Ammonite biostratigraphy of the uppermost Hauterivian in the Betic Cordillera (SE Spain)

Ammonite biostratigraphy of the uppermost Hauterivianin the Betic Cordillera (SE Spain)

Biostratigraphie d’ammonites de l’Hauterivien terminaldans la Cordillère Bétique (sud-est de l’Espagne)

Miguel Company *, José Sandoval, José M. Tavera

Departamento de Estratigrafía y Paleontología, Facultad de Ciencias, Universidad de Granada, 18002 Granada, Spain

Received 2 October 2002; accepted 23 December 2002

Abstract

A detailed analysis of the stratigraphic distribution of ammonites from fourteen sections in the External Zones of the Betic Cordillera hasenabled us to identify accurately the sequence of bioevents that take place throughout the uppermost Hauterivian and to propose a more precisebiostratigraphic scheme for this interval. Thus, we have divided the two currently admitted zones (the Crioceratites balearis Zone and thePseudothurmannia angulicostata auct. Zone) into several subzones. Four subzones can be recognised within the Cr. balearis Zone. The baseof each subzone is defined by the first occurrence of one of four successive species belonging to the same Crioceratites lineage. These speciesare: Cr. balearis, Cr. binelli, Cr. krenkeli and Cr. angulicostatus. The Ps. ohmi Zone (which replaces the classical Ps. angulicostata Zone) canbe divided into three subzones characterised by three successive species of the genus Pseudothurmannia: Ps. ohmi, Ps mortilleti (hereconsidered as a senior synonym of Ps. catulloi) and Ps. picteti. According to the current definition, the first occurrence of Taveraidiscus hugii(OOSTER) marks the lower boundary of the Barremian stage. This event fits into a major faunal-renewal episode that begins in the upper partof the Ps. picteti Subzone.

© 2003 Éditions scientifiques et médicales Elsevier SAS. All rights reserved.

Résumé

L’analyse détaillée de la distribution stratigraphique des ammonites dans quatorze coupes localisées dans les Zones Externes de laCordillère Bétique nous a permis d’identifier avec précision la séquence des bioévénements qui ont eu lieu durant l’Hauterivien sommital etde proposer un schéma zonal précis pour cet intervalle. Ainsi, nous avons divisé les deux zones actuellement admises (Zone à Crioceratitesbalearis et Zone à Pseudothurmannia angulicostata auct.) en plusieurs sous-zones. Quatre sous-zones ont pu être reconnues dans la Zone à Cr.balearis. La base de chaque sous-zone est définie par la première apparition de l’une des quatre successives espèces appartenant à la mêmelignée crioceratitique. Ces espèces sont : Cr. balearis, Cr. binelli, Cr. krenkeli et Cr. angulicostatus. La Zone à Ps. ohmi (qui vient remplacerla Zone classique à Ps. angulicostata) peut être subdivisée en trois sous-zones caractérisées par trois espèces successives du genrePseudothurmannia : Ps. ohmi, Ps. mortilleti (considérée ici comme synonyme de Ps. catulloi) et Ps. picteti. D’après la définitionactuellement admise, la première apparition de Taveraidiscus hugii (OOSTER) marque la limite inférieure de l’étage Barremien. Cetévénement coïncide avec un épisode de renouvellement faunique important qui débute dans la partie supérieure de la sous-zone à Ps. picteti.

© 2003 Éditions scientifiques et médicales Elsevier SAS. All rights reserved.

Keywords: Ammonoids; Upper Hauterivian; Zonation; Mediterranean Province

Mots clés : Ammonites ; Hauterivien supérieur ; Zonation ; Province Méditerranéenne

* Corresponding author.E-mail address: [email protected] (M. Company).

Geobios 36 (2003) 685–694

www.elsevier.com/locate/geobio

© 2003 Éditions scientifiques et médicales Elsevier SAS. All rights reserved.doi:10.1016/j.geobios.2002.12.001

1. Introduction

In the current standard zonation for the Mediterraneanregion (Hoedemaeker and Rawson, 2000), the uppermostHauterivian interval is represented by the Crioceratites bale-aris Zone and the Pseudothurmannia angulicostata auct.Zone. These two units, introduced by Busnardo (1984) in hiszonation for the Lower Cretaceous of southeastern France,were adopted by the Lower Cretaceous Cephalopod Team inits first zonal scale formulated at the Digne Workshop (Hoe-demaeker and Bulot, 1990). The Ps. angulicostata auct.Zone was later, at the proposal of Ph. Hoedemaeker duringthe Mula Workshop (Hoedemaeker and Company, 1993),divided into two subzones: a lower Ps. ohmi Subzone and anupper Ps. catulloi. This disposition has been retained un-changed in the zonations subsequently proposed by theworking group.

The excessive simplicity of this scheme contrasts with thehigh resolution attained by some of the zonations recentlyproposed for other Lower Cretaceous intervals (see Kleinand Hoedemaeker, 1999). To solve this deficiency, moredetailed analyses of the ammonite distribution in the upper-most Hauterivian were needed in order to identify accuratelythe sequence of bioevents and to enable the construction of amore precise zonation for this interval. To this end, weundertook bed-by-bed sampling of several sections locatedin different palaeogeographic domains of the Betic Cordil-lera (Fig. 1). These sections are:

• Barranco de la Aguzadera (La Guardia, Jaén): sectionsX.G and X.G1.

• Ermita de Cuadros (Bedmar, Jaén): section X.EC.• Río Argos (Caravaca, Murcia): sections X.Ag1 (= sec-

tion A in Hoedemaeker, 1995) (Fig. 2), X.Ag4 andX.Ag5.

• Barranco de Cavila (Caravaca, Murcia): section X.Kv3.• Arroyo de Gilico (Cehegín, Murcia): section X.V1

(Fig. 3).• Cerro del Tornajo (Lorca, Murcia): sections X.Tj1 and

X.Tj2.• Sierra del Cid (Petrer, Alicante): sections X.A1 and

X.A2.• Barranco de la Querola (Cocentaina, Alicante): section

X.Q.• Cantera de l’Almuxic (Oliva, Valencia): section X.O.

More than 5000 identifiable ammonites were collectedfrom the interval studied in these sections. The analysis ofspecies distribution has enabled us to divide the two classiczones into several subzones (Fig. 4). Thus, we have recogn-ised four subzones in the Cr. balearis Zone and three sub-zones in the Ps. ohmi Zone (= Ps. angulicostata auct. Zone).All of these are interval subzones, the lower boundary ofwhich is defined by the first occurrence of the index species,the upper boundary coinciding with the base of the next unit.Although the zonal scheme presented here is proposed onlyfor the Betic Cordillera, its constituent units can be easily

Fig. 1. Geographical and geological location of the studied sections.Fig. 1. Localisation géographique et géologique des coupes étudiées.

686 M. Company et al. / Geobios 36 (2003) 685–694

Fig. 2. Río Argos-1 section (X.Ag1). Lithological succession and ammonite distribution.Fig. 2. Coupe de Río Argos 1 (X.Ag1). Succession lithologique et distribution des ammonites.

687M. Company et al. / Geobios 36 (2003) 685–694

recognised in many other parts of the Mediterranean area. Apreview of these results was presented by Aguado et al.(2001).

2. Zonation

2.1. Crioceratites balearis Zone

This unit was introduced, without formal definition, byBusnardo (1984) and later defined by Hoedemaeker and

Leereveld (1995) as the biostratigraphic interval between thefirst occurrence of Cr. balearis (NOLAN) and the first occur-rence of Ps. ohmi (WINKLER). Four subzones, defined bythe consecutive appearances of four different chronospeciesbelonging to the same Crioceratites lineage, can be recogn-ised within this zone. These species are: Cr. balearis(Fig. 5(1–3)), Cr. binelli (ASTIER) (Fig. 5(4)), Cr. krenkeli(SARKAR) (Fig. 5(6–8)) and Cr. angulicostatus(D’ORBIGNY) (Fig. 5(9–10)). They correspond to four suc-cessive steps in what appears to be an evolutionary trend

Fig. 3. Arroyo Gilico section (X.V1). Lithological succession and ammonite distribution.Fig. 3. Coupe de Arroyo Gilico (X.V1). Succession lithologique et distribution des ammonites.


towards a stronger ornamentation and a clearer differentia-tion between main and intermediate ribs in the middle onto-genetic stages. In addition to these forms, we have foundspecimens attributable to Cr. majoricensis (NOLAN)(Fig. 5(5)), which probably represent morphotypes of thesame lineage showing a more prolonged trituberculate stage(trituberculate ribs can be present in the innermost whorls ofall members of the group).

Together with the genus Crioceratites, the faunal assem-blage from this zone is composed mainly of long-rangingspecies such as Plesiospitidiscus subdiffıcilis (KARAK-ASCH) (Fig. 6(3)), Abrytusites neumayri (HAUG), Neolis-soceras subgrasianum (DRUSHCHITS), Lytoceras subfim-briatum (D’ORBIGNY), Phylloceras thetys (D’ORBI-GNY), Phyllopachyceras infundibulum (D’ORBIGNY) andPhyllopachyceras winkleri (UHLIG).

2.1.1. Cr. balearis SubzoneCr. balearis is the first member of the lineage. Its orna-

mentation in the middle stages consists of uniform and denseribs lacking distinct umbilical tubercles. The fauna in thisinterval is scarce and shows low diversity. The last specimensof Discoidellia couratieri VERMEULEN occur at the base

of this subzone, whereas the first Paraspiticeras appear in itsupper part.

2.1.2. Cr. binelli SubzoneThe next species of the group, Cr. binelli, differs from Cr.

balearis in the appearance of rib bundles rising from well-defined umbilical bullae. The faunal assemblages from thissubzone are still poorly diversified and numerically domi-nated by the index species and Pl. ligatus.

2.1.3. Cr. krenkeli SubzoneCr. krenkeli shows a clear differentiation between main

and intermediate ribs from quite early ontogenetic stages. Inthis subzone, the fauna is more abundant and diversified thanin the previous ones. Discoidellia vermeuleni CECCA,FARAONI and MARINI and the first representatives of thegenus Anahamulina, attributable to An. jourdani (ASTIERsensu OOSTER), appear together with the index species atthe base of this interval.

2.1.4. Cr. angulicostatus SubzoneAs is well known (Sarkar, 1955; Hoedemaeker, 1995), the

species Ammonites angulicostatus D’ORBIGNY has been

Fig. 4. Proposed zonation and ranges of the most significant ammonite species.Fig. 4. Zonation proposée et distribution stratigraphique des principales espèces d’ammonites.



misinterpreted by most authors. After having analysed a castof the holotype, we are convinced, in agreement with Hoede-maeker (1995), that this taxon should be placed among theCrioceratites species. Cr. angulicostatus would then be thelast member of the lineage that begins with Cr. balearis andthe ancestor of the forms currently included in the genusPseudothurmannia (see taxonomic note below).

The first Emericiceras and Acrioceras, respectively repre-sented by Em. thiollierei (ASTIER) and Ac. meriani(OOSTER) (Fig. 5(11)), also appear in this subzone. Thesetwo nominal species may be no more than the two antidimor-phs of a single biological species.

This stratigraphic interval is very unevenly represented inthe sections studied (compare Figs. 2 and 3), probably be-cause of the slumps, which frequently affect the sediments ofthat age.

2.2. Pseudothurmannia ohmi Zone

We use this unit in the sense of Hoedemaeker and Leerev-eld (1995), who introduced it as a substitute for the ancientPs. angulicostata Zone. According to their interpretation, thePs. ohmi Zone would correspond to the interval comprisedbetween the first occurrence of the index species and thelower boundary of the Barremian stage. This interval ischaracterised by the development of the genus Pseudothur-mannia. It can be divided into three subzones defined by theconsecutive appearances of Ps. ohmi (WINKLER) (Fig. 6(1,2)), Ps. mortilleti (PICTET and DE LORIOL) (Fig. 6(4)) andPs. picteti (SARKAR) (Fig. 6(6, 7)). These three species alsorepresent three successive stages of an evolutionary trendtowards a more involute coiling.

Together with the Pseudothurmannia species, which areby far the main components, the faunal assemblages fromthis zone are composed of heteromorphs, desmoceratids,phylloceratids and other minor groups. Contrary to the datapresented by some authors (Vašícek, 1995; Hoedemaeker,1995; Avram and Melinte, 1998), we have not found Crio-ceratites of the balearis-binelli group coexisting withPseudothurmannia. In this respect, our observations coin-cide with those of Vermeulen (1980), Braga et al. (1982),Autran (1993) and Ropolo (1995). These discrepancies maybe due to differences in taxonomic interpretations.

2.2.1. Pseudothurmannia ohmi SubzoneThe base of this subzone, as already defined by Hoede-

maeker and Leereveld (1995), coincides with the first occur-rence of the index species. Ps. ohmi is the first and moreevolute species of the genus Pseudothurmannia. It differsfrom its ancestor, Cr. angulicostatus, in having the whorlsalways in touch and having definitely lost the initial trituber-culate stage. The fauna from this subzone is very abundantand composed, in addition to the index species, of taxaalready present in lower levels.

2.2.2. Pseudothurmannia mortilleti SubzoneThe lower boundary of this subzone is defined by the first

occurrence of Ps. mortilleti, here considered a senior syn-onym of Ps. catulloi (PARONA). An important faunal re-newal, already pointed out by Hoedemaeker (1995), takesplace around this boundary. Besides the index species, Ps.pseudomalbosi (SARASIN and SCHÖNDELMAYER) (hereconsidered a senior synonym of Ps. sarasini SARKAR)(Fig. 6(5)), Anahamulina subcylindrica (D’ORBIGNY)(Fig. 6(9)), “Barremites” uhligi (HAUG sensu SARASINand SCHÖNDELMAYER), Discoidellia favrei (OOSTER)and Lytoceras densifimbriatum UHLIG also appear at thislevel. At the same time, D. vermeuleni and other long-ranging taxa such as Nl. subgrasianum, L. subfimbriatumand Ph. winkleri disappear.

This faunal turnover coincides with the start of an organic-rich interval that, because of its sedimentologic and palaeon-tologic characteristics, can be considered the equivalent ofthe Faraoni Level, recognised in a similar stratigraphic posi-tion in central and northern Italy and southeastern France(Cecca et al., 1994; Cecca et al., 1996; Baudin et al., 1999).

2.2.3. Pseudothurmannia picteti SubzoneThe base of this subzone is defined by the appearance of

Ps. picteti, the youngest and more involute species of thegenus Pseudothurmannia. Apart from the index species,which is restricted to the lower part of the subzone, the faunafrom this interval is not well characterised. Small and hardlyinterpretable heteromorphs are frequent, among which wehave identified Paraspinoceras morloti (OOSTER)(Fig. 6(8)), a probable senior synonym of Par. evolutus(FALLOT and TERMIER). The first true Barremites, attrib-

Fig. 5. 1. Crioceratites balearis (NOLAN), X.Ag1.131.7, Cr. balearis Subzone. 2. Crioceratites balearis (NOLAN), X.G.6.10, Cr. balearis Subzone. 3.Crioceratites balearis (NOLAN), X.G.6.4, Cr. balearis Subzone. 4. Crioceratites binelli (ASTIER), X.EC.3.1, Cr. binelli Subzone. 5. Crioceratitesmajoricensis (NOLAN), X.EC.4.1, Cr. binelli Subzone. 6. Crioceratites krenkeli (SARKAR), X.G1.2.1, Cr. krenkeli Subzone. 7. Crioceratites krenkeli(SARKAR), X.G1.(5-7).1, Cr. krenkeli Subzone. 8. Crioceratites krenkeli (SARKAR), X.G1.6.1, Cr. krenkeli Subzone. 9. Crioceratites angulicostatus(D’ORBIGNY), X.V1.-2.65, Cr. angulicostatus Subzone. 10. Crioceratites angulicostatus (D’ORBIGNY), X.V1.-4.15, Cr. angulicostatus Subzone. 11.Acrioceras meriani (OOSTER), X.Ag1.145.30, Ps. ohmi Subzone. (All specimens natural size).Fig. 5. 1. Crioceratites balearis (NOLAN), X.Ag1.131.7, Sous-Zone à Cr. balearis. 2. Crioceratites balearis (NOLAN), X.G.6.10, Sous-Zone à Cr. balearis.3. Crioceratites balearis (NOLAN), X.G.6.4, Sous-Zone à Cr. balearis. 4. Crioceratites binelli (ASTIER), X.EC.3.1, Sous-Zone à Cr. binelli. 5. Crioceratitesmajoricensis (NOLAN), X.EC.4.1, Sous-Zone à Cr. binelli. 6. Crioceratites krenkeli (SARKAR), X.G1.2.1, Sous-Zone à Cr. krenkeli. 7. Crioceratites krenkeli(SARKAR), X.G1.(5-7).1, Sous-Zone à Cr. krenkeli. 8. Crioceratites krenkeli (SARKAR), X.G1.6.1, Sous-Zone à Cr. krenkeli. 9. Crioceratites angulicostatus(D’ORBIGNY), X.V1.-2.65, Sous-Zone à Cr. angulicostatus. 10. Crioceratites angulicostatus (D’ORBIGNY), X.V1.-4.15, Sous-Zone à Cr. angulicostatus.11. Acrioceras meriani (OOSTER), X.Ag1.145.30, Sous-Zone à Ps. ohmi. (Tous les échantillons sont figurés en grandeur naturelle).



utable to B. dimboviciorensis BRESKOVSKI, also appear inthis interval. The forms described by Cecca et al. (1998) as B.primitivus, coming from the Faraoni Level, are interpreted byus as a variety of Ps. subdiffıcilis.

2.3. Hauterivian/Barremian boundary

According to the current definition (Rawson, 1996), thefirst occurrence of Taveraidiscus hugii (OOSTER)(Fig. 6(10)) marks the lower boundary of the Barremianstage. This event forms a part of a major faunal renewal thatbegins in the upper part of the Ps. picteti Subzone. Otherspecies such as T. intermedius (D’ORBIGNY) (Fig. 6(11)) –here considered a senior synonym of T. vandeckii (OOSTER)and T. kiliani (PAQUIER) – “Barremites” boutini(MATHERON), Silesites sp., Psilotissotia mazuca (CO-QUAND), Arnaudiella malladae (NICKLÈS) and Hamulin-ites munieri (NICKLÈS) also appear around this level.

Hoedemaeker (1995) argued that the Hauterivian/Barremian boundary should be drawn at the base of hisPs. catulloi Subzone, equivalent to the base of our Ps. mor-tilleti Subzone. This author considered this level to separatean assemblage of reputedly Hauterivian ammonites from anassemblage composed mostly of Barremian species. Never-theless, some of the taxa, which, according to Hoedemaeker,would appear in the Ps. catulloi Subzone, are actuallypresent in lower levels. This is the case of Ab. neumayri andthe genera Paraspiticeras, Emericiceras and Acrioceras.Moreover, Ps. subdiffıcilis is still present throughout the Ps.mortilleti Subzone, being substituted by B. dimboviciorensisin the Ps. picteti Subzone. It is also worth mentioning that theassemblages from the Ps. mortilleti Subzone are composedfor the most part of specimens of Pseudothurmannia (63% ofthe whole) and Plesiospitidiscus and other long-ranging taxainherited from lower levels (12%), giving these assemblagesa marked Hauterivian look.

3. Taxonomic note

On establishing the genus Pseudothurmannia, Spath(1923) designated Am. angulicostatus D’ORBIGNY (in Pic-tet, 1863: Pl. 1bis, Fig. 1) as “genotype”. Sarkar (1955)

however, showed that Pictet’s specimen could not be conspe-cific with Am. angulicostatus D’ORBIGNY and separated itas a new species Ps. picteti SARKAR. Moreover, as shownabove, the species of d’Orbigny is closer to Crioceratitesspecies than to the forms currently included in the genusPseudothurmannia. We believe that Article 70.3 of theI.C.Z.N. is applicable to this case. According to it, and inorder to maintain the usage, we designate Ps. pictetiSARKAR as type species of the genus Pseudothurmannia.

Acknowledgements

We are very grateful to our colleagues Ph. Hoedemaeker(Nationaal Natuurhistorisch Museum, Leiden), G. Schairer(Bayerische Staatssammlung für Paläontologie, Munich) andD. Decrouez (Muséum d’histoire naturelle, Geneva) for hav-ing provided us with casts of the holotypes of Cr. angulicos-tatus, Ps. ohmi and Ps. picteti. Critical comments of F.Atrops and P.F. Rawson are also gratefully appreciated. Thiswork has been co-financed by Project BTE 2001-3020(Spanish Ministry of Science and Technology) and ResearchGroup RNM-178 (Junta de Andalucía).

References

Aguado, R., Company, M., Sandoval, J., Tavera, J.M., 2001. Caracterizaciónbioestratigráfica del límite Hauteriviense-Barremiense en las CordillerasBéticas. Geotemas 3/2, 127–130.

Autran, G., 1993. L’évolution de la marge nord-est provençale (Arc deCastellane) du Valanginien moyen à l’Hauterivien à travers l’analysebiostratigraphique des séries de la région de Peyroules : séries conden-sées, dicontinuités et indices d’une tectogenèse distensive. Paléobiolo-gie. Annales du Muséum d’Histoire naturelle de Nice 10, 1–240.

Avram, E., Melinte, M., 1998. The Hauterivian-Barremian stage boundaryin Svinita area (Banat, SW Romania). Romanian Journal of Stratigraphy77/4, 37–46.

Baudin, F., Bulot, L.G., Cecca, F., Coccioni, R., Gardin, S., Renard, M.,1999. Un équivalent du « Niveau Faraoni » dans le Bassin du Sud-Est dela France, indice possible d’un événement anoxique fini-hauterivienétendu à la Tethys méditerranéenne. Bulletin de la Société géologique deFrance 170, 487–498.

Fig. 6. 1. Pseudothurmannia ohmi (WINKLER), X.Ag5.19.r, Ps. ohmi Subzone. 2. Pseudothurmannia ohmi (WINKLER), X.Ag1.144.39, Ps. ohmi Subzone.3. Plesiospitidiscus subdiffıcilis (KARAKASCH), X.V1.-11.63, Cr. krenkeli Subzone. 4. Pseudothurmannia mortilleti (PICTET and DE LORIOL), X.V1.6.2,Ps. mortilleti Subzone. 5. Pseudothurmannia pseudomalbosi (SARASIN and SCHÖNDELMAYER), X.V1.3a.16, Ps. mortilleti Subzone. 6. Pseudothurman-nia picteti SARKAR., X.V1.10.1, Ps. picteti Subzone. 7. Pseudothurmannia picteti SARKAR., X.G1.20.1, Ps. picteti Subzone. 8. Paraspinoceras morloti(OOSTER), X.V1.13.28, Ps. picteti Subzone. 9. Anahamulina subcylindrica (D’ORBIGNY), X.V1.30.1, T. hugii Zone. 10. Taveraidiscus hugii (OOSTER),X.Ag4.28.104, T. hugii Zone. 11. Taveraidiscus intermedius (D’ORBIGNY), X.Ag4.37.28, T. hugii Zone. (All specimens natural size).Fig. 6. 1. Pseudothurmannia ohmi (WINKLER), X.Ag5.19.r, Sous-Zone à Ps. ohmi. 2. Pseudothurmannia ohmi (WINKLER), X.Ag1.144.39, Sous-Zone à Ps.ohmi. 3. Plesiospitidiscus subdiffıcilis (KARAKASCH), X.V1.-11.63, Sous-Zone à Cr. krenkeli. 4. Pseudothurmannia mortilleti (PICTET and DE LORIOL),X.V1.6.2, Sous-Zone à Ps. mortilleti. 5. Pseudothurmannia pseudomalbosi (SARASIN and SCHÖNDELMAYER), X.V1.3a.16, Sous-Zone à Ps. mortilleti. 6.Pseudothurmannia picteti SARKAR., X.V1.10.1, Sous-Zone à Ps. picteti. 7. Pseudothurmannia picteti SARKAR., X.G1.20.1, Sous-Zone à Ps. picteti. 8.Paraspinoceras morloti (OOSTER), X.V1.13.28, Sous-Zone à Ps. picteti. 9. Anahamulina subcylindrica (D’ORBIGNY), X.V1.30.1, Zone à T. hugii. 10.Taveraidiscus hugii (OOSTER), X.Ag4.28.104, Zone à T. hugii. 11. Taveraidiscus intermedius (D’ORBIGNY), X.Ag4.37.28, Zone à T. hugii. (Tous leséchantillons sont figurés en grandeur naturelle).


Braga, J.C., Company, M., Linares, A., Sandoval, J., Rivas, P., 1982. Con-tribución al conocimiento bioestratigráfico del Hauteriviense-Barremense en la región de Jaén. Cuadernos de Geología ibérica 8,677–689.

Busnardo, R., 1984. Échelles biostratigraphiques. Ammonites. In: Cotil-lon, P. (Ed.), Synthèse géologique du Sud-Est de la France. Crétacéinférieur. Mémoires du Bureau de Recherches géologiques et minières,125, 292–294.

Cecca, F., Marini, A., Pallini, G., Baudin, F., Begouen, V., 1994. A guide-level of the uppermost Hauterivian (Lower Cretaceous) in the pelagicsuccession of Umbria-Marche Apennines (Central Italy): the FaraoniLevel. Rivista italiana di Paleontologia e Stratigrafia 99, 551–568.

Cecca, F., Galeotti, S., Coccioni, R., Erba, E., 1996. The equivalent of the“Faraoni Level” (uppermost Hauterivian, Lower Cretaceous) recorded inthe eastern part of Trento Plateau (Venetian Southern Alps, Italy). Rivistaitaliana di Paleontologia e Stratigrafia 102, 417–424.

Cecca, F., Faraoni, P., Marini, A., 1998. Latest Hauterivian (EarlyCretaceous) ammonites from Umbria-Marche Apennines (Central Italy).Palaeontographia Italica 85, 61–110.

Klein, J., Hoedemaeker, P.J., 1999. Ammonite stratigraphy of the Valangin-ian to Barremian for the Mediterranean region. Scripta geologica spec.Issue 3, 97–127.

Hoedemaeker, P.J., 1995. Ammonite distribution around the Hauterivian-Barremian boundary along the Río Argos (Caravaca, SE Spain). Géolo-gie alpine, Mém. H.S. 20 (1994), 219–277.

Hoedemaeker, P.J., Bulot, L., 1990. Preliminary ammonite zonation for theLower Cretaceous of the Mediterranean region. Géologie alpine 66,123–127.

Hoedemaeker, P.J., Company, M., 1993. Ammonite zonation for the LowerCretaceous of the Mediterranean region; basis for the stratigraphic cor-relations within IGCP-Project 262. Revista española de Paleontología 8,117–120.

Hoedemaeker, P.J., Leereveld, H., 1995. Biostratigraphy and sequencestratigraphy of the Berriasian-lowest Aptian (Lower Cretaceous) of theRío Argos succession, Caravaca, SE Spain. Cretaceous Research 16,195–230.

Hoedemaeker, P.J., Rawson, P.F., 2000. Report on the 5th InternationalWorkshop of the Lower Cretaceous Cephalopod Team (Vienna, 5 Sep-tember 2000). Cretaceous Research 21, 857–860.

Pictet, F.J., 1863. Sur l’enroulement varié de l’Ammonites angulicostatus etsur la limite des genres Ammonites et Crioceras. Mélanges Paléon-tologiques, 1re livraison, 11–14.

Rawson, P.F., 1996. The Barremian stage. Bulletin de l’Institut royal desSciences naturelles de Belgique. Sciences de la Terre (66-supp), 25–30.

Ropolo, P., 1995. Implications of variation in coiling in some Hauterivian(Lower Cretaceous) heteromorph ammonites from the Vocontian basin,France. Memorie descrittive della Carta geologica d’Italia 51, 137–165.

Sarkar, S.S., 1955. Révision des ammonites déroulées du Crétacé inférieurdu Sud-Est de la France. Mémoires de la Société géologique de France,nouv. Série 72, 1–176.

Spath, L.F., 1923. A monograph of the Ammonoidea of the Gault. Part I.Palaeontographical Society, London.

Vašícek, Z., 1995. Lower Cretaceous ammonite biostratigraphy in the West-ern Carpathians (The Czech and Slovac Republics). Géologie alpine,Mém. H.S. 20 (1994), 169–189.

Vermeulen, J., 1980. Étude de la Famille des Pulchelliidae. Révision de troisespèces types du Barrémien du Sud-Est de la France. Thèse Doctorat deSpecialité de l’Université de Nice, pp. 1–92.


Documents

Ammonite biostratigraphy of the uppermost Hauterivian in the Betic Cordillera (SE Spain)