie, Stuttgart, Teil 1 (1997), Heft 7-9, p. 943-949.
Y.-X., T.J., I.P., D.A., M.A., D.M., T.D., E. & I. (2008).- Toward an orbital chronology for the early Aptian Oceanic Anoxic Event (OAE1a, ~120 Ma).- Earth and Planetary Science Letters, Amsterdam, vol. 271, p. 88-100.
S., C.E., S.M., H., E., C. & P.A. (2009).- A volcanic CO2 pulse triggered the Cretaceous Oceanic Anoxic Event 1a and a biocalcification crisis.- Geology, Boulder, vol. 37, p. 819-822.
A.P., H., R.S., R.V., P., A. & M. (1998).- High-resolution δ13C stratigraphy through the early Aptian "Livello Selli" of the Alpine Tethys.- Paleoceanography, Washington, vol. 13, nº 5, p. 530-545.
M.I., H.J., P.A. & J. (2009).- Impact of early Aptian carbon cycle perturbations on evolution of a marine shelf system in the Basque-Cantabrian Basin (Aralar, N Spain).- Earth and Planetary Science Letters, Amsterdam, vol. 287, p. 392-401.
J.A., M., J., J.M., T., R., G., F.J.-M.R. & R. (2012).- Lower Aptian ammonite and carbon isotope stratigraphy in the eastern Prebetic domain (Betic Cordillera, southeastern Spain).- Geologica Acta, Barcelona, vol. 10, nº 4, p. 333-350.
M., W., J.A., J.-P. & G. (1998).- Correlation of biostratigraphic and stable isotope events in the Aptian historical stratotype of La Bédoule (southeast France).- Comptes Rendus de l'Académie des Sciences, Paris, (Série IIa, Sciences de la Terre et des Planètes), nº 327, p. 693-698.
M., I., J.A., G.A. de, E., M. & G. (2011).- High-resolution chemo- and biostratigraphic records of the early Aptian oceanic anoxic event in Cantabria (N Spain): Palaeoceanographic and palaeoclimatic implications.- Palæogeography, Palæoclimatology, Palæoecology, Amsterdam, vol. 299, p. 137-158.
I. & D. (2004).- Practical manual of Cretaceous planktonic foraminifera.- International School on Planktonic Foraminifera, Course: Cretaceous, Perugia, 283 p.
M., M. de, L., M., J.-P., W., J.A. & G. (2005).- Early Aptian δ13C and manganese anomalies from the historical Cassis-La Bédoule stratotype sections (S.E. France): relationship with a methane hydrate dissociation event and stratigraphic implications.- Carnets de Géologie [Notebooks on Geology], Brest, Article 2005/04 (CG2005_A04), 18 p.
S.A., L.J., A. & I.G. (2008).- Mid-Cretaceous oceanic anoxic events in the Pacific Ocean revealed by carbon-isotope stratigraphy of the Calera Limestone.- Geological Society of America, Bulletin, Tulsa, vol. 120, nº 11-12, p. 1416-1426.
P., M., R., G. & G. (2006).- The Deshayesitidae , 1949 (Ammonoidea) of the Aptian historical stratotype region at Cassis-La Bédoule (SE France).- Carnets de Géologie [Notebooks on Geology], Brest, Memoir 2006/01 (CG2006_M01), 46 p. (14 Pls.).
S.O. & H.C. (1976).- Cretaceous oceanic anoxic events: causes and consequences.- Geologie en Mijnbouw, Utrecht, vol. 55, p. 179-184.
H. & A. (1991).- Ice Age interludes during the time of Cretaceous greenhouse climate? In: D.W., J.A. & H. (eds.), Controversies in modern geology: Evolution of geologic theories in sedimentology, earth history and tectonics.- Academic Press, London, p. 173-191.
H., A. & K.B. & O. (1998).- Correlation of Early Cretaceous carbon isotope stratigraphy and platform drowning events: A possible link?- Palæogeography, Palæoclimatology, Palæoecology, Amsterdam, vol. 137, p. 189-203.
| Cau section | Raco Ample section | L'Alcoraia section | ||||||||
| Sample | δ13Ccarb (‰PDB) |
δ18Ocarb (‰PDB) |
Sample | δ13Ccarb (‰PDB) |
δ18Ocarb (‰PDB) |
Sample | δ13Ccarb (‰PDB) |
δ18Ocarb (‰PDB) |
||
| 54 | 3.10 | -1.78 | 46 | 2.63 | -2.29 | 212 | 3.01 | -1.50 | ||
| 53 | 3.05 | -2.16 | 45 | 2.66 | -2.14 | 210 | 2.99 | -2.03 | ||
| 51 | 3.41 | -2.07 | 44 | 2.78 | -2.35 | 209 | 2.92 | -1.77 | ||
| 50 | 3.70 | -1.67 | 43 | 2.64 | -1.99 | 208 | 3.38 | -2.24 | ||
| 49 | 3.57 | -1.92 | 42 | 2.46 | -2.06 | 207 | 2.98 | -1.74 | ||
| 48 | 3.55 | -2.04 | 41 | 3.82 | -2.32 | 206 | 3.08 | -1.55 | ||
| 47 | 3.61 | -2.15 | 40 | 2.70 | -2.50 | 205 | 3.01 | -1.65 | ||
| 46b | 3.88 | -1.66 | 39 | 3.17 | -2.27 | 204 | 3.68 | -1.10 | ||
| 46a | 3.58 | -1.72 | 38 | 3.13 | -2.02 | 203 | 3.38 | -1.52 | ||
| 46 | 3.78 | -2.02 | 37 | 3.47 | -2.32 | 202 | 3.17 | -1.69 | ||
| 44* | 3.04 | -1.97 | 36 | 3.43 | -2.45 | 201 | 3.74 | -1.44 | ||
| 43 | 4.04 | -1.67 | 35 | 3.39 | -2.52 | 200 | 3.78 | -1.47 | ||
| 42 | 3.54 | -2.52 | 34 | 3.24 | -2.41 | 199 | 3.30 | -2.12 | ||
| 41 | 4.07 | -1.22 | 33 | 3.57 | -2.46 | 198 | 3.85 | -1.29 | ||
| 39 | 3.88 | -2.02 | 32 | 3.100 | -2.36 | 197 | 3.76 | -1.92 | ||
| 38 | 3.78 | -2.08 | 31 | 3.96 | -2.35 | 196 | 4.23 | -1.42 | ||
| 37 | 3.96 | -1.95 | 30 | 4.03 | -2.27 | 195 | 3.76 | -1.92 | ||
| 35 | 4.04 | -1.49 | 29 | 3.81 | -2.47 | 194 | 4.36 | -1.41 | ||
| 33 | 3.71 | -2.09 | 28 | 3.97 | -2.25 | 193 | 4.44 | -1.57 | ||
| 32 | 3.77 | -1.96 | 27 | 3.44 | -2.61 | 191 | 4.13 | -2.07 | ||
| 31 | 3.84 | -1.96 | 26 | 3.74 | -2.56 | 190 | 4.02 | -2.34 | ||
| 30 | 3.99 | -1.85 | 24 | 3.93 | -2.41 | 189 | 4.43 | -1.85 | ||
| 29a | 3.100 | -2.01 | 23 | 4.02 | -2.39 | 188 | 4.36 | -1.65 | ||
| 29 | 3.59 | -1.97 | 22 | 3.64 | -2.46 | 187 | 4.11 | -1.75 | ||
| 28 | 3.69 | -1.69 | 21 | 3.93 | -2.08 | 186 | 3.71 | -2.50 | ||
| 27 | 3.52 | -1.85 | 20 | 3.89 | -2.25 | 185 | 4.08 | -2.06 | ||
| 26 | 3.61 | -1.92 | 19a* | 2.82 | -2.76 | 184 | 3.77 | -2.31 | ||
| 25 | 2.97 | -1.98 | 19 | 4.00 | -2.06 | 183 | 3.97 | -2.32 | ||
| 23 | 2.48 | -2.05 | 18 | 3.96 | -2.24 | 182* | 3.07 | -1.44 | ||
| 16 | 4.00 | -2.43 | 181 | 3.84 | -2.09 | |||||
| Reproducibility | ± 0.03 | ±0.03 | 15 | 3.83 | -2.56 | |||||
| 14 | 3.75 | -2.32 | Reproducibility | ± 0.01 | ± 0.06 | |||||
| *IFNE | 13 | 2.91 | -2.73 | |||||||
| 11a | 3.10 | -2.27 | ||||||||
| 11 | 2.62 | -2.25 | ||||||||
| Reproducibility | ± 0.02 | ± 0.05 | ||||||||