<figure><img src="image_38.png" /><figcaption>**Figure 37.** Carbon isotopic correlation of the Cañada Luenga section with other marine successions such as Berrias (France; section after Grabowski et al., 2016, 2021; on the right part, magnetic zonation after Wimbledon et al., 2024, see Fig. 38), Capriolo, Polaveno (Italy; sections after Channell et al., 1993 and Bersezio et al., 2002, respectively), Kryta Valley (Poland; section after Grabowski et al., 2024), Barlya (Bulgaria; section after Grabowski et al., 2021), Hárskút (Hungary; section after Lodowski et al., 2022), and Atlantic Ocean (DSDP Hole 534A after Bornemann and Mutterlose, 2008), calibrated by bio-magnetostratigraphy. The base of Chron M15r is used as the datum plane for correlation. Carbon isotopic correlation with other sections, including Vergol, is shown in Fig. 36.</figcaption></figure>

Concerning the Boreal Realm, the Speeton section is characterized by carbon-isotope stratigraphy (McArthur et al., 2004). However, just two samples are available for the top part of the Berriasian stage, and the Berriasian–Valanginian interval is condensed or some strata are missing within the late Valanginian sequence. Mutterlose et al. (2014) compared these Boreal results with Tethyan data; the $\delta^{13}\text{C}$ values of the Boreal belemnites show the same long-term trend as the Tethyan

ones, but they are in general by 1–2‰ more positive than the Tethyan data. Pauly et al. (2013) published the first carbon-isotope record ($\delta^{13}\text{C}_{\text{carb}}$ and $\delta^{13}\text{C}_{\text{org}}$) for the upper Ryazanian–Barremian interval of NE Greenland (Rødryggen and Kuhn Ø sections). They noted that $\delta^{13}\text{C}_{\text{carb}}$ values observed in their study are on average much lighter than contemporaneous values presented for the Tethyan bulk-rock carbonate (Weissert and Erba 2004) and belemnite guards (McArthur et al.,
2007). The minor negative shifts “b” and “h” are indicated with doubt on the Kuhn Ø section (Fig. 36).

## Strontium isotope stratigraphy (SIS)

For Early Cretaceous time, the construction of ⁸⁷Sr/⁸⁶Sr trends (Figs. 22, 32, 33) is largely based on data coming from SE France and SE Spain, including the Vergol and Cañada Luenga sections, respectively (McArthur et al., 2007, 2020; Bodin et al., 2009, 2015; McArthur and Howarth, 2025).

Mutterlose et al. (2014) used SIS to resolve some of the difficulties of correlation between the Tethyan and Boreal realms in the Valanginian–Barremian interval. Their data were from Speeton (McArthur et al., 2004) and the Vocontian basin (McArthur et al., 2007; Bodin et al., 2009). According to Mutterlose et al. (2014; their fig. 3), the profile through the Boreal and the Tethyan realms show a good match. Nevertheless, these authors stated that “the overlap of the two Sr-isotope curves highlights discrepancies between the Boreal and the Tethyan zonation schemes for the Valanginian/Hauterivian boundary and the lower/upper Barremian boundary”. Whether “discrepancies” is the appropriate term is moot: there seems to us to be no reason why Tethyan and Boreal zonal boundaries should coincide. Mutterlose et al. (2014) therefore both aided Tethyan–Boreal correlation and also highlighted minor zonal mismatches in existing correlations of that time. It is emphasised here that their fig. 3 represents, in our view, a preliminary correlation of Tethyan and Boreal Realms and a correlation by SIS that can be substantially improved by further analysis of belemnites and brachiopods (which are readily available from multiple sites) to modern standards (to ≤ ± 0.000004 in ⁸⁷Sr/⁸⁶Sr) at a greater sample density. This example therefore is for illustrative purposes only.

Möller et al. (2015, fig. 2) provided ⁸⁷Sr/⁸⁶Sr-data for the upper Ryazanian and the Valanginian through the Rødryggen section (Wollaston Forland, NE Greenland). Data are for belemnite specimens. These authors noted a good match between the values of ⁸⁷Sr/⁸⁶Sr in Greenland and those from France, Spain and England (McArthur et al., 2004, 2007; Bodin et al., 2009). Of most importance, however, is that regression analysis of the ⁸⁷Sr/⁸⁶Sr data of Möller et al. (2015) predicts a value of 0.707293 ± 0.000003 (2.se, *n* = 14) for the Ryazanian/ Valanginian boundary based on the ammonite zonal scheme of NE Greenland. This value is within uncertainty of the value of 0.707289 ± 0.000004 (2.se, *n* = 12) for the GSSP at Vergol. Further analysis could be made to test this point as material for analysis is not in short supply. Note that all samples of Möller et al. (2015) were > 0.15 m from the R/V boundary and that the boundary value was obtained by interpolation. These authors discussed the position of the Ryazanian/ Valanginian boundary according to their data (cf. discrepancy of the ammonite and Sr-isotope based ages on one hand and the nannofossil findings on the other).

## Magnetic stratigraphy

In the Cañada Luenga section, the base of the magnetic polarity Chron M14r occurs in the upper part of the *H. otopeta* Subzone, top part of the *P. murgeanui* calpionellid Subzone (Ogg et al., 1988; Aguado et al., 2000). Since then, in terms of magnetostratigraphy, the base of the Valanginian stage is consistently assigned to the lower part of Chron

M14r (see the Geologic Time Scale, Ogg et al., 2012, 2016; Gale et al., 2020). The magnetic scale of the Cañada Luenga section can be drawn on the Vergol section according to a precise correlation based on an integrated calibration (see above; bio-chemio-cyclo-stratigraphy, Fig. 33; method of graphic correlations, Fig. 34). In terms of global correlations, this couple of sections will be correlated with (a) the Berrias section (SE France); (b) a set of sections along a European West–East transect; (c) sections and/or boreholes located in South America, Africa and Atlantic Ocean; and (d) two sections located in England and Colombia to establish correlations with continental successions.

Vergol-Cañada Luenga versus Berrias: At Berrias, the magneto-stratigraphy was performed by Galbrun (1984, 1985; see also Galbrun and Rasplus, 1984, and Galbrun et al., 1986). According to Galbrun (1985, p. 134), “a correlation between BER.SZ.N.1 and Chron M15n seems improbable because of the short thickness of this polarity sub-zone”. Ogg et al. (1988) did not correlate them either. However, subsequent authors such as Jan du Chêne et al. (1993), and Blanc (1996) interpreted this small interval of normal polarity (layer 193/65 in Galbrun et al., 1986) as Chron M15n, and Grabowski et al. (2016, 2021b) followed that interpretation (Fig. 38). It should be noted that Galbrun (1985) included the top part of the section (beds 191 to 198) in his interval BER.Z.R.1 (see his fig. 5) that is correlated with Chron M15r. But it seems that he correlated the top of the BER.SZ.N.1 with the top of Chron M15n in his fig. 6 (see the dashed line). This could explain this interpretation made by some authors.

However, the presence and position of M15n in the Berrias section is difficult to accept from the point of view of ammonite and calpionellid stratigraphy in the Cañada Luenga section. According to Jan du Chêne et al. (1993), the base of their Chron M14r is reported in the upper part of the “Callisto Subzone” and so below the “Otopeta Sub-zone”. For Blanc (1996, fig. 60), the base of this magnetic event (M14r) occurs in the “Otopeta Subzone” as the author lowered its base to nearly match with the base of Chron M15r. This is not in agreement with the current magneto-bio-stratigraphic calibration (see data on the Cañada Luenga section). Some discrepancies in the correlations based on the calpionellid zonation are also noted (Fig. 38). Indeed, at Cañada Luenga, the base of Chron M14r is recorded in the top part of the *P. murgeanui* Subzone. However, at Berrias, this magnetic event is stratigraphically lower, in a transitional interval covering the d3i and d3s calpionellid subzones, and the d3t subzone (= *P. murgeanui* Sub-zone) is not recorded (Blanc, 1996, figs. 56 and 60). This is further evidence that the interpretations of (the base of) M14r proposed by Jan du Chêne et al. (1993) and Blanc (1996) might be wrong. These issues might be partly due to the bad outcrop conditions for the top part of the section (cf. alluvial deposits of the river partly covering beds) that could be characterized by some condensed intervals and even stratigraphic gaps.

Recently, the magnetostratigraphy of the Berrias section was revised and calibrated with the biostratigraphy (Wimbledon et al., 2024). According to these authors, the top part of the section (including the layer 193) is characterized by Chron M15r and dated from the *C. oblonga* Subzone (Fig. 38). They did not recognize M15n and M14r. Therefore, the base of M15r was chosen as datum plane for the correlations of sections.

Vergol-Cañada Luenga versus a European W–E transect (France, Italy, Austria, Hungary, Poland, Bulgaria, Ukraine): Ogg et al.
<figure><img src="image_39.png" /><figcaption>**Figure 38.** Magnetostratigraphic correlation of the Vergol-Cañada Luenga sections with the Berrias section: A, section after Galbrun (1984, 1985), Galbrun and Rasplus (1984), Galbrun et al. (1986); B, section after Jan du Chène et al. (1993); C, section after Blanc (1996); D, section after Grabowski et al. (2016, 2021b); E, section after Wimbledon et al. (2024). The base of Chron M15r is used as datum plane for correlation. Magnetostratigraphic correlation with other sections is continued in Fig. 39.</figcaption></figure>

(1988) proposed a correlation of the Berrias section with others from Spain (Cehegín), central (Bosso) and northern (Capriolo and Xausa)

Italy (Fig. 39). For the Italian sections, the base of Chron M14r is recorded in the upper part of the *Calpionellopsis* Zone (Zone D, i.e.
<figure><img src="image_40.png" /></figure>

Figure 39. Magnetostratigraphic correlation of the Vergol-Cañada Luenga sections with other marine successions from France (Berrias section after Ogg et al., 1988), Italy (Xausa, Capriolo and Bosso sections after Ogg et al., 1988; Polaveno section after Bornemann and Mutterlose, 2008), Hungary (Hárskút section after Lodowski et al., 2022), Poland (Rówienka section after Grabowski et al., 2019; Kryta Valley after Grabowski et al., 2024), Bulgaria (Barlya section after Grabowski et al., 2021), and Ukraine (Crimea, Zavodskaya Balka composite after Arkadiev et al., 2017). The base of Chron M15r is used as the datum plane for correlation. Magnetostratigraphic correlation with other sections is continued in Fig. 40.

*H. otopeta* Subzone) as observed at Cañada Luenga. The issue about the interpretation of M14r at Berrias clearly appears on this figure. It can be also noted in their work that the base of M15r occurs in the middle part of the Calpionellid D2 Subzone, while for Jan du Chêne et

al. (1993) this magnetic event matches with the basal part of D3 Subzone. Channell et al. (1993) also provided an integrated study (magnetostratigraphic scale and carbon isotopic curve calibrated by a calcareous nannofossil zonation) on some Italian sections such as Capri-
Continental successions

olo (Fig. 39), Pusiano and Polaveno (see also Bornemann and Mutterlose, 2008; Fig. 39). Chron M14r is recorded in the central northern Calcareous Alps (Austria), however without detailed data (Krische et al., 2018). In agreement with data of the Cañada Luenga section (Aguado et al., 2000), the base of M14r is recorded in the top part of the *Calpionellopsis* Zone, *P. murgeanui* Subzone, of the Hárskút (Hun-

gary, Lodowski et al., 2022; see also Fözy et al., 2010), Rówienka (Poland, Grabowski et al., 2019a) and Barlya (Bulgaria, Grabowski et al., 2016, 2021b; see also Lakova et al., 1999; Petrova et al., 2011) sections (Fig. 39). In the Kryta Valley section (Poland, Grabowski et al., 2024), the *P. murgeanui* Subzone is not recognized but the base of M14r is also recorded in the top part of the *Calpionellopsis* Zone. For

<figure><img src="image_41.png" /></figure>

**Figure 40.** Magnetostratigraphic correlation of the Cañada Luenga section with other marine successions from Argentina (Puerta Curaco section after Kohan Martinez et al., 2017, including calpionellid-ammonite zonal schemes reported here from Kietzmann et al., 2021) and Namibia (Paraná–Etendeka composite section after Dodd et al., 2015); two continental successions located in England (Dorset composite section after Ogg et al., 1994) and Colombia (Cuchilla del Ramo section after Jiménez et al., 2021) are included. The base of Chron M15r is used as the datum plane for correlation. Magnetostratigraphic correlation with other sections is shown in Figs. 38 and 39.
the four sites, a calibration with nannofossil and/or ammonite zonas-
tions and/or a carbon isotopic curve is provided. For Ukraine (Crimea),
Arkadiev et al. (2017, 2018) proposed a magnetic scale alongside the
Zavodskaya Balka composite section in which the base of Chron
M14r is dated from the top part of the Berriasian (Fig. 39).

**Vergol-Cañada Luenga versus South America, Africa and Atlantic Ocean:** In their cyclostratigraphic study performed on sequences of the Neuquén basin (Argentina), Kietzmann et al. (2015) interpreted that the top part of the Arroyo Loncoche section could correspond to the Chron M14r that is correlated with the base of the *Neocomites wichmanni* Zone (cf. Andean ammonite zonation). However, according to them, the succession above the M15n is an interval with no magnetic data. In the same basin, Kohan Martínez et al. (2017) studied the Puerta Curaco section characterized by a magnetostratigraphic scale (with unnamed chrons), but with no zonal scheme for dating. A few years later, this section was dated by the study of a calpionellid distribution and an ammonite zonation (Kietzmann et al., 2021). As the magnetostratigraphy is not reported in fig. 6 of the latter authors, we propose to report some calpionellid events in fig. 1 of Kohan Martínez et al. (2017). This allowed us to identify the magnetic chrons, mainly using the FOs of *C. simplex* and *C. oblonga* that are generally recorded in chrons M16r and M16n of the studied sections, respectively (Fig. 40). According to this pattern, the FO of *C. darderi* is observed in Chron M13r at Puerta Curaco; but it should be noted that this index species is represented by one sample and could occur earlier (in M14r as expected). However, our interpretation should be considered with caution. Dodd et al. (2015) reported an extensive magnetostratigraphic study for the Etendeka portion (in Namibia, Tafelkop section) of the Paraná–Etendeka LIP (Fig. 40). In the basal part of their composite magnetostratigraphy, Chron M14r is recorded. For the Atlantic Ocean, the DSDP holes 534A and 603B are characterized by a magnetostratigraphic scale (Ogg, 1983, 1987). According to Ogg (1987), “the Valanginian cannot be correlated between sites and do not match the M-sequence block model”. However, in site 534A, the M14r seems to be recognized. These two boreholes were correlated with the Polaveno section (Bornemann and Mutterlose, 2008; see Fig. 37 for the correlation between the Polaveno section and DSDP hole 534A), showing in the three sites the trend in the carbon isotopic curve during the Valanginian.

**Vergol-Cañada Luenga versus continental successions:** A syn-
thesis of Tethyan-Boreal correlations between marine and continen-
tal facies covering the Berriasian-Valanginian interval was made by
Hoedemaker (1987). It should be noted that the B/V boundary is placed
in his chart at the base of the *T. alpillensis* Zone, and the interpretation of
his *T. pertransiens* Zone does not correspond to the current concept.
The B/V boundary defined and largely characterized in marine suc-
cessions can be correlated with the non-marine ones of the English
Purbeck-Wealden stratotypes zoned by ostracods and palynomorphs
(Allen and Wimbledon, 1991). Those authors proposed updated cor-
relations between the north European Purbeck-Wealden onshore
basins, and with global marine standards. Ogg et al. (1994), who pro-
vided a composite magnetic scale of the Portland and Purbeck Beds
from the Dorset and Wilshire of southern England, noted that “the ter-
restrial to marginal-marine Purbeck Beds encompass polarity chrons
M19r through M14r, implying deposition from latest Tithonian (Late
Portlandian) to the beginning of the Valanginian stage” (Fig. 40).
Another work allowing us a correlation with a non-marine succession

is given by Jiménez et al. (2021) who provided a magnetostratigra-
phy of a thick continental succession (largely fluvial-facies sedimen-
tary sequence) well exposed in the northern Andes (Colombia). According
to their Model A (their fig. 11), the Chron M14 could be recorded in
the top part of the Cuchilla del Ramo section (Fig. 40).

Synthesis

In order to summarize and complete previous parts on the global
correlation, a compilation of marine successions is made for France
and Spain (Table 4a), Europe (Table 4b), and South America and
Africa (Table 4c). DSDP wells and continental successions are also
reported (Table 4d). For each line (section/wells), a cross (or a circle)
is put in the column (markers) when original/source data are avail-
able; main references are also indicated.

The Vergol section: Requirements for a GSSP
and Series of Stratigraphic Markers

The Vergol Section and Requirements for a GSSP

Requirements and key features of the Vergol section for the GSSP
of the Berriasian/Valanginian (B/V) boundary are presented in Table 5:
geology and lithology (Table 5a), bio-chemical-physical stratigraphy
(Table 5b), and accessibility, development and protection Table 5c).

Series of Stratigraphic Markers through the Vergol Sec-
tion

The base of the Valanginian is defined at the base of limestone bed
number VGL-B136. This level coincides with the First Occurrence
(FO) of the ammonite species *Hoedemaekeria* (nov. gen.) *pertrans-
siens* which marks the base of the *H. pertransiens* Zone.

Concerning the carbon isotope stratigraphy, a short-lived plateau in
values (~1.1‰ in limestone; ~0.8‰ in marls) is recorded in the upper
part of *T. alpillensis* Zone, and then a general trend toward low δ¹³C
values occurs across the B/V boundary to reach a negative shift in the
lower part of the *H. pertransiens* Zone (~0.5‰ in limestone; ~0.3‰
in marls).

At the base of VGL-B136 (19.23 m), the predicted value of ⁸⁷Sr/
⁸⁶Sr is 0.707289 (± 0.000004; 2.se, n = 12). The Valanginian GSSP is,
for now, the only Cretaceous GSSP that has been profiled for ⁸⁷Sr/⁸⁶Sr.

In addition to the primary marker, a series of secondary biostrati-
graphic events of inter-regional correlation value is provided in Table
6 in order to characterize the interval around the B/V boundary at the
Vergol section.

Summary

The Global boundary Stratotype Section and Point (GSSP) for the
base of the Valanginian Stage is the base of bed VGL-B136 at 19.23
metres in the Vergol Section (Montbrun-les-Bains, Drôme, France).
This point is marked by the First Occurrence (FO) of the ammonite
*Hoedemaekeria* (nov. gen.) *pertransiens* as primary marker. Additional
<table><caption>Table 4a. Lists of sections or wells representing marine palaeo-environments located in France and Spain (Table 4a), in other countries of Europe (Table 4b), and in South America and Africa (Table 4c); list of DSDP wells and continental successions (Table 4d). For each site, data available on biostratigraphy (A= ammonite, B= belemnite, C= calpionellid, N = calcareous nannofossil, CD = calcareous dinoflagellate, OD = organic dinoflagellate) and chemical-physical stratigraphy (C = carbon isotopes, Sr = strontium isotopes, Mag = magnetic scale) is indicated by a cross (x) or a circle (o). Main references are indicated; some of them can be consulted preferentially (* = see references therein)</caption><thead><tr><th rowspan="2">Section</th><th rowspan="2">Location</th><th colspan="4">Biostratigraphy</th><th colspan="3">Chemical-physical stratigraphy</th><th rowspan="2">Reference</th></tr><tr><th>A</th><th>B</th><th>C</th><th>N</th><th>CD=x<br>OD=0</th><th colspan="2">Isotope</th><th rowspan="2">Mag</th></tr><tr><th></th><th></th><th></th><th></th><th></th><th></th><th></th><th>C</th><th>Sr</th><th></th></tr></thead><tbody><tr><td>Vergol</td><td>France</td><td>x</td><td>x</td><td>x</td><td>x</td><td>x, o</td><td>x</td><td>x</td><td>McArthur et al. (2007)<br>Gréselle et al. (2011)<br>Martinez et al. (2013)<br>Janssen (2021)<br>Kenjo et al. (2021*)<br>McArthur and Howarth (2025)<br>Current work</td></tr><tr><td>Angles</td><td>France</td><td>x</td><td></td><td>x</td><td>x</td><td></td><td>x</td><td></td><td>Allemann and Remane (1979)<br>Duchamp-Alphonse et al. (2007*)</td></tr><tr><td>Barret-le-Bas</td><td>France</td><td>x</td><td></td><td>x</td><td></td><td></td><td></td><td></td><td>Remane and Thieuloy (1973a)<br>Allemann and Remane (1979)<br>Thieuloy (1979)<br>Blanc (1996)</td></tr><tr><td>Montclus</td><td>France</td><td>x</td><td></td><td>x</td><td>x</td><td></td><td>x</td><td></td><td>Morales et al. (2013, 2016*)</td></tr><tr><td>Orpierre</td><td>France</td><td></td><td>x</td><td>x</td><td></td><td></td><td>x</td><td></td><td>Charbonnier et al. (2013*)</td></tr><tr><td>Berrias</td><td>France</td><td>x</td><td></td><td>x</td><td>x</td><td>x, o</td><td>x</td><td>x</td><td>Galbrun et al. (1986)<br>Emmanuel and Renard (1993)<br>Jan du Chène et al. (1993*)<br>Blanc (1996)</td></tr><tr><td>Ginestoux –<br>Les Oliviers<br>La Garenne</td><td>France</td><td>x</td><td></td><td>x</td><td></td><td></td><td></td><td></td><td>Le Hégarat and Remane (1968)<br>Le Hégarat (1973)</td></tr><tr><td>La Faurie - Pusteau</td><td>France</td><td>x</td><td></td><td>x</td><td></td><td></td><td></td><td></td><td>Le Hégarat (1973)<br>Remane and Thieuloy (1973b)</td></tr><tr><td>Majastres</td><td>France</td><td>x</td><td>x</td><td>x</td><td>x</td><td></td><td></td><td></td><td>Bulot (1995)<br>Blanc (1996)<br>Janssen (2021)</td></tr><tr><td>Cañada Luenga</td><td>Spain</td><td>x</td><td>x</td><td>x</td><td>x</td><td>x, o</td><td>x</td><td>x</td><td>Ogg et al. (1988)<br>Aguado et al. (2000*)<br>Janssen (2003, 2021)<br>McArthur et al. (2007)<br>Current work</td></tr><tr><td>Miravetes</td><td>Spain</td><td>x</td><td>x</td><td>x</td><td>x</td><td>o</td><td></td><td></td><td>Allemann et al. (1975)<br>Hoedemaeker (1982)<br>Hoedemaeker and Leereveld (1995)<br>Janssen (1997, 2003)<br>Leereveld (1997)<br>Aguado et al. (2000*)</td></tr></tbody></table>

markers for correlation are provided. A Standard Auxiliary Boundary Stratotype (SABS) at Cañada Luenga section (Cehegin, SE Spain) demonstrates that this point corresponds to a level within magnetic Chron M14r.

## Integrated Stratigraphy of the Berriasian/Valanginian Boundary of the Vergol Section

The Vergol section (Vocontian basin, SE France) is located in a parcel of land that belongs to the municipality of Montbrun-les-Bains (Departement of Drôme); as public property, the site is fully and permanently accessible. The outcrop conditions are highly suitable for accurate observations and high-resolution sampling.

The Berriasian/Valanginian (B/V) boundary was studied in a 53.12 m thick interval from beds VGL-B95 to VGL-V43 (Fig. 41). The suc-

cession is composed of a marl–limestone alternation, stacked hierarchically (see below), characterized by a continuous sedimentation (no gaps or condensation) and the absence of tectonic disturbance. This thick and expanded section has a very good sedimentary record; the average sedimentation rate is 23 m/Myr (see below).

The Vergol site is well correlated with other sections of SE France, from the Jura-Dauphinois to Provence platforms, via the Vocontian basin. This large transect allowed us to define a cyclostratigraphic framework, and four orders of depositional cycles were recognized (elementary and small/medium/large sequences). Coupled with a study on the depositional geometries, a reconstruction of sea-level fluctuations is proposed for the studied interval. It can be noted that the boundary level (VGL-B136) occurred during a sea-level highstand (Fig. 41). A correlation between the Vergol and Ait Hamouch (Morocco) sections shows that the major sequence boundaries Be8, Va1 and Va2 were recognized in
<table><caption>Table 4b. (continued)</caption><thead><tr><th rowspan="2">Section</th><th rowspan="2">Location</th><th colspan="4">Biostratigraphy</th><th colspan="3">Chemical-physical stratigraphy</th><th rowspan="2">Reference</th></tr><tr><th>A</th><th>B</th><th>C</th><th>N</th><th>CD=x<br>OD=0</th><th colspan="2">Isotope</th><th rowspan="2">Mag</th></tr><tr><th></th><th></th><th></th><th></th><th></th><th></th><th></th><th>C</th><th>Sr</th><th></th></tr></thead><tbody><tr><td>(Fiume) Bosso</td><td>Italy</td><td></td><td>x</td><td>x</td><td></td><td></td><td></td><td></td><td>x</td><td>Channell and Grandesso (1987*)<br>Ogg et al. (1988)<br>Bralower et al. (1989)</td></tr><tr><td>Capriolo</td><td>Italy</td><td></td><td>x</td><td>x</td><td></td><td></td><td>x</td><td></td><td>x</td><td>Channell et al. (1987, 1993)<br>Ogg et al. (1988)</td></tr><tr><td>Chiaserna Monte Acuto</td><td>Italy</td><td></td><td></td><td>x</td><td></td><td></td><td></td><td></td><td></td><td>Sprovieri et al. (2006)</td></tr><tr><td>Fonte Giordano</td><td>Italy</td><td></td><td></td><td>x</td><td></td><td></td><td></td><td></td><td>x</td><td>Bralower et al. (1989)</td></tr><tr><td>Polaveno</td><td>Italy</td><td></td><td></td><td>x</td><td></td><td></td><td>x</td><td></td><td>x</td><td>Bornemann and Mutterlose (2008)</td></tr><tr><td>Pusiano</td><td>Italy</td><td></td><td></td><td>x</td><td></td><td></td><td>x</td><td></td><td>x</td><td>Channell et al. (1993)</td></tr><tr><td>Xausa</td><td>Italy</td><td></td><td>x</td><td>x</td><td></td><td></td><td>x</td><td></td><td>x</td><td>Channell et al. (1987)<br>Ogg et al. (1988)<br>Weissert and Channell (1989)</td></tr><tr><td>Hollenstein an der Ybbs</td><td>Austria</td><td>x</td><td></td><td>x</td><td></td><td>x</td><td></td><td></td><td></td><td>Vašíček et al. (1999)</td></tr><tr><td>Klausriegler-Bach</td><td>Austria</td><td>x</td><td></td><td>x</td><td></td><td>x</td><td></td><td></td><td></td><td>Lukeneder and Reháková (2004)</td></tr><tr><td>Hochkogel</td><td>Austria</td><td>x</td><td></td><td>x</td><td></td><td>x</td><td></td><td></td><td></td><td>Lukeneder and Reháková (2007)</td></tr><tr><td>Hárskút</td><td>Hungary</td><td>x</td><td>x</td><td>x</td><td>x</td><td>x</td><td>x</td><td></td><td>x</td><td>Fözy et al. (2010)<br>Price et al. (2016*)<br>Lodowski et al. (2022)</td></tr><tr><td>Kapušnica</td><td>Poland</td><td>x</td><td></td><td>x</td><td></td><td>x</td><td></td><td></td><td></td><td>Pszczółkowski and Myczyński (2004)</td></tr><tr><td>Kryta Valley</td><td>Poland</td><td></td><td></td><td>x</td><td>x</td><td>x</td><td>x</td><td></td><td>x</td><td>Grabowski et al. (2024)</td></tr><tr><td>Lysonka</td><td>Poland</td><td>x</td><td></td><td>x</td><td></td><td>x</td><td>x</td><td></td><td></td><td>Pszczółkowski and Myczyński (2004)<br>Grabowski et al. (2013)</td></tr><tr><td>Rówienka</td><td>Poland</td><td></td><td></td><td>x</td><td></td><td></td><td>x</td><td></td><td>x</td><td>Grabowski et al. (2019a)</td></tr><tr><td>Strážovce</td><td>Slovakia</td><td>x</td><td>x</td><td>x</td><td>x</td><td>x</td><td></td><td></td><td></td><td>Vašíček et al. (1983)</td></tr><tr><td>Mráznické Lúcky</td><td>Slovakia</td><td></td><td></td><td>x</td><td></td><td>x</td><td></td><td></td><td></td><td>Vašíček et al. (1983)</td></tr><tr><td>Brodno</td><td>Slovakia</td><td></td><td></td><td>x</td><td></td><td>x</td><td></td><td></td><td></td><td>Vašíček et al. (1994)</td></tr><tr><td>Glboč</td><td>Slovakia</td><td></td><td></td><td>x</td><td></td><td>x</td><td>x</td><td></td><td></td><td>Vašíček et al. (1994)<br>Grabowski et al. (2010)</td></tr><tr><td>Barlya</td><td>Bulgaria</td><td>x</td><td></td><td>x</td><td>x</td><td>x</td><td></td><td></td><td>x</td><td>Lakova et al. (1999)<br>Petrova et al. (2011)<br>Grabowski et al. (2016, 2021*)</td></tr><tr><td>Zavodskaya Balka</td><td>Ukraine<br>(Crimea)</td><td>x</td><td></td><td></td><td></td><td></td><td></td><td></td><td>x</td><td>Arkadiev et al. (2017, 2018)</td></tr><tr><td>Speeton</td><td>England</td><td>x</td><td></td><td>x</td><td></td><td>x</td><td>x</td><td></td><td></td><td>McArthur et al. (2004*)<br>Mutterlose et al. (2014)<br>Duxbury (2018)</td></tr><tr><td>Rödryggen</td><td>Greenland</td><td>x</td><td></td><td>x</td><td></td><td></td><td>x</td><td>x</td><td></td><td>Pauly et al. (2012a, b, 2013)<br>Möller et al. (2015)<br>McArthur and Howarth (2025)</td></tr></tbody></table>

<table><caption>Table 4c. (continued)</caption><thead><tr><th rowspan="2">Section/well</th><th rowspan="2">Location</th><th colspan="4">Biostratigraphy</th><th colspan="3">Chemical-physical stratigraphy</th><th rowspan="2">Reference</th></tr><tr><th>A</th><th>B</th><th>C</th><th>N</th><th>CD=x<br>OD=0</th><th colspan="2">Isotope</th><th rowspan="2">Mag</th></tr><tr><th></th><th></th><th></th><th></th><th></th><th></th><th></th><th>C</th><th>Sr</th><th></th></tr></thead><tbody><tr><td>Puerta Curaco</td><td>Argentina</td><td>x</td><td></td><td>x</td><td></td><td></td><td></td><td></td><td>x</td><td>Kohan Martínez et al. (2017)<br>Kietzmann et al. (2021)</td></tr><tr><td>Cuesta del Chihuido</td><td>Argentina</td><td>x</td><td></td><td>x</td><td></td><td>x</td><td></td><td></td><td></td><td>Kietzmann et al. (2021, 2023)</td></tr><tr><td>Narambuena block (wells 1-3)</td><td>Argentina</td><td></td><td></td><td>x</td><td></td><td>x</td><td></td><td></td><td></td><td>Kietzmann et al. (2021, 2023)</td></tr><tr><td>Zalidou, Aït Hamouch</td><td>Morocco</td><td>x</td><td></td><td></td><td>x</td><td></td><td>x</td><td></td><td></td><td>Reboulet et al. (2022*)</td></tr><tr><td>Tafelkop</td><td>Namibia</td><td></td><td></td><td></td><td></td><td></td><td></td><td></td><td>x</td><td>Dodd et al. (2015)</td></tr></tbody></table>
<table><caption>**Table 4d. (continued)**</caption><thead><tr><th rowspan="2">Well/section</th><th rowspan="2">Location</th><th colspan="4">Biostratigraphy</th><th colspan="3">Chemical-physical stratigraphy</th><th rowspan="2">Reference</th></tr><tr><th>A</th><th>B</th><th>C</th><th>N</th><th>CD=x<br>OD=0</th><th>Isotope<br>C</th><th>Sr</th><th>Mag</th></tr></thead><tbody><tr><td>DSDP 535</td><td>Gulf of Mexico</td><td></td><td></td><td></td><td>x</td><td></td><td>x</td><td></td><td>x</td><td>Bornemann and Mutterlose (2008*)</td></tr><tr><td>DSDP 534A<br>DSDP 603B</td><td>West Atlantic</td><td></td><td></td><td></td><td>x</td><td></td><td>x</td><td></td><td>x</td><td>Bornemann and Mutterlose (2008*)<br>Price et al. (2016*)</td></tr><tr><td>Dorset<br>(continental succession)</td><td>England</td><td></td><td></td><td></td><td></td><td></td><td></td><td></td><td>x</td><td>Ogg et al. (1994*)</td></tr><tr><td>Cuchilla del Ramo<br>(continental succession)</td><td>Colombia</td><td></td><td></td><td></td><td></td><td></td><td></td><td></td><td>x</td><td>Jiménez et al. (2021)</td></tr></tbody></table>

<table><caption>**Table 5a. Key features of the Vergol section for geology and lithology (Table 5a), bio-chemical-physical stratigraphy (Table 5b), and accessibility, development and protection (Table 5c)**</caption><thead><tr><th>GEOLOGY and LITHOLOGY</th><th>Vergol section (Montbrun-les-Bains, France, Vocontian basin)</th></tr></thead><tbody><tr><td>Exposure over an adequate thickness.</td><td>Yes. 53 m thick, from beds VGL-B95 to VGL-V43.</td></tr><tr><td>Continuous sedimentation.<br>No gaps or condensation close to the boundary.</td><td>Yes. A basinal and expanded section without gaps or condensation.</td></tr><tr><td>Rate of sedimentation.</td><td>According to the astrochronology, the average sedimentation rate is around 23 m/Myr.</td></tr><tr><td>Absence of synsedimentary or tectonic disturbance.</td><td>Yes, both factors can be excluded. There is a slump, but 35 m above the B/V boundary.</td></tr><tr><td>Absence of metamorphism and strong diagenetic alteration.</td><td>Yes, both factors can be excluded. According to the clay mineralogy, the influence of diagenesis was not sufficient to profoundly modify the initial detrital composition of the clay assemblages.</td></tr><tr><td>Absence of vertical facies changes at/near the boundary.</td><td>Yes. From the base to the top of the section, there is a uniform lithology made by a monotonous marl-limestone alternation.</td></tr><tr><td>Favourable facies for long range correlations.</td><td>Yes. Located in open marine environment and characterized by a hemipelagic facies, the section is suitable for long distance correlations.</td></tr></tbody></table>

<table><caption>**Table 5b. (continued)**</caption><thead><tr><th>BIO-CHEMICAL-PHYSICAL STRATIGRAPHY</th><th>Vergol section (Montbrun-les-Bains, France, Vocontian basin)</th></tr></thead><tbody><tr><td>Biostratigraphy.</td><td>Abundant and diverse of generally well-preserved ammonoids, belemnites, calpionellids, nannofloras and dinoflagellates (and other palynomorphs). The section is also characterized by ichnofossils and microfacies study.</td></tr><tr><td>Chemostratigraphy.</td><td>Accurate carbon, oxygen and strontium isotope stratigraphy available. Carbonate, organic and phosphorus contents also analysed.</td></tr><tr><td>Sequence stratigraphy.</td><td>Cyclostratigraphic framework available. Four orders of depositional cycles are recognized. The major sequence boundaries are identified in the northern (France, including Vergol) and southern (Morocco) margins of the Tethys Ocean.</td></tr><tr><td>Astrochronology.</td><td>Available. Obtained from the detection of the Milankovitch cycles from the Gamma-Ray Total Count and Mass Magnetic Susceptibility signals. The age model, based on astrochronology performed on the Vergol section and anchored on a radioisotopic age from the Neuquén basin (Argentina), allows us to date the base of the Valanginian Stage (= base of the <i>H. pertransiens</i> ammonite Zone) at 137.05 Ma (± 0.2 Ma), and the base of ammonite (sub-)zones (and therefore their numerical durations).</td></tr><tr><td>Magnetostratigraphy.</td><td>No. Palaeomagnetic investigations (both thermal and alternating field demagnetization methods) reveal that the Vergol section is remagnetized. However, an integrated stratigraphy provides an accurate correlation with the Cañada Luenga SABS characterized by magnetic chrons.</td></tr><tr><td>Chronometry.</td><td>No. But see astrochronology for an age model.</td></tr></tbody></table>

<table><caption>**Table 5c. (continued)**</caption><thead><tr><th>ACCESSIBILITY, DEVELOPMENT and PROTECTION</th><th>Vergol section (Montbrun-les-Bains, France, Vocontian basin)</th></tr></thead><tbody><tr><td>GSSP indicated by a permanent marker.</td><td>A permanent marker will be placed.</td></tr><tr><td>Physical and logistical accessibility.</td><td>Section very close of the road (D159) with car park. Large area of exposure. Very good outcrop conditions highly suitable for accurate observations and high-resolution sampling.</td></tr><tr><td>Free access for research.</td><td>Open access from public. Section fully and permanently accessible for researchers as it is public property.</td></tr><tr><td>Permanent protection of the site.</td><td>Section located in the "Parc Naturel Régional des Baronnies Provençales". Substantial public support also provided by the Montbrun-les-Bains municipality and the Council of the Drôme Department. These institutions are engaged in the development and protection of the site (in preparation).</td></tr></tbody></table>
<table><caption>Table 6. Series of primary and secondary biological markers along the Vergol section. See also Fig. 4 for the indications of cumulative thicknesses (in meter, measured from the base of the section) of the Vergol section</caption><thead><tr><th>Bed number<br>M (Marl layer)<br>L (Limestone layer)</th><th>Meter at the<br>base (b) or<br>top (t) of layer</th><th>Event<br>LO (Last Occurrence)<br>FO (First Occurrence)</th></tr></thead><tbody><tr><td>VGL-V5 (L)</td><td>28.87 (b)</td><td>FO <i>Berriasibelus exstinctorius</i> (belemnite)</td></tr><tr><td>VGL-V4 (L)</td><td>28.11 (b)</td><td>FO <i>Micrantholithus speetonensis</i> (calcareous nannofossil)</td></tr><tr><td>VGL-V2 (L)</td><td>26.91 (b)</td><td>FO <i>Neolissoceras (Vergoliceras) salinarium</i> (ammonite) and <i>Calpionellites caravacaensis</i> (calpionellid)</td></tr><tr><td>VGL-B150 (M)</td><td>25.27 (b)</td><td>FO <i>Castellanibelus orbignyanus</i> (belemnite)</td></tr><tr><td>VGL-B149 (L)</td><td>24.54 (b)</td><td>FO <i>Calpionellites major</i> (calpionellid)</td></tr><tr><td>VGL-B146 (M)</td><td>23.57 (b)</td><td>FO <i>Calcicalathina oblongata</i> (calcareous nannofossil)</td></tr><tr><td>VGL-B142 (M)</td><td>22.08 (b)</td><td>occurrence <i>Thalassiphora? charollaisii</i> (organic dinoflagellate)</td></tr><tr><td>VGL-B141 (L)</td><td>21.27 (b)</td><td>FO <i>Neocomites premolicus</i> (ammonite)</td></tr><tr><td>VGL-B137 (L)</td><td>19.80 (b)</td><td>FO <i>Hoedemaekeria</i> (nov. gen.) <i>gratianopolitense</i> (ammonite)</td></tr><tr><td><b>VGL-B136 (L)</b></td><td><b>19.23 (b)</b></td><td><b>FO Hoedemaekeria (nov. gen.) pertransiens (ammonite)</b></td></tr><tr><td>VGL-B135 (L)</td><td>19.04 (t)</td><td>LO <i>Hoedemaekeria</i> (nov. gen.) <i>otopeta</i> and <i>Berriasella calisto</i> (ammonite)</td></tr><tr><td>VGL-B133 (L)</td><td>17.89 (b)</td><td>FO <i>Calpionellites darderi</i> and <i>C. coronatus</i> (calpionellid)</td></tr><tr><td>VGL-B129 (L)</td><td>16.46 (t)</td><td>LO <i>Tirnovella alpillensis</i> (ammonite)</td></tr><tr><td>VGL-B119 (L)</td><td>12.98 (b)</td><td>FO <i>Colomisphaera conferta</i> (calcareous dinoflagellate)</td></tr><tr><td>VGL-B117 (L)</td><td>12.05 (b)</td><td>FO <i>Praecalpionellites murgeanui</i> (calpionellid)</td></tr><tr><td>VGL-B116 (L)</td><td>11.33 (b)</td><td>FO <i>Hoedemaekeria</i> (nov. gen.) <i>otopeta</i> (ammonite)</td></tr><tr><td>VGL-B112 (M)</td><td>9.03 (b)</td><td>FO <i>Percivalia fenestrata</i> (calcareous nannofossil)</td></tr><tr><td>VGL-B110 (M)</td><td>7.28 (b)</td><td>FO <i>Muderongia mcwhaei</i> (organic dinoflagellate)</td></tr><tr><td>VGL-B107 (L)</td><td>5.97 (b)</td><td>FO <i>Colomisphaera vogleri</i> (calcareous dinoflagellate)</td></tr><tr><td>VGL-B96 (L)</td><td>0.38 (b)</td><td>FO <i>Tirnovella alpillensis</i> (ammonite)</td></tr><tr><td>VGL-B95 (L)</td><td>0 m (b)</td><td>Base of this bed = base of the section</td></tr></tbody></table>

the northern and southern margin of the Mesozoic Tethys Ocean, respectively.

Macro/microfossils are generally abundant, diverse and well preserved. Ammonites, belemnites, calpionellids, calcareous nannofossils and calcareous dinoflagellate cysts, palynomorphs (including organic-walled dinoflagellate cysts), ichnofossils and microfacies were studied with high-resolution sampling and analysis. At Vergol, the base of the Valanginian is defined at the base of limestone bed VGL-B136 (base of layer at 19.23 m) that coincides with the FO of *Hoedemaekeria pertransiens* which, as index species, also marks the base of the first Valanginian ammonite zone (Fig. 41). The ammonite data/results from two authors (J. Klein and S. Reboulet) are largely in agreement. The FO of *Castellanibelus orbignyanus* (belemnite) is recorded in marl layer VGL-B150 (base of layer at 25.27 m). The microfossil events that best approximate the B/V boundary are the FO of *Calpionellites darderi* (calpionellid) in limestone bed VGL-B133 (base of layer at 17.89 m) and the FO of *Calcicalathina oblongata* (calcareous nannofossil) in marl layer VGL-B146 (base of layer at 23.57 m). Other secondary biostratigraphic markers include the FO of *Colomisphaera conferta* (calcareous dinoflagellate) recorded in limestone bed VGL-B119 (base of layer at 12.98 m). Two organic-walled dinoflagellate cysts events might be of particular significance for regional value: an isolated occurrence of *Thalassiphora? charollaisii* in marl layer VGL-B142 (base of layer at 22.08 m) and the FO of *Muderongia mcwhaei* in marl layer VGL-B110 (base of layer at 7.28 m).

Concerning the carbon isotope stratigraphy, both marls and limestones displays the same long-term trend in $\delta^{13}$C values in the interval

around the B/V boundary: a short-lived plateau in values (~1.1‰ in limestone; ~0.8‰ in marls) in the upper part of the *Tirnovella alpilensis* ammonite Zone, and then a general trend toward low $\delta^{13}$C values occurring across the B/V boundary to reach a negative shift in the lower part of the *H. pertransiens* ammonite Zone (~0.5‰ in limestone; ~0.3‰ in marls; Fig. 41). Strontium isotope stratigraphy (based on belemnites) is available for the Vergol section. According to the curve, the predicted value of $^{87}$Sr/$^{86}$Sr at the B/V boundary is 0.707289 ± 0.000004 (2.se, n = 12).

Vergol is a suitable reference section to establish an astronomical time scale of the studied interval (detection of the Milankovitch cycles from the GRTC and MS signals). Five 405-kyr eccentricity cycles are identified; for each of these, a sedimentation rate is proposed (Fig. 41). For the B/V sequence covering the boundary, the value is 17 m/Myr. A rate increase is observed for the Valanginian sequences to reach 26.5 m/Myr for V1 and 29 m/Myr for V2. Comparatively, both Berriasian sequences are characterized by lower sedimentation rates, 23.5 m/Myr for T.A.-405-1 and 18 m/Myr for T.A.-405-2. This is in agreement with the study of ichnofossils as only these two Berriasian sequences are characterized by the presence of *Zoophycos*, considering that their installation and development are partly explained by a low(er) sedimentation rate.

The floating ages of the 405-kyr eccentricity cycles are anchored on a CA-ID-TIMS U-Pb age obtained from zircons coming from a tuff layer in the Neuquén basin (Argentina, lower Hauterivian). This radioisotopic age is tied to the ammonite zonation recognized in this basin which in turn is correlated with the Mediterranean standard
<figure><img src="image_42.png" /><figcaption>Figure 41. Integrated stratigraphy of the Vergol section: biostratigraphy including ichnofossils, sequence stratigraphy, cyclo-astrochronology and chemical stratigraphy (strontium and carbon isotopes).</figcaption></figure>

zonation. The age model allows the base of the Valanginian Stage (= base of the *H. pertransiensis* ammonite Zone) to be dated at 137.05 Ma (±0.2 Ma). The uncertainty here includes the uncertainty in the radio-isotopic age obtained in the lower Hauterivian of the Neuquén basin and the uncertainty in the correlations from the Neuquén basin to the Vocontian basin. Numerical ages and durations of ammonite (sub-) zones are also provided.

Concerning the magnetostratigraphy, it was not possible to characterize magnetic reversals through the Vergol section. The palaeomagnetic study indicates that the upper Berriasian-lower Valanginian succession of Vergol was remagnetized. However, the magnetic scale was established in the Cañada Luenga section that is very well-correlated with the Vergol section using a solid integrated stratigraphy.

The integrated stratigraphy (bio-chemical-physical investigations)
<figure><img src="image_43.png" /><figcaption>**Figure 42.** Integrated stratigraphy of the Vergol section: biostratigraphy including a Sporomorph EcoGroup (SEG) plot, sequence stratigraphy, chemical stratigraphy (phosphorus content, clay mineralogy and organic geochemistry) and physical stratigraphy (Field GRS and XRF measurements).</figcaption></figure>

applied on the studied interval of the Vergol section allowed us to characterize sea-level and climatic fluctuations, and to give some information on water column and seafloor conditions. For example, this can be interpreted by modifications observed in the clay mineral assemblages, phosphorus contents, field GRS and XRF measurements, and Sporomorph EcoGroups (Fig. 42).

In conclusion, the base of the Valanginian is accurately dated by (bio-)stratigraphic events and the B/V boundary interval is also strongly characterized by major palaeoenvironmental changes well expressed at Vergol. This has strengthened the choice of the section as a GSSP.
## Main Characteristics of the Cañada Luenga Section

The SABS section for the base of the Valanginian is located in the Cañada Luenga ravine, near Cehegín (Murcia, SE Spain). The analyzed interval (beds 0 to 20) is about 13 metres thick and includes the uppermost Berriasian *Tirnovella alpillensis* ammonite Zone and the lower part of the basal Valanginian *Hoedemaekeria pertransiens* ammonite Zone. The lowermost part of the section (beds 0 to 3, 1.2 m thick, corresponding to the lower part of the *T. alpillensis* ammonite Subzone) is made up of nodular limestone, with evident signs of condensation. The rest of the section consists of an alternation of marl and marly limestone beds, deposited in a distal marine environment, with an average sedimentation rate of 9 m/Myr.

The fossil record is abundant and well preserved. The analysis of the stratigraphic distribution of ammonites, belemnites, calpionellids, calcareous dinoflagellates and calcareous nannofossils allows the establishment of a very accurate correlation with the Vergol section. The FO of *H. pertransiens*, primary marker for the B/V boundary, is located in bed 9 of the section (Figs. 31, 32). The correlation with the Vergol section is also reinforced by non-biostratigraphic tools, such as the carbon isotope curve, strontium isotope record and cyclostratigraphic analysis.

The Cañada Luenga section provides a reliable magnetostratigraphic record for the B/V boundary interval, spanning from the upper part of the M16n polarity chron to the lower part of the M14r polarity Chron. The high-resolution correlation between the Cañada Luenga and Vergol sections, well-controlled by an integrated stratigraphy (Fig. 33; see also graphic correlation, Fig. 34), ensures precise calibration of the GSSP against the Geomagnetic Polarity Time Scale. Thus, the base of magnetic Chron M14r recognized at Cañada Luenga (bed CL7) should occur in the “Otopeta calcareous bundle” at Vergol, and may be placed approximatively at layer VGL-B126 (Fig. 33).

## Acknowledgements

The final work on the Vergol section benefited from financial support of a project (2021-2023) funded by the Polish and French Ministries of foreign affairs (*Partenariat Hubert Curien*, cf. the current palaeomagnetic study that also includes the contribution of Chmielewski Andrezj, Iwanczuk Jolanta and Ploch Izabela from the Polish Geological Institute of Warsaw, colleagues who are hereby thanked), the CNRS SYSTER program (*WOAW SYSTER French project*; with the contribution of two students Léa Baubant and Durel Franchevel who are acknowledged), Project APVV-20-0079 (Slovakian National Grant Agency, thanks to Diana Ölveczká) and various grants from the Laboratoire de Géologie de Lyon. The International Subcommission on Cretaceous Stratigraphy is thanked for its support (via the former chair Maria Rose Petrizzo and the current chair Ian Jarvis) on the activities of the Valanginian Working Group and for the relevant comments made on the proposal by members (see the list in: http://cretaceous.stratigraphy.org/). We are also grateful to the Executive Committee and members of the International Commission on Stratigraphy who carefully scrutinized the formal proposal. Sincere thanks are also extended to the IUGS Executive Committee. The municipality of Montbrun-les-Bains, the Drôme Department and the “Parc Naturel Régional des Baronnies

Provençales” are thanked for their support in the project of development and protection of the Vergol site. The authors are grateful to other members of the Valanginian Working Group, the members of the Subcommission on Cretaceous Stratigraphy and the International Commission on Stratigraphy for their contribution in the “selection process” of a GSSP/SABS for the Stage. We acknowledge Peter Rawson and Ian Jarvis (Chair, Cretaceous Subcommission) for correcting the English of the formal proposal and the current manuscript, respectively. We would like to thank Sophie Passot (Lyon) for her bibliographic assistance. We are grateful to the editorial team of Episodes, especially Maria Rose Petrizzo, Associate Editor, and Brad S. Singer and an anonymous reviewer for both corrections and comments which improved the quality of an earlier version of the manuscript.

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Wilpshaar, M., and Leereveld, H., 1994, Palaeoenvironmental change in the Early Cretaceous Vocontian basin (SE France) reflected by dinoflagellate cysts. Review of Palaeobotany and Palynology, v. 84, pp. 121–128. doi:10.1016/0034-6667(94)90046-9

Wilson, J.L., 1975, Carbonate facies in geologic history. Springer, Berlin, 471 p. doi:10.1007/978-1-4612-6383-8

Wimbledon, W.A.P., Reháková, D., Svobodová, A., Elbra, T., Schnabl, P., Pruner, P., Šifnerová, K., Kdýr, Š., Dzyuba, O., Schnyder, J., Galbrun, B., Košťák, M., Vaňková, L., Copestake, P., Hunt, C.O., Riccardi, A., Poulton, T. P., Bulot, L.G., Frau, C., and Lena, L. de, 2020, The proposal of a GSSP for the Berriasian Stage (Cretaceous System): Part 1. Voluminia Jurassica 2020, v. 18, pp. 53–106. doi:10.7306/vj.18.5

Wimbledon, W.A.P., Elbra, T., Pruner, P., Schnabl, P., Kdýr, Š., Šifnerová, K., Frau, C., Bulot, L.G., Ölveczká, D., Svobodová, A., Mikuláš, R., and Reháková, D., 2024, A re-description of the historical stratotype for the Berriasian Stage (Cretaceous System): Biostratigraphy and magnetostratigraphy. Cretaceous Research, v. 160, 105892. doi:10.1016/j.cretres.2024.105892

Wippich, M.G.E., 2003, Valanginian (Early Cretaceous) ammonite faunas from the western High Atlas, Morocco, and the recognition of western Mediterranean ‘standard’ zones. Cretaceous Research, v. 24, pp. 357–374. doi:10.1016/S0195-6671(03)00049-1

Worsley, T.R., 1971, Calcareous nannofossil zonation of Upper Jurassic and Lower Cretaceous sediments from the Western Atlantic. Proceedings of the 2nd Planktonic Conference, 1970, v. 2, pp. 1301–1321.

Wortmann, U.G., and Weissert, H., 2000, Tying platform drowning to perturbations of the global carbon cycle with a delta $\delta^{13}C_{org}$-curve from the Valanginian of DSDP site 416. Terra Nova, v. 12, pp. 289–294. doi:10.1046/j.1365-3121.2000.00312.x

<figure><img src="image_44.png" /></figure>

Stéphane Reboulet lecturer (since 1996) at the University of Lyon (France), teaches Palaeontology and Geology at the Lyon Observatory. His research interests in the Lyon Geology Laboratory include the taxonomy, evolution, biostratigraphy and palaeoecology of early Cretaceous ammonites from the Mediterranean Province. He is chair (since 2005) of the Lower Cretaceous Ammonite Working Group (the Kilian Group; https://cretaceous.stratigraphy.org/wgs/kilian), and co-chair (since 2016) of the Valanginian Working Group (https://cretaceous.stratigraphy.org/wgs/valanginian) of the International Subcommission on Cretaceous Stratigraphy. He was involved in the development of the Hauterivian Proposal (GSSP ratified in 2019) and the Golden Spike ceremony (2024, including the Albian GSSP).
<figure><img src="image_45.png" /></figure>

**Miguel Company** is co-chair of the Valanginian Working Group of the International Sub-commission on Cretaceous Stratigraphy. Now retired, he was until 2023 'Profesor Titular' (senior lecturer) at the University of Granada (Spain), teaching general and applied palaeontology. His research interests focus on taxonomy, evolution, palaeoecology, palaeobiogeography and biostratigraphy of Early Cretaceous ammonites from the Tethyan Realm. He has also been chair of the Barremian Working Group, leading the development of the GSSP proposal for this stage (ratified in March 2023) and the Golden Spike ceremony (November 2024).

<figure><img src="image_46.png" /></figure>

**Now retired, Jaap Klein** was managing director science communication at the University of Amsterdam (The Netherlands), and from 1990 honorary researcher at the Naturalis Biodiversity Center, Department of Marine Zoology. He is the author of Fossilium Catalogus I: Animalia Lower Cretaceous Ammonites in 11 volumes.

<figure><img src="image_47.png" /></figure>

**François Baudin** is currently professor of Sedimentology and Petroleum Geology at Sorbonne University, Paris (France). He got his PhD at Pierre and Marie Curie University (1989) and "Habilitation à Diriger des Recherches" at the same place (1998). His researches are focused to the processes that control the preservation and distribution of organic matter in sedimentary rocks as well as recent sediments and soils. He has published more than 200 articles in international journals and several textbooks. François Baudin is active in some scientific societies including the Geological Society of France, which he has chaired from 2020 to 2022.

<figure><img src="image_48.png" /></figure>

**Damian Gerard Lodowski** holds the position of the assistant professor in the Polish Geological Institute, National Research Institute. In 2017-2023 he did his PhD entitled "Tracing the latest Jurassic-earliest Cretaceous paleoenvironmental changes in circum Carpathian region in light of sedimentologic, paleomagnetic and geochemical data". Currently he is primarily focused on the topic of the J/K oceanographic perturbations, their controlling factors and geographic distribution. Member of the Coniacian working group.

<figure><img src="image_49.png" /></figure>

**Jean-François Deconinck** is Professor Emeritus at the University of Burgundy Europe. A specialist in clay sedimentation, he has worked mainly in Jurassic and Cretaceous formations where he focuses on reconstructing depositional environments. He uses clay minerals in particular as tools for reconstructing ancient climates.

<figure><img src="image_50.png" /></figure>

**Davide Olivero** is "Maître de Conférences" (lecturer) at the Lyon Observatory at the University of Lyon (France). At the beginning of his career he worked on the Middle Jurassic ammonites of the French Subalpine basin. Now his research focuses on the ichnology and palaeoecology, especially in the Mesozoic and Cenozoic successions of southeastern France. He was formerly involved in the proposal of the Bathonian GSSP, ratified in 2008.

<figure><img src="image_51.png" /></figure>

**Ginés Alfonso de Gea** is senior lecturer in the Department of Geology at the University of Jaén (Spain). He teaches geology, stratigraphic, micropalaeontology, rock sedimentary and geologic maps. His research is focussed on stratigraphy, biostratigraphy (using nanofossils and planktonic foraminifera), sedimentology and geochemistry of the Cretaceous of the Betic Cordillera. Currently, his research focuses on the analysis of palaeogeographic and palaeoenvironmental changes during the Cretaceous, with special interest in the multidisciplinary study of Oceanic Anoxic Events.

<figure><img src="image_52.png" /></figure>

**Daniela Reháková** is university teacher in the Department of Geology and Palaeontology, Faculty of Natural Sciences, Comenius University in Bratislava. She teaches systematic, palaeontology of invertebrates, palaeoecology, biostratigraphy and sequence stratigraphy. She is the (co-)author of more than 300 scientific contributions in morphometry, biostratigraphy and evolution of Late Jurassic to Early Cretaceous calpalenellids and calcareous dinoflagellates, and carbonate microfacies and paleoenvironmental modelings.
# Appendix 1. Taxonomic note on the new genus *Hoedemaekeria* (Ammonite)

Company M. and Reboulet S. are contributors of this taxonomic note. Thus, considering taxonomic rules, they should be considered as co-authors of this new genus.

* Order Ammonitida Haeckel, 1866

* Suborder Ammonitina Haeckel, 1866

* Superfamily Perisphinctoidea Steinmann, 1890

* Family Neocomitidae Salfeld, 1921

* Genus *Hoedemaekeria* nov. gen.

* ZooBank registration number: 37B95C43-797A-4C5F-93B7-5602790-B8CAE

* Type species: *Thurmannia pertransiens* Sayn, 1907, p. 43.

**Specific content.** *Hoedemaekeria pertransiens* (Sayn, 1907), *Hoedemaekeria gratianopolitensis* (Sayn, 1907) and *Hoedemaekeria otopeta* (Thieuloy, 1979).

**Etymology.** The new genus is dedicated to our Dutch colleague Philip J. Hoedemaeker, who was the first to question the attribution of its type species to the genus *Thurmanniceras*, in which it had traditionally been included (see Klein, 2005, pp. 279-280). The generic name is to be treated as feminine.

**Diagnosis.** Discoidal, subinvolute to subevolute neocomitids, with compressed, rectangular to subtrapezoidal whorl section, gently convex flanks and flattened venter. Marked sexual dimorphism, with small to moderate sized microconchs (45-70 mm in diameter) showing lappeted apertures, and large to very large macroconchs (120-250 mm in diameter) with simple apertures.

Both dimorphs show a similar ontogenetic development. In the early whorls, the section is equidimensional to weakly compressed. The ribs are rigid, slightly prorsirate, simple or bifurcated towards the middle of the flank, and end in an oblique, small ventrolateral thickening, leaving a narrow smooth ventral band. Numerous oblique constrictions regularly appear throughout this stage.

Gradually the shell acquires its characteristic morphology, the whorl expansion rate increasing and the section compressing. The ribs become sinuous, arise singly or in pairs from small periumbilical bulae and most of them bifurcate in the upper third of the flank. The constrictions tend to disappear and, in some species, also a more or less pronounced attenuation of the ribbing on the flank occurs.

In the body chamber, which occupies about half a whorl, noticeable changes occur in the structure of the shell. The microconchs develop an elliptical section, with a gently convex venter, accompanied by a moderate umbilical egression. In the macroconchs, the relative whorl width increases, and the ribs tend to cross the broadly rounded ventral region. Strongly thickened, even tuberculated, ribs may also appear near the aperture in the macroconchs.

**Remarks.** As mentioned above, the species included in the new genus have traditionally been assigned to the genus *Thurmanniceras* (see lists of synonymy in Klein, 2005). The type species of this genus (*T. thurmanni*) was defined by Pictet and Campiche (1860) on heterogeneous and poorly preserved material, which, together with a strongly idealized original iconography, considerably hampered the subsequent interpretation of the genus.

The lectotype of *T. thurmanni* (in Pictet and Campiche, 1860, pl. 34, fig. 1a, b; designated by Baumberger 1906), of which we have examined casts and photographs, is a fragment corresponding to half a whorl with a diameter close to 118 mm. At this stage, the whorl section is ovate, with moderately convex flanks, truncated venter, and sharp ventrolateral shoulders. The ornamentation consists of weakly falcoid ribs, which arise singly in a barely perceptible umbilical thickening and divide towards the middle of the flank into two ribs that exhibit a small, but distinct, ventrolateral tubercle, and cross the venter without hardly losing relief. Some additional bifurcated and intercalatory ribs also occur sporadically in the upper part of the flank.

From our perspective, the differences in shell shape and ornamentation pattern are sufficiently diagnostic to justify the exclusion of *H. pertransiens* and its close relatives from the genus *Thurmanniceras*, whose content would be restricted to the type species.

**Stratigraphic and geographic distribution.** Uppermost Berriasian (*Tirnovella alpillensis Zone*, *H. otopeta Subzone*) and lowermost Valanginian (*H. pertransiens Zone*) from the Western Tethys (Mediterranean Province and Mexico; see “Criteria for the Global Correlation of the Berriasian/Valanginian Boundary”, part “Ammonites”).

# Appendix 2. Taxonomic index

Alphabetic list of the taxa mentioned in the text and figures.

* Ammonites

* *Berriasella calisto* (Orbigny, 1850)

* *Berriasella picteti* (Kilian, 1906)

* *Berriasella* Uhlig, 1905

* *Bochianites neocomiensis* (Orbigny, 1842)

* Bochianitidae Spath, 1922

* *Clavithurmannia foraticostata* Thieuloy, 1979

* *Delphinites* (*Delphinites*) *ritteri* Sayn, 1901

* *Delphinites* (*Pseudogarnieria*) Spath, 1923

* *Erdenella paquieri* (Simionescu, 1899)

* *Fauriella boissieri* (Pictet, 1867)

* *Groebericeras bifrons* Leanza, 1945

* Haploceratidae Zittel, 1884

* *Hoedemaekeria* (nov. gen.) Company & Reboulet (this paper; see Appendix 1, Taxonomic note)

* *Hoedemaekeria* (nov. gen.) *gratianopolitensis* (Sayn, 1907)

* *Hoedemaekeria* (nov. gen.) *otopeta* (Thieuloy, 1979)

* *Hoedemaekeria* (nov. gen.) *pertransiens* (Sayn, 1907)

* *Holcophylloceras silesiacum* (Oppel, 1865)

* *Holcoptychites agrioensis* (Weaver, 1931)

* *Karakaschiceras inostranzewi* (Karakasch, 1889)

* *Kilianella* Uhlig, 1905

* *Kilianella asiatica* Spath, 1939

* *Kilianella chamalocensis* Mazenot, 1939

* *Kilianella crassiplicata* (Stanton, 1896)

* *Kilianella drumensis* (Breistroffer, 1937)

* *Kilianella lucensis* (Sayn, 1907)

* *Kilianella pexiptycha* (Uhlig, 1882)

* *Kilianella roubaudiana* (Orbigny, 1850)

* *Kilianiceras* Djanélidzé, 1922
Leptoceras Uhlig, 1883
Leptoceras studeri (Ooster, 1860)
Lytoceras Suess, 1865
Lytoceras honnoratianum (Orbigny, 1841)
Lytoceras quadrisulcatum (Orbigny, 1841)
Lytoceratidae Neumayr, 1875
Neocomites neocomiensiformis (Uhlig, 1902)
Neocomites premolicus Sayn, 1907
Neocomites wichmanni Leanza, 1945
Neocomitidae Salfeld, 1921
Neolissoceras (Neolissoceras) Spath, 1923
Neolissoceras (Neolissoceras) grasianum (Orbigny, 1841)
Neolissoceras (Vergoliceras) Atrops & Reboulet, 1996
Neolissoceras (Vergoliceras) extracornutum (Cecca, 1995)
Neolissoceras (Vergoliceras) salinarium (Uhlig, 1888)
Olcostephanidae Pavlow, 1892
Olcostephanus Neumayr, 1975
Olcostephanus laticosta (Gerth, 1925)
Olcostephanus drumensis Kilian, 1910
Olcostephanus (Jeannoticeras) Thieuloy, 1965
Olcostephanus (Jeannoticeras) jeannoti (Orbigny, 1841)
Paratollia Casey, 1973
Phylloceras (Hypophylloceras) tethys (Orbigny, 1841)
Phylloceratidae Zittel, 1884
Platylenticeras Hyatt, 1900
Platylenticeras heteropleurum occidentale (Sayn, 1901)
Platylenticeras latum tenue Koenen, 1915
Protancyloceras Spath, 1924
Protancyloceras punicum Arnould-Saget, 1953
Protancyloceratidae Breistroffer, 1947
Ptychophylloceras (Semisulcatoceras) semisulcatum (Orbigny, 1841)
Sarasinella Uhlig, 1905
Sarasinella ambigua (Uhlig, 1902)
Sarasinella eucyrta (Sayn, 1907)
Sarasinella longi (Sayn, 1907)
Sarasinella subspinosa (Uhlig, 1910)
Sarasinella trezanensis (Sayn, 1907)
Sarasinella uhligi Spath, 1939
Sarasinella varians (Uhlig, 1910)
Spiticeras Uhlig, 1903
Spiticeras gevreyi Djanélidzé, 1922
Spiticeras multiforme Djanélidzé, 1922
Spiticeras polytroptychum (Uhlig, 1888)
Thurmanniceras Cossmann, 1901
Thurmanniceras thurmanni (Pictet & Campiche, 1860)
Tirnovella alpillensis (Mazenot, 1939)

## Belemnites

Adiakritobelus Janssen & Fözy, 2004
Berriasibelus Delattre, 1952
Berriasibelus conicus (Blainville, 1827)
Berriasibelus exstinctorius (Raspail, 1829)
Berriasibelus aff. exstinctorius (Raspail, 1829) sensu Janssen, 2021
Berriasibelus incertus (Weis, 1991)
Berriasibelus kabanovi (Weis, 1991)
Berriasibelus triquetrus (Weiss, 1991)

Castellanibelus Combémorel, 1972
Castellanibelus orbignyanus (Duval-Jouve, 1841)
Castellanibelus sp. E (sensu Janssen, 2021)
Conobelus piradoensis Janssen, 2003
Curtohibolites Stoyanova-Vergilova, 1963
Duvalia Bayle, 1878
Duvalia lata constricta Stoyanova-Vergilova, 1965
Duvalia lata lata (Blainville, 1827)
Duvalia miravetesensis Janssen, 2003
Duvalia superconstricta Janssen, 2018
Duvalia tornajoensis Janssen, 2003
Gillieronibelus mayeri (Gilliéron, 1873)
Hibolites (sensu Blainville, 1827, non Hibolithes Denys de Montfort, 1808)
Hibolites aff. pistilliformis (Blainville, 1827) sensu Janssen, 2021
Mirabelobelus Janssen & Clément, 2002
Mirabelobelus blanvillei Janssen & Clément, 2002
Pseudobelus Blainville, 1827
Pseudobelus bipartitus Blainville, 1827
Tithonobelus Janssen, 2022
Tithonobelus orbignyi (Janssen & Clément, 2002)

## Calpionellids

Borzaites atava (Grün & Blau, 1996)
Calpionella alpina Lorenz, 1902
Calpionella elliptica Cadish, 1932
Calpionella minuta Houša, 1990
Calpionellites Colom, 1948
Calpionellites allemanni Řehánek, 1988
Calpionellites caravacaensis Allemann in Allemann & Trejo, 1975
Calpionellites coronatus Trejo in Allemann & Trejo, 1975
Calpionellites darderi (Colom, 1934)
Calpionellites major Colom, 1948
Calpionellites uncinatus Cita & Pasquaré, 1959
Calpionellopsis Colom, 1948
Calpionellopsis oblonga (Cadish, 1932)
Calpionellopsis simplex (Colom, 1939)
Crassicollaria parvula Remane, 1962
Lorenziella hungarica Knauer & Nagy, 1964
Lorenziella plicata Remane in Le Hégarat & Remane, 1968
Praecalpionellites Pop, 1986
Praecalpionellites hillebrandti Grün & Blau, 1999
Praecalpionellites murgeanui (Pop, 1974)
Praecalpionellites siriniaensis Pop, 1986
Remaniella Catalano, 1965
Remaniella borzai Pop, 1994
Remaniella cadischiana (Colom, 1948)
Remaniella catalanoui Pop, 1996
Remaniella colomi Pop, 1996
Remaniella filipescui Pop, 1994
Sturiella dolomitica (Grün & Blau, 1996)
Tintinnopsella carpathica (Murgeanu & Filipescu, 1933)
Tintinnopsella dacica Filipescu & Dragastan, 1970
Tintinnopsella doliphormis (Colom, 1939)
Tintinnopsella longa (Colom, 1939)
Tintinnopsella subacuta (Colom, 1948)
## Calcareous dinoflagellate cysts

Cadosina minuta Borza, 1980 – note: This taxon should be transferred to the Acritarchs (Granier, 2024). This author introduces a new genus and a new species, namely *Octahedronoides tethysianus*. According to Daniela Reháková and Stan Duxbury, further investigations are needed before making any changes.

* Cadosina semiradiata fusca Wanner, 1940

* Cadosina semiradiata cieszynica (Nowak, 1968)

* Cadosina semiradiata olzae (Nowak, 1966)

* Cadosina semiradiata semiradiata Wanner, 1940

* Cadosinopsis nowakii Borza, 1984

* Carpistomiosphaera valanginiana Borza, 1986

* Colomisphaera carpathica (Borza, 1964)

* Colomisphaera conferta Řehánek, 1985

* Colomisphaera fortis Řehánek, 1982

* Colomisphaera heliosphaera (Vogler, 1941)

* Colomisphaera lapidosa (Vogler, 1941)

* Colomisphaera lucida Borza, 1986

* Colomisphaera vogleri (Borza, 1969)

* Parastomiosphaera malmica Borza, 1964

* Stomiosphaera echinata Nowak, 1968

* Stomiosphaera moluccana Wanner, 1940

* Stomiosphaera wanneri Borza, 1969

* Stomiosphaerina proxima Řehánek, 1987

## Organic-walled dinoflagellate cysts

* Aprobolocysta humilis Duxbury, 2024

* Aprobolocysta pustulosa Smith & Harding, 2004

* Batioladinium reticulatum Stover & Helby, 1987

* Bicornus obscurus Duxbury 2024

* Biorbifera johnewingii Habib, 1972

* Bourkidinium granulatum Morgan, 1975

* Cauca maculosa Duxbury, 2018

* Chlamydophorella Cookson & Eisenack, 1958

* Chlamydophorella caminus Duxbury, 2024

* Circulodinium hirtellum Alberti, 1961

* Cribroperidinium Neale & Sarjeant, 1962

* Cribroperidinium orthoceras (Eisenack, 1958) Davey 1969

* Ctenidodinium elegantulum Millioud, 1969

* Cymososphaeridium validum Davey, 1982

* Dapsilodinium deflandrei (Valensi, 1947) Lentin & Williams, 1981

* Dapsilodinium warrenii (Habib, 1976) Lentin & Williams, 1981

* Diacanthum hollisteri Habib, 1972

* Dingodinium spinosum (Duxbury, 1977) Davey, 1979

* Downiesphaeridium flexuosum (Davey et al. 1966) Islam 1993

* Druggidium apicopaucicum Habib, 1973

* Egmontodinium toryna (Cookson & Eisenack, 1960) Davey, 1979

* Exiguisphaera asketa Duxbury, 2018

* Exiguisphaera phragma Duxbury, 1979

* Exochosphaeridium robustum Backhouse, 1988

* Foucheria modesta Monteil, 1992

* Heslertonia inferior Duxbury, 2024

* Hystrichodinium pulchrum Deflandre, 1935

* Hystrichodinium voigtii (Alberti, 1961) Davey, 1974

* Hystrichosphaeridium diversum Duxbury, 2018

* Hystrichosphaerina schindewolfii Alberti, 1961

* Impletosphaeridium tribuliferum (Sarjeant 1962) Islam 1993

* Kleithriasphaeridium fasciatum (Davey & Williams, 1966) Davey, 1974

* Kleithriasphaeridium simplicispinum (Davey & Williams, 1966) Davey, 1974

* Muderongia Cookson & Eisenack, 1958

* Muderongia dedecosa (Gocht, 1957) Duxbury, 2023

* Muderongia extensiva Duxbury, 1977

* Muderongia mcwhaei Cookson & Eisenack, 1958

* Muderongia simplex Alberti, 1961

* Paragonyaulacysta borealis Brideaux & Fisher, 1976

* Perisseiasphaeridium cretaceum Duxbury, 2018

* Phoberocysta Millioud, 1969

* Phoberocysta latissima Duxbury, 2024

* Phoberocysta neocomica (Gocht, 1957) Millioud, 1969

* Prolixosphaeridium prolatum Duxbury, 2024

* Protoellipsodinium seghire subsp. medaure Below, 1981

* Protoellipsodinium touile mugatae Below, 1981

* Pseudoceratium pelliferum subsp. pelliferum Gocht, 1957

* Pseudoceratium pelliferum subsp. radiculatum (Gocht, 1957) Duxbury, 2024

* Scriniodinium pharo (Duxbury) Davey, 1982

* Sentusidinium cuculliforme Davies, 1983*Spiculodinium? inordinatum* Duxbury, 2024

* Spiniferites Mantell, 1850

* Systematophora areolata Klement in Davey, 1982

* Systematophora sp. A Monteil, 1993

* Systematophora? daveyi Riding & Thomas, 1988

* Systematophora? scoriacea (Raynaud, 1978) Monteil, 1992

* Tanyosphaeridium hirsutum Duxbury 2024

* Tanyosphaeridium magneticum Davies, 1983

* Tanyosphaeridium cf. variecalamum Davey & Williams, 1966

* Thalassiphora? charollaisii Monteil, in press

* Vexillocysta spinosa Duxbury, 2018

* Wallodinium lunum (Cookson & Eisenack, 1960) Lentin & Williams, 1973

* Wrevittia helicoidea (Eisenack & Cookson, 1960) Helenes & Lucas-Clark, 1997

## Miospores

* Appendicisporites Weyland & Krieger, 1953

* Callialasporites dampieri (Balme, 1957) Dev, 1961

* Callialasporites trilobatus (Balme, 1957) Dev, 1961

* Cicatricosisporites Potonié & Gelletich, 1933

* Classopollis torosus Burger, 1965

* Concavissimisporites variverrucatus Brenner 1963

* Cyathidites Couper, 1953

* Foveosporites subtriangularis Kemp, 1970

* Gleichenidites senonicus Ross, 1949

* Lycopodiumsporites austroclavatidites (Cookson, 1953) Potonié, 1956

* Monosulcites Cookson ex Cooper, 1953

* Pilosisporites trichopapillosus (Thiergart, 1949) Delcuort & Spru mont, 1955

* Sestrosporites pseudoalveolatus (Couper, 1958) Dettmann, 1963

* Staplinisporites caminus (Balme, 1957) Pocock, 1962

* Trilobosporites bernissartensis (Delcuort & Sprumont 1955) Potonié, 1956

* Vitreisporites pallidus (Reissinger, 1950) Nilsson, 1958
## Acritarchs

* Cyclopsiella Drugg & Loeblich, 1967

* Halophoridia caperata (Srivastava 1984) Duxbury, 2024

* Micrhystridium Deflandre, 1939

* Pterospermella Eisenack, 1972

* Rhombodella cf. vesca Duxbury, 1980

* Tasmanites Newton, 1875

## Calcareous nannofossils

* Anfractus harrisonii (Medd, 1979)

* Assipetra infracetacea (Thierstein, 1973) Roth, 1973

* Axopodorhabdus dietzmannii Reinhardt, 1965

* Biscutum constans (Górka, 1957) Black in Black & Barnes, 1959

* Biscutum ellipticum (Gorka, 1957) Grün in Grün & Allemann, 1975.

* Calcicalathina Thierstein, 1971

* Calcicalathina erbae Bergen, 2000

* Calcicalathina oblongata (Worsley, 1971) Thierstein, 1971

* Calcicalathina praeoblongata Aguado in Aguado et al., 2000

* Conusphaera mexicana subsp. mexicana (Trejo, 1969)

* Conusphaera mexicana subsp. minor Bown & Cooper, 1989

* Conusphaera rothii (Thierstein, 1971) Jakubowski, 1986

* Cretarhabdus angustiforatus (Black, 1971) Bukry 1973, emended
Bralower et al., 1989

* Cretarhabdus conicus Bramlette & Martini, 1964

* Cretarhabdus inaequalis Crux, 1987

* Cretarhabdus aff. striatus (Stradner, 1963) Black, 1973

* Crucibiscutum salebrosum (Black, 1971) Jakubowski, 1986

* Cruciellipsis cuvillieri (Manivit, 1966) Thierstein, 1971

* Cyclagelosphaera margerelii Noël, 1965

* Diadorhombus rectus Worsley, 1971

* Diazomatolithus lehmanii Noël, 1965

* Diazomatolithus subbeticus Grün, 1975

* Discorhabdus ignotus (Górka, 1957) Perch-Nielsen, 1968

* Discorhabdus rotatorius (Bukry, 1969) Thierstein, 1973

* Eiffellithus windii Applegate & Bergen, 1988

* Ethmorhabdus hauterivianus (Black, 1971) Applegate et al. in
Covington & Wise, 1987

* Haqius circumradiatus (Stover, 1966) Roth, 1978.

* Haqius ellipticus (Grün in Grün & Allemann, 1975), Bown, 2005

* Helenea chiastia Worsley, 1971

* Helenea quadrata (Worsley, 1971) Rutledge & Bown in Bown et al., 1998

* Kokia curvata Perch-Nielsen, 1988

* Manivitella pemmatoidea (Deflandre in Manivit, 1965) Thierstein, 1971

* Micrantholithus hoschulzii (Reinhardt, 1966) Thierstein, 1971

* Micrantholithus obtusus Stradner, 1963

* Micrantholithus speetonensis Perch-Nielsen, 1979

* Nannoconus bermudezii Brönnimann, 1955

* Nannoconus broennimanni Trejo, 1959

* Nannoconus bucheri Brönnimann, 1955

* Nannoconus colomi Kamptner, 1938

* Nannoconus dolomiticus Cita & Pasquaré, 1959

* Nannoconus globulus subsp. globulus Brönnimann, 1955

* Nannoconus globulus subsp. minor (Brönnimann, 1955) Bralower in
Bralower et al., 1989

* Nannoconus inornatus Rutledge & Bown, 1996

* Nannoconus Kamptner, 1931

* Nannoconus kamptneri subsp. kamptneri Brönnimann, 1955

* Nannoconus kamptneri subsp. minor (Brönnimann, 1955) Bralower in
Bralower et al., 1989

* Nannoconus oviformis Perch-Nielsen, 1988

* Nannoconus quadratus (Noël 1959) Deres & Achéritéguy 1980

* Nannoconus steinmannii subsp. minor (Kamptner, 1931) Deres &
Achéritéguy, 1980

* Nannoconus steinmannii subsp. steinmannii Kamptner, 1931

* Nannoconus wintereri Bralower & Thierstein, 1989

* Percivalia fenestrata (Worsley, 1971) Wise, 1983

* Percivalia nebulosa (Bralower in Bralower et al., 1989) Aguado in
Aguado et al. 2000

* Polycostella senaria Thierstein, 1971

* Retecapsa octofenestrata Bralower in Bralower et al., 1989

* Retecapsa surirella (Deflandre & Fert, 1954) Grün in Grün & Allemann, 1975

* Rhagodiscus asper (Stradner, 1963) Reinhardt, 1967

* Rhagodiscus dekaenelii Bergen, 1994

* Rhagodiscus gallagheri (Rutledge & Bown, 1996)

* Rhagodiscus nebulosus Bralower in Bralower et al., 1989

* Rhagodiscus pseudoangustus (Crux, 1987)

* Rotelapillus laffittei (Noël, 1957) Noël, 1973

* Rucinolithus wisei Thierstein, 1971

* Sollasites arcuatus Black, 1971

* Sollasites horticus (Stradner et al. in Stradner & Adamiker, 1966)
Cepek & Hay, 1969

* Speetonia colligata Black, 1971

* Staurolithites crux (Deflandre & Fert, 1954) Caratini, 1963

* Staurolithites laffittei Caratini, 1963

* Staurolithites mutterlosei Crux, 1989

* Triquetrorhabdulus shetlandensis Perch-Nielsen, 1988

* Tubodiscus frankiae Bown, 2005

* Tubodiscus jurapelagicus (Worsley, 1971) Roth, 1973

* Tubodiscus verenae Thierstein, 1973

* Umbria granulosa Bralower & Thierstein in Bralower et al., 1989

* Watznaueria Reinhardt, 1964

* Watznaueria barnesiae (Black in Black & Barnes, 1959)
Perch-Nielsen, 1968

* Watznaueria biporta (Bukry, 1969)

* Watznaueria britannica (Stradner, 1963) Reinhardt, 1964

* Watznaueria communis Reinhardt, 1964

* Watznaueria cynthae Worsley, 1971

* Watznaueria fossacincta (Black, 1971) Bown in Bown & Cooper, 1989.

* Watznaueria manivitae Bukry 1973

* Watznaueria ovata Bukry, 1969

* Zeugrhabdotus diplogrammus (Deflandre in Deflandre & Fert,
1954) Burnett in Gale et al., 1996

* Zeugrhabdotus elegans (Gartner 1968) Burnett in Gale et al., 1996

* Zeugrhabdotus embergeri (Noël, 1958) Perch-Nielsen, 1984

* Zeugrhabdotus erectus (Deflandre in Deflandre & Fert, 1954)
Reinhardt, 1965

* Zeugrhabdotus fissus Grün & Zweili, 1980

* Zeugrhabdotus trivectis Bergen, 1994

* Zygolithus xenotus Stover, 1966

## Ichnofossils

* Zoophycos Massalongo, 1855