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1 March 2011 Lower Tithonian Microconchiate Simoceratins from Eastern Mexico: Taxonomy, Biostratigraphy, and Palaeobiogeography
Ana B. Villaseñor, Federico Olóriz, Celestina González-Arreola
Author Affiliations +

The precise record of simoceratins sampled bed-by-bed is first reported from Mexico (Mazatepec area in Puebla, central-eastern Mexico), as well as the existence of lappeted peristomes in these ammonites. Both Pseudovolanoceras aesinense and the subspecies Pseudovolanoceras aesinense chignahuapense are shown to occur among Mexican simoceratins. The European species and the Mexican subspecies share the same stratigraphic range in the studied sections, yet they differ in ephebic sculpture. Ecological adaptation to neritic seas corresponding to eastern Mexico areas is interpreted, forcing phenotypic deviation with geographic significance, i.e., subspeciation. The new subspecies would indicate stratigraphic horizons within the Semiformiceras semiforme/Haploceras verruciferum Chronozone in the Mediterranean Tethys. A revision of contemporaneous simoceratins in the Americas is founded on a comparative analysis with respect to the European species P. aesinense.


Upper Jurassic deposits from East-Central Mexico have long been investigated due to their importance for oil exploration. Cantú-Chapa (1967) gave valuable preliminary information about Middle Tithonian to Berriasian ammonites gathered from outcrops in the Mazatepec area, Puebla, Mexico. CantúChapa (1989) proposed a type-section for the Tithonian—Berriasian boundary in the Mazatepec area, and Adatte et al. (1992) provided a precise biostratigraphy for calpionellids, indicating the Jurassic—Cretaceous boundary in the area. On the basis of calpionellid and ammonite biostratigraphy, Stinnesbeck et al. (1993) questioned the previous proposal for the Jurassic/Cretaceous boundary type-section made by CantúChapa (1989). A further approach to sedimentology and diagenesis in Kimmeridgian deposits of the “San Andrés” Formation at Jonotla (Puebla) and Tlacolula (Veracruz), a region which includes the Mazatepec area, was made by Hernández De La Fuente (1996).

Institutional abbreviation.—BSPG, Bayerische Staatssammlung für Paläontologie und Geologie, Munich, Germany; CCS, Material housed in the Museo di Paleontologia del Servizio Geologico d'ltalia, Roma, Italy; GPIBO, Goldfuss-Museum und Paläontologisches Institut der Universität Bonn, Germany; IGM, National Paleontological Collection (Museo Maria Carmen Perrilliat Montoya), Institute of Geology, Mexico City, Mexico; NS3Col, Museo di Paleontologia dell'Università di Roma, Italy; Rin, Collection housed in the Comune di Piobicco, Pesaro, Italy; SMNS, Staatlisches Museum für Naturkunde, Stuttgart, Germany; UNAM, Universidad Nacional Autónoma de México, Mexico; USNM, United States Natural Museum, New York, USA.

Other abbreviations.—Ac, A; Cantú-Chapa collection; C, number of constrictions; CT, Colle Tordina (Monti della Rossa, Appennino Marchigiano), Italy; Dm, measured shell diameter; M, macroconchs; m, microconchs; FAD, first occurrence datum; MTQ, Mazatepec Quesos section in the Apulco River area in Fig. 2; PS, periumbilical sculpture; PS/2, number of periumbilical sculptural elements, ribs, bullae or tubercles, per half-a-whorl; U, umbilical size; U/D, size ratio between the umbilicus and shell diameter; Wh, whorl height; Wh/D, size ratio between whorl height and shell diameter; specimen number a, b, letters refer to mould and cast of the same specimen.

Fig. 1.

Location of the studied sections. A. Regional location for Puebla state. B. Inlet for the precise location of the sections investigated on the banks of the Apulco River in the Mazatepec area.


Geological setting

The geological locality Apulco River section MT-2 lies within the Apulco Valley, Sierra Norte de Puebla, near the village of Mazatepec, Puebla (Figs. 1, 2). This mountainous region belongs to the geologic subprovince of Eastern Sierra Madre (López Ramos 1979a: 291, figs. 6-1, 6–8) and the Mexican Fold-and-Thrust Belt (Suter 1990; a geologic province according to Ortega-Gutiérrez et al. 1992) where NNW—SSE trending folds are interrupted southward by rocks of the Transmexican Volcanic Axis or Belt.

Upper Jurassic outcrops above the Apulco River banks are difficult to access due to dense forest coverage in the area near Mazatepec. The Upper Jurassic section shows a lower, coarse bedded part containing mid-shelf to lower-ramp carbonates (San Andres Formation; Hernández De La Fuente 1996). Overlying it are thinner bedded, brownish to grey-black siltstones with silty interbeds and occasional calcareous horizons showing common, mainly parallel, fine cross lamination (upper Lower Kimmeridgian and Tithonian Tamán Formation; see Cantú-Chapa 1971 for regional biostratigraphy and correlation). Regional deepening is 108° to 308° NE, and common faulting impedes precise lateral observation and correlation among outcrops. Evidence of synsedimentary sliding (slumps) and horizons containing more calcareous concretions are common in the Lower Tithonian succession. Coverage by alluvium (severe flooding during 1999) affects the Tithonian deposits. Cherty intercalations in grayish to darkish and more calcareous clayey limestones characterise the Pimienta Formation (López Ramos 1979b: 315).

The new Apulco section MTQ crops out along the west bank of the Apulco River, close to the hydroelectric station (Figs. 1, 2) and shows a 22 m thick succession made of brownish, more or less calcareous siltstones and silty limestones (Taman Formation) containing decimetre to metre size concretions in the lower and middle part of the section.

Historical background

An overview of Upper Jurassic rocks and palaeoenvironments in the Apulco Valley, located in Sierra Norte de Puebla between Jonotla (Puebla) and Tlacolula (Veracruz), was given by Hernández De La Fuente (1996). In studying fossiliferous sections of the area, this author included some outcrops mentioned by Cantú-Chapa (1971: fig. 1). In his geological locality Apulco River, Hernández De La Fuente (1996) collected Idoceras sp., Mazapilites sp., and Uhligites sp. (without illustration), and mentioned the common occurrence of ammonites within the Tamán Formation.

Over the past ten years, two of us (ABV and FO) have studied outcrops around the Apulco River as part of a research programme focusing on sections of the San Andrés, Tamán, and Pimienta Formations, to provide a precise biostratigraphy based on bed-by-bed sampling (e.g., Villaseñor et al. 2000a, 2003; Villaseñor and Olóriz 2001, 2009; López-Caballero 2006; López-Caballero et al. 2007).

This paper presents the palaeontological analysis carried out on the first specimens of simoceratins collected bed-bybed in Mexico from Lower Tithonian siltstones of the Tamán Formation cropping out along the Apulco River, Mazatepec, Puebla (Figs. 1, 2). The studied material was collected from Apulco section MT-2 (Villaseñor et al. 2003; López-Caballero et al. 2007; Villaseñor and Olóriz 2009) and the new MTQ section.

Fig. 2.

Stratigraphic sections with indication of precise records of Pseudovolanoceras aesinense (Meneghini, 1885) and Pseudovolanoceras aesinense chignahuapense (Cantú-Chapa, 1990) in the Apulco sections MT-2 and MTQ. Note the occurrence of other ammonites significant for biostratigraphy and correlation.


Records of simoceratins from the Americas.—Precise information about the record of Lower Tithonian simoceratins from the Americas is rare, and to date only four specimens have been reported with illustration, aside from some text citations. Krantz (1928) identified the southernmost record, from Argentina, while the other three records were reported by Imlay (1942) from Cuba, and Verma and Westermann (1973), and Cantú-Chapa (1990) from Mexico. Among citations without illustrations, Leanza and Hugo (1977) alluded to Krantz's specimen and reported Simoceras aff. S. volanense Krantz, 1928 non Oppel (1863) from the same section or area studied by Krantz (1928); Leanza and Zeiss (1990, 1992, 1994) and Parent and Capello (1999) cited the occurrence of Simoceras in the Neuquen Basin, Argentina; Leanza (in Leanza and Zeiss 1990) cited Volanoceras from the same locality, and Parent (2001) and Parent et al. (2006) mentioned Volanoceras krantzense Cantú-Chapa, 1990. The mention without illustration made by Krantz (1928) of a geographically intermediate record of Simoceras in Peru (Welter 1913 in Krantz 1928: 13) was not taken into account in later revisions of simoceratins, and was unavailable for control. Based on the descriptions provided by all these authors, the following additional comments concern the interpretations made below.

Krantz (1928: pl. 3: 7) described Simoceras aff. volanense Oppel, 1863 from his locality 30 (surroundings of Barda Blanca, Argentina). The specimen was collected from clayey marls of the Middle Tithonian, together with Aspidoceras (Pseudhimalayites) steinmanni Haupt, 1907 and Pseudolissoceras zitteli Burckhardt, 1903, among other ammonites. Basically, Krantz (1928: 13–14) described his specimen of 85 mm in diameter as an extremely evolute and strongly sculptured form. In the outer whorl, radial periumbilical tubercles are connected by ribs with peripheral ones elongated towards the aperture. The beginning of the outer row of tubercles in the third whorl precedes that of the periumbilical tubercles. Krantz (1928) recognised differences between the Argentinean specimen and the European Simoceras volanense Oppel, 1863 (in Zittel 1870), namely the absence of the constrictions described by Zittel (1870), although he noted some more excavated inter-rib spaces in the Argentinean specimen. Krantz (1928) distinguished his specimen from Simoceras schwertschlageri Schneid, 1915 on the basis of its stronger, more radial sculpture. Later interpretations of this specimen include those of Santantonio (1986), Cecca (1999: 22) and Carlo Sarti in personal communication to Parent and Capello (1999), who reinterpret the Argentinean specimen as Simoceras aesinense (Meneghini, 1885); Fözy (1988) raises doubts about the species- and even genus-level meaning; Cantú-Chapa (1990) put forth the species Volanoceras krantzense CantúChapa, 1990, a proposal followed by Parent (2001), Cecca (2002a), who considered Simoceras (Pseudovolanoceras) krantzense Cantú-Chapa, 1990 a genuine species after examination of a gypsum cast, Schweigert et al. (2002) and Parent et al. (2006); and Villaseñor et al. (2000b) foresee the possibility of revealing a local subspecies of S. aesinense (Meneghini, 1885) (see below).

Imlay (1942: pl. 3: 2–3) described Simoceras sp. juv. cf. volanense (Oppel, 1863) from the Viñales Limestone in the northeastern slope of Loma Sabanilla, Santa Clara Province, north-central Cuba, locality 268 of the Atlantic Refining Company of Cuba. Imlay (1942: pl. 3: 2–3) identified a very loose coiling, subquadrate whorl section with maximal thickness near the middle of gently convex flanks, and a coarse sculpture in the specimen 11 mm in size (note three-time magnification indicated by Imlay). This author also observed prominent and slightly prorsiradiate ribs terminating in coarse tubercles on the shoulders. Imlay (1942: 1446) noted the resemblance of the Cuban specimen with both the European Ammonites volanense (Oppel 1863: pl. 58: 2a, b), which was included in Simoceras, and the South American Simoceras aff. volanense Oppel in Krantz (1928: pl. 3: 7). Later, Cecca (1999: 22) interpreted the Cuban specimen as S. aesinense (Meneghini, 1885) while Schweigert et al. (2002: 8) reinterpreted this species as belonging to Volanoceras, a younger synonym of genus Simoceras according to Cecca (1999: 11).

Verma and Westermann (1973: 196, pl. 37: 2) described Simoceras cf. S. volanense (Oppel, 1863) from the Virgatosphinctinae Beds, upper part of the El Pastor Member, La Caja Formation, in locality 40C: a creek close to the small village of El Pastor in the southern part of Sierra de Catorce, San Luis Potosí, Mexican Altiplano. These authors recognised that the specimen was somewhat distorted, and they describe loose coiling, a subquadrate to depressed whorl section, and blunt ribs between two rows of tubercles in the specimen of 72 mm under study. They also observed a constriction at the end of the preserved inner mould, which they interpreted as a probable indication of complete growth, and the possible existence of constrictions in the inner whorls. Verma and Westermann (1973: 196–197) assumed a close affinity with Simoceras aff. volanense Oppel in Krantz (1928), which was considered synonymous with Oppel's (1863) original, and denser ribbing in Simoceras sp. juv. cf. volanense Oppel in Imlay (1942). Later interpretations considered the specimen described by Verma and Westermann (1973) as: Simoceras (Volanoceras) cf. volanense (Oppel, 1863) by Callomon (1992), who envisaged an age corresponding to the mid-to-upper Lower Tithonian in Europe; Simoceras close to S. aesinense (Meneghini, 1885) (Olóriz et al. 1999: 478); S. aesinense (Meneghini, 1885) (synonym Simoceras schwertschlageri Schneid, 1915) (Cecca 1999), Simoceras of the group of S. aesinense (Meneghini, 1885) (Villaseñor et al. 2000b), S. aesinense (Meneghini, 1885) (Villaseñor et al. 2000a: A-469) with the local subspecies S. aesinense chignahuapense (Cantú-Chapa, 1990) for eastern and north-central Mexico and doubts as to how many subspecies of S. aesinense (Meneghini, 1885) were in the Americas; and Volanoceras krantzense Cantú-Chapa, 1990 (Schweigert et al. 2002: 9).

Cantú-Chapa (1990: 41–45, fig. 2a–d) described Volanoceras chignahuapense sp. nov. from Lower Tithonian deposits that crop out in Chignahuapan, Puebla, central-eastern Mexico. The specimen of 40.13 mm in shell size was gathered from a calcareous concretion and magnified at 1.4 and 2.2 in Cantú-Chapa (1990: fig. 2a, b and 2c, d, respectively). This author noted a serpenticone shell with a rectangular whorl section, two to three constrictions per complete whorl, and simple, flattened ribs as wide as the inter-rib spaces. He also described periumbilical swelling of ribs and periumbilical tubercles on the inner whorls (the latter unidentifiable in his illustrations), and ventrolateral termination of ribs in spiny, tangentially elongated tubercles. Cantú-Chapa (1990) indicated Volanoceras (Geyssant, 1985) as the most appropriate genus-level interpretation, and therefore made a detailed examination and comparative analysis of supposedly conspecific forms showing simple or bifurcate ribs on the inner whorls (as discussed in point d below). This author recognised a particular affinity with Simoceras aff. volanense Oppel in Krantz (1928) through ventrolateral tuberculation, and rightly remarked that the Argentinean specimen is distinguished by an absence of constrictions, a feature that he also used to differentiate Ammonites volanense in Oppel (1863) from the specimen described by Krantz (1928). Cantú-Chapa (1990) likewise proposed the interpretation of the specimen described by Krantz (1928) as Volanoceras krantzense sp. nov., and thus a separation from the European “Simoceras cfr. volanense Oppel, 1863 sp. var. aesinense” in Meneghini (1885), (= Simoceras, Volanoceras or Pseudovolanoceras aesinense Meneghini, 1885 of several authors). Cantú's (1990) proposal (Cantú-Chapa 1990: 43) assumed the occurrence of bifurcate ribs in Volanoceras aesinense (Meneghini, 1885); but they are absent from both the corresponding type specimens. CantúChapa (1990: 43) rejected the conspecific relationships interpreted by Geyssant (1988) for the Italian species V. aesinense (Meneghini, 1885) with all simoceratin specimens referred to Tithonian Simoceras in the Americas. Concerning the small Cuban specimen (Imlay 1942), Cantú-Chapa (1990) stated that because it was a juvenile it would not be used for comparative analyses (but see point e below). Moreover, according to Cantú-Chapa, the Mexican specimen described by Verma and Westermann (1973) could not be interpreted at the species level because of poor preservation. Cantú-Chapa (1990: 43) rightly separated his Mexican specimen from Simoceras volanense Oppel in Zittel (1870) and Simoceras schwertschlageri in Schneid (1915). Finally, Cantú-Chapa (1990: 43, 45) outlined similarities and differences between Volanoceras chignahuapense sp. nov. and the closest species V. aesinense (Meneghini, 1885), indicating similarity in tuberculation and constrictions but absence of bifurcate ribs in the Mexican specimen. As commented above, the type of “Simoceras cfr. volanense Oppel, 1863 sp. var. aesinense” in Meneghini (1885: 376) does not show bifurcations, and both these forms furthermore show an exclusive character typical of the Meneghini' species, namely the longitudinal furrow between tubercles on the shoulders in moulds. This feature was not analysed by Cantú-Chapa (1990), but it is seen clearly in his fig. 2a, b. Later interpretations of Cantú's species Volanoceras chignahuapense Cantú-Chapa, 1990, refer to Cecca (1999: 26) and Schweigert et al. (2002), who assumed Volanoceras chignahuapense Cantú-Chapa, 1990 as conspecific with Simoceras aesinense (Meneghini, 1885) but belonging to different genera/subgenera (Simoceras and Volanoceras, respectively), whereas Villaseñor et al. (2000a) considered it to be the geographic subspecies Simoceras aesinense chignahuapense (Cantú-Chapa, 1990). Cecca (2002a) did not change his interpretation at the species level (e.g., Cecca 1999), but included it in his new subgenus Pseudovolanoceras.

With regard to the hypotheses given below, this revision of interpretations of Lower Tithonian simoceratids from the Americas features some significant points:

(i) The early separation of the Argentinean specimen from the European species S. volanense Oppel, 1863 made by Krantz (1928), who compared two supposedly adult specimens.

(ii) The similarity Imlay (1942) found between his Cuban nucleus, assumed to be juvenile, the European species S. volanense Oppel, 1863, and the Argentinean specimen described by Krantz (1928). This does not indicate defective analysis, since the very nucleus (precisely the part that is barely observable in the Cuban specimen but crucial for interpretation) is not well preserved in the European Ammonites volanense in Oppel (1863) and S. volanense Oppel in Zittel (1870). The outer whorls in the latter were considered to belong to other species V. aesinense (Meneghini, 1885) by Geyssant (1985), a reinterpretation that could apply to the complete illustration (e.g., Santantonio 1986). In fact, true A. volanense Oppel, 1863 nuclei have been characterised by the occurrence of dominant bifurcates below ca. 20 mm, which was considered by Santantonio (1986) to be crucial for differentiation of the morphologically close species S. aesinense (Meneghini, 1885) and S. volanense (Oppel, 1863). The nucleus studied by Imlay (1942) basically coincides with that of the Argentinean specimen described by Krantz (1928). As mentioned above, the latter specimen was interpreted as Volanoceras krantzense Cantú-Chapa, 1990 by Schweigert et al. (2002) following Cantú-Chapa (1990), admitting the occurrence “pseudo-bifurcations” in nuclei and an intermediate, evolutionary place between V. aesinense (Meneghini, 1885) and V. schwertschlageri (Schneid, 1915). “Pseudo-bifurcations” for these authors (Schweigert et al. 2002: fig. 5a) refer to the sculptural structure resulting from the incidence of growth increments on ribbing orientation on the flanks. Connected to growth increments, these structures must show congruent orientation with adjacent, later simple ribs. However, it is not the sole case among interpreted Volanoceras illustrated by Schweigert et al. (2002; e.g., V. krantzense Cantú-Chapa, 1990 in pl. 2: 2 showing a specimen from Spain with an incorrect reference in the figure caption) and real bifurcate ribs occur (e.g., in the same illustration and in a later ontogenetic phase in Volanoceras schwertschlageri (Schneid, 1915, illustrated in their pl. 3: 1a)—i.e., in contrast to “pseudo-bifurcations”, real bifurcate ribs show neither a congruence of rib projection on the flanks nor necessarily imply relation with more or less accentuated constrictions.

(iii) The interpreted affinity proposed by Verma and Westermann (1973) between their specimen collected from Sierra de Catorce, Mexico, and those described from Cuba (Imlay 1942) and Argentina (Krantz 1928), the latter being considered synonymous by these authors in contrast to some later interpretations (see above).

(iv) The artificial, compound character that Geyssant (1985: 679) interpreted for the illustration of S. volanense Oppel in Zittel (1870: pl. 32: 7), who interpreted the inner whorls as resembling A. volanense in Oppel (1863: pl. 58: 2a, b) while the outer evoked “Simoceras cfr. volanense var. aesinense” in Meneghini [1885 = Volanoceras aesinense (Meneghini, 1885) in Geyssant's (1985) interpretation]. Even if coinciding with Geyssant's (1985) observation (but see Santantonio 1986), assuming no difference in ribbing on the inner whorls among species of his new genus Volanoceras, the reference to Zittel's (1870) illustration does not help to clarify a crucial difference: the occurrence of bifurcate ribs on the inner whorls in Ammonites volanense Oppel, 1863 and the occurrence of simple ribs in Simoceras aesinense (Meneghini, 1885) (see above comments on “pseudo-bifurcations” sensu Schweigert et al. 2002). This distinction, unappreciated in interpretations subsequent to Oppel (1863: 232, pl. 58: 2a), was highlighted by Santantonio (1986), who described bifurcate ribs on the inner whorls of Simoceras volanense Oppel, 1863 (at least up to 18 mm) as he interpreted this taxon. In fact, close analysis of the nucleus in Oppel's illustration (1863: pl. 58: 2a) at less than 20 mm (see also Schweigert et al. 2002: pl. 4: 1 under magnification ×300) appears to reveal convergence of ribs close to the whorl overlap. Unfortunately, sculptural details in Zittel's (1870) illustration are unappreciable, most likely due to unfavourable preservation of the original specimen.

(v) Comments by Cantú-Chapa (1990) are relevant in two senses. Firstly, the close affinity between his Mexican species, the Argentinean specimen described by Krantz (1928) and S. aesinense (Meneghini, 1885) was soundly based on tuberculation, but he over-emphasised the sole difference in the development of constrictions with respect to the former, and did not observe the crucial shallow furrow recognisable in moulds of inner whorls of the species S. aesinense (Meneghini, 1885) as well as in the specimen he described (e.g., Cantú-Chapa 1990: fig. 2d). Other differences are minor or do not exist (e.g., bifurcate ribs in S. aesinense Meneghini, 1885). Secondly, he rightly interpreted that a sole nucleus (in reference to the Cuban specimen described by Imlay 1942) must not be used for comparative analysis at the species level (and, by extension, at the genus level); nevertheless, he worked with a potential juvenile and/or incomplete specimen showing probably less than one-fourth of the body chamber at 40.13 mm, and described his new species as included in the genus Volanoceras Geyssant, 1985. Villaseñor et al. (2000a) gave a preliminary interpretation as S. aesinense chignahuapense (Cantú-Chapa, 1990) for this incomplete specimen described by Cantú-Chapa (1990), while Cecca (2002a) proposed it as a junior synonym of the Meneghini (1885) species.

In addition to the above, we agree with the guidelines given by Santantonio (1986) for the precise differentiation of Tithonian simoceratin species, i.e., the occurrence of dominant bifurcate ribs vs. simple ribs in their nuclei. Hence, we assume a well established fact in the species group of S. aesinense (Meneghini, 1885) and A. volanense Oppel, 1863—i.e., different nuclei with simple and bifurcate ribbing, respectively. Genus Volanoceras, as proposed by Geyssant (1985), is therefore polyphyletic, as it has been the common interpretation for Simoceras, even when the use of subgenera is restricted (e.g., Fözy 1988).

Material and methods

In both of the sections investigated bed-by-bed, macrofossils —mainly bivalves and ammonites (1200 specimens and fragments)—were found in discontinuous horizons within the stratigraphic interval containing simoceratins. In general, macrofossil preservation is moderate to poor (imprints and leaf preservation sensu Seilacher et al. 1976), and preservation in volume as inner moulds is rare. Haploceratidae, perisphinctids and simoceratins predominate in ammonite assemblages where most of the specimens can be identified only at the genus level.

The simoceratins described were found in the lowermost 3.5 m of the Apulco section MT-2, and in the upper 10 to 12 m of the new Apulco section MTQ (Fig. 2). The total number of identified specimens was twenty-one. Among stratigraphically collected specimens, fifteen belong to section MT-2, and six specimens were gathered from bed MTQ-11 in section MTQ.

Biochronostratigraphy was conducted according to the Secondary Standard of reference for the Tithonian (e.g., Geyssant 1997).

Preparation of the material and shell/mould measurement (in millimetres; see Appendix 1) was mainly performed in the Laboratory for Invertebrates of the UNAM, with complementary work carried out at the University of Granada, Spain.

Notes on Simoceratinae: systematics, taxonomy, and evolutionary patterns

Several proposals have been put forth over the past 30 years regarding systematics, taxonomy, and evolution in Lower Tithonian simoceratins above the species level (e.g., Olóriz 1978; Geyssant 1982, 1985, 1988; Santatonio 1986; Fözy 1988; Cecca 2002a; Schweigert et al. 2002). An abridged review is given below.

Olóriz (1978) interpreted a comprehensive genus Simoceras differentiated into morphologic, evolutionary subgenera according to basic phenotype differences through ontogeny, which starts with an initial perisphinctoid-stage followed by: (i) tuberculate or simoceroid-stage (subgenus Simoceras); (ii) shell smoothing or Iytoceroid-stage (Lytogyroceras); or their combination (subgenus Simolytoceras). Olóriz (1978: 237) envisaged three potential interpretations of evolution at the subgenus level, which can be simplified in terms of: Iterative evolution from a perisphinctoid nucleus (then considered as evidence of phylogenetic connection with Idoceratinae); and anagenetic and/or cladogenetic evolution from the basic simoceroid-stage. This author acknowledged difficulties with stratigraphic condensation in obtaining fine stratigraphy to clarify the relative FADs of Simolytoceras and Lytogyroceras, and did not study the species S. aesinense (Meneghini, 1885) among the rare (then considered Simoceras volanense Oppel, 1863 group) simoceratins collected from Haploceras verruciferum Biozone deposits in ammonitico rosso facies (Semiformiceras semiforme/Haploceras verruciferum Chronozone in the Secondary Standard for Tethyan areas; e.g., Geyssant 1997). In addition, this author identified a “simoceratin-like” morphology in one of the two groups interpreted as Virgatosimoceras (Olóriz 1978: 204), overemphasising their perisphinctoid nuclei resembling those shown by the older Nebrodites as well as the occurrence of Idoceras-like rib furcations.

Santantonio (1986) analysed abundant, well-preserved material, rightly typified traits' recognition for identification of Lower Tithonian simoceratin species, and considered common, defective preservation in ammonitico rosso facies as a major difficulty in separating Simoceras aesinense (Meneghini, 1885) from the S. volanense Oppel, 1863 group (genus level interpretation according to Santantonio 1986). He put forth Virgatosimoceras as a key-branch for evolution in Lower Tithonian simoceratins, potential polyphyly for the S. volanense Oppel (1863) group, as well as an obscure origin for S. aesinense (Meneghini, 1885), and recommended future separation of the latter at the genus or subgenus level. S. aesinense (Meneghini, 1885) was interpreted as a separate branch within the polyphyletic genus Simoceras.

Geyssant (1982, 1985, 1988) interpreted the evolutionary pattern in Lower Tithonian simoceratins and proposed punctuated equilibrium and palaeogeographic dynamics as the appropriate template for their interpretation. Geyssant (1982) interpreted genus Simoceras in a broad sense, as usual at the time, and identified “Simoceras n. sp. gr. volanense Oppel, 1863” from the Semiformiceras semiforme Biozone (equivalent to the Haploceras verruciferum Zone = Semiformiceras semiformel Haploceras verruciferum Chronozone in the Secondary Standard for Tethyan areas; e.g., Geyssant 1997), envisaging a widespread geographic distribution (southern Europe, Cuba, Mexico, and Argentina). This author interpreted discontinuous in-situ evolution, allopatric speciation and recolonisation by species belonging to genus Simoceras in southern Europe and nearby northern areas (Franconia). Based on ICZN rules, Geyssant (1985) restricted the use of genus Simoceras to the Simoceras admirandum Zittel, 1869/ Simoceras biruncinatum Quenstedt, 1847 group and erected the new genus Volanoceras for Lower Tithonian simoceratins such as V. aesinense (Meneghini, 1885), V. schwertschlageri (Schneid, 1915), and V. volanense (Oppel, 1863). Implicit in Geyssant's (1985) interpretation is the polyphyletic character of her new genus Volanoceras, while Simoceras turned to be monophyletic. No particular comments about V. aesinense (Meneghini, 1885) were provided. Geyssant (1988) revisited her punctuated equilibrium hypothesis, now applied to Volanoceras that she envisaged as a single monophyletic linage.

Fözy (1988) approached the interpretation of Simoceratinae promoting the use of assumed monophyletic taxa, and followed Geyssant (1985, 1988) when analysing Volanoceras, thus anticipating hypotheses later detailed by Schweigert et al. (2002). However, this author did not provide an evolutionary pattern at the subfamily level, and the degree of monophyly resulted heterogeneous in the taxa he identified in simoceratins. In his study of the material gathered from ammonitico rosso and related facies containing envisaged juveniles and adults, Fözy (1988) approached dimorphic couples at the subgenus level following Callomon (1969).

In 2002 the most recent reinterpretations of Tithonian simoceratins were published, in parallel, by Fabrizio Cecca and Günter Schweigert and collaborators. Schweigert et al. (2002) revisited Lower Tithonian simoceratins and reinterpreted Volanoceras' species, their stratigraphy, palaeobiogeography and evolution, partially based on bibliographic re-evaluations; they proposed invalidation of the oldest species related to the S. aesinense (Meneghini, 1885) group (S. praecursor in Santantonio 1986) and promoted recuperation of an old species name (Ammonites perarmatiforme Schauroth, 1865) for the youngest specimens reported. These authors envisaged a chronocline for Volanoceras and, following Geyssant (1985), did not recognise relevant differences in inner whorl sculpture between the V. aesinense (Meneghini, 1885) and V. volanense (Oppel, 1863) groups. Hence, the potential polyphyly derived from Santantonio's (1986) model was overlooked. Schweigert et al. (2002) interpreted V. aesinense (Meneghini, 1885) including European, Cuban, and east-Mexican records, and confirmed species-level status and conspecifity for the Argentinean and central Mexico records. On the other hand, Cecca (2002a) basically followed Santantonio (1986) and proposed the new subgenus Pseudovolanoceras for S. aesinense (Meneghini, 1885) and related species from the Americas. This author recognised difficulty with Volanoceras' evolution as proposed by Geyssant (1982), due to limitations forced by both the defective preservation of inner whorls and the precise biostratigraphic interpretation of some species crucial for Geyssant's (1982) interpretation. He therefore proposed species reorganisation among Lower Tithonian simoceratins, which were allocated in three morpho-evolutionary subgenera within genus Simoceras: S. (Simoceras) restricted to the S. admirandum Zittel, 1869/5. biruncinatum Quenstedt, 1847 group, S. (Volanoceras) for the S. volanense Oppel, 1863/S. vicentinum group, and S. (Pseudovolanoceras) for S. aesinense (Meneghini, 1885) and related species.

On the basis of all the above, we consider two alternative options for the present interpretation of Lower Tithonian simoceratins above the species level: (i) interpreting a comprehensive genus Simoceras subdivided in subgenera with evolutionary, not merely morphologic meaning (e.g., Olóriz 1978; Cecca 2002a); or (ii) interpreting evolutionary relevance at the genus level, meaning that no subgenera apply. In option (i) the genus level is strictly nominal and provides the closest allusion to the immediately higher taxonomic level of reference (e.g., subfamily/family), and thus a higher level of polyphyly is assumed; whereas subgenera will provide phylogenetic information revealing relatively major phenotype breaks (innovations) within an assumed cohesive grouping of ammonites such as Simoceratinae. Alternatively, in option (ii) the genus level directly identifies these breaks in phenotype evolution (innovations forcing relative monophyly), with no direct information about the immediately higher level of taxonomic reference (family/subfamily level). At present, we favour option (ii), interpreting genus-level clade identification (through recognition of innovations) reinforcing taxonomy with evolutionary significance at this level—i.e., based on inner whorl sculpture as the crucial phenotype stage for the interpretation of higher-level taxonomy and evolution, and later morphological breaks (innovations) for clade-level, phylogenetic identification at the genus level.

This proposal is supported by (i) available information about precise biostratigraphy; (ii) iterative evolution of simoceratins from a “perisphinctoid”, Virgatosimoceras-like or closely related branch as the main evolutionary pattern; (iii) difficulty in approaching genus-level monophyly sensu stricto some other way; (iv) the polyphyletic character of the latter genus-level taxon created for Simoceratinae (Volanoceras as interpreted by Geyssant 1985, 1988 and Schweigert et al. 2002); and (v) avoiding maintenance of genera as large, heterogeneous and presumably polyphyletic species complexes. Accordingly, and based on the available information, the genus-level taxonomy proposed points to approaching the least inclusive taxonomic unit at this level.

At the species level, our interpretation accords with postulates derived from: (vi) phenotype cohesion (e.g., Templeton 1989); (vii) relevance of dynamic biogeography, at least for determining subspecies (e.g., Nelson and Platnick 1981); and (viii) recognition of species-flock, species complex and metapopulation-metacommunity concepts and their enlightening potential for interpreting cephalopod diversity, biogeography and underlying dynamics at the population and species levels (e.g., Yacobucci 1999; Norman 2003; Yoshida et al. 2006; Bolstad 2009; Gillanders et al. 2009; Olóriz and Villaseñor 2010, and references therein). Thus, the species level is approached within the conceptual framework favouring the relevance of environmental forcing, of biogeographic range processes, and autapomorphy (e.g., Van Valen 1976 and Ridley 1989 to complement citations above).

Remarks on the simoceratin species Simoceras aesinense (Meneghini, 1885) sensu Santantonio (1986).—Some observations concerning the ontogenetic course of Simoceras cfr. volanense Oppel, 1863 sp. var. aesinense in Meneghini (1885) deserve mention here.

Meneghini (1885: 376–378) described a specimen of 62 mm in size (which accords with his illustration in pl. 20: 4a, b), identified the last whorl as the last one preserved, and recognised both difficulty in identifying constrictions on the inner whorls and their deepness on the outer whorl. In addition, Meneghini (1885) noted depressed tubercles on shell periphery (shoulders), pointed ones on the umbilical edge, ribs between these two rows that changed around the middle of the penultimate whorl (29–30 mm in his illustration) to become ventrally enlarged towards the outer whorl while showing a small, and delicate tuberculation on the inner whorls; he likewise reported suture line details from the third whorl. In comparison with the Lower Tithonian species Ammonites volanense Oppel, 1863, Meneghini (1885) found differences in coiling degree and rib density on the inner whorls, differential crowding of ribs and morphology of the peripheral tubercles with respect to Simoceras volanense (Oppel in Zittel 1870: 95, pl. 32: 7–9), and lesser similarity in both the looser coiling and gradual change in sculpture with respect to A. volanensis in Oppel (1863: pl. 58: 2a, b). On this basis, Meneghini (1885) formalised the recognition of his “S. cfr. volanense Oppel, 1863 sp. var. aesinense” as the most frequent among the Simoceras that he compared from Tithonian deposits in the Marche (central Italy), indicating that specimens larger than 45 mm show spiny periumbilical and peripheral tubercles on the outer whorl preserved. In this whorl, the author described two constrictions towards the end, the posterior one deep and bordered by an aboral simple, slightly finer rib concave forwards and terminating in the corresponding spiny tubercle on the shoulder. A similar constriction was identified by Meneghini (1885) closer to the end of the preserved outer whorl, as well as another two early in the same whorl, four in the penultimate whorl, and a few more irregularly spaced ones on the innermost whorls that show ribs with spiny tubercles on the shoulders. Finally, Meneghini (1885) stressed the absence of suture lines adorally from the outermost constriction described.

Santantonio (1986) indicated that Meneghini's (1885) type was lost during the Second World War, but was able to analyse a cast, and promoted the name S. aesinense (Meneghini, 1885) as a valid species. On the basis of abundant and well preserved material, this author accurately described the ontogeny in the S. aesinense (Meneghini, 1885) species and interpreted its morphologic variability. He recognised dimorphism on the exclusive basis of shell size within a range of small to medium sized individuals (up to 65 and 94 mm, respectively), and identified the beginning of the body chamber at around 60 mm in macroconchs (between 20 and 35 mm in microconchs). In addition, he observed subquadrate whorl sections, loose coiling that decreased throughout the ontogeny, and no difference in sculpture between sexual dimorphs other than those related to shell size. Santantonio (1986) did not describe the type of peristome in microconchs (see previous allusion to his comments about defective preservation in rosso ammonitico facies), but interpreted crowded constrictions at the end of preserved shells and moulds as an indication of complete individuals. This author established the following ontogenetic phases in the sculpture of the species S. aesinense (Meneghini, 1885): (i) below 15 mm, ribs are simple, wider than inter-rib spaces, slightly concave adorally and terminating in small ventrolateral clavi that elongate tangentially during the ontogeny; (ii) at 30 mm, the periumbilical part of the ribs may have a comparatively higher relief, which coincides with their relative depression at the mid-flank, while ventrolateral clavi are prominent; (iii) around 40–45 mm the typical combination of progressive rib swelling, decreasing sculpture at the mid-flank, and the tangential expansion of clavi occurs, and typical individuals show radial-periumbilical bullae, a mid-flank depression with possible development of geminate ribs, and ventrolateral clavi elongated longitudinally. This third stage is accentuated in macroconchs larger than 60 mm, especially in development of bullae and the mid-flank germination of ribs. Santantonio (1986) gave fewer details about constrictions, but accurately noted their decreasing number (from around two in the inner whorls), their increasing excavation toward the outer whorls, and the persistent occurrence of relative sharp edges. In addition, he described the significant relief of clavi, which could be connected by subtle, wide folds of the ventral region. Santantonio (1986) placed special emphasis on the occurrence of a “cordone spirale” observable between clavi of well preserved shells, which determines an interclavi groove identifiable in phragmocones and body chambers preserved as inner moulds. Moreover, he mentioned small ribs (i.e., riblets) in the clavi walls of well-preserved specimens. In Santantonio's (1986) comparative analysis of the Lower Tithonian species S. aesinense (Meneghini, 1885) and S. volanense (Oppel, 1863) he stressed high variability in the change of bullae to periumbilical tubercles in specimens of greater size, and in their onset during the ontogeny (from 25–30 mm onwards), and gave the precise stratigraphic range for species S. aesinense (Meneghini, 1885) in coincidence with the Lower Tithonian Haploceras verruciferum/ Semiformiceras semiforme Chronozone in the Mediterranean Tethys.

Among the data provided by Meneghini (1885) and Santantonio (1986), the following points are of relevance for the interpretation of Lower Tithonian simoceratins from the Americas:

(i) Species S. aesinense (Meneghini, 1885) has small macroconchs (body chamber beginning as small as 60–70 mm). Recognition of the outer whorl in Meneghini's type as the last preserved (Meneghini 1885), and the clarification about a small final part without suture lines in the type (Meneghini 1985), indicate the possible existence of larger individuals (later confirmed by Santantonio 1986).

(ii) The noteworthy difference in recognition of constrictions indicates intra-species variability for this character.

(iii) Ribbing changes at ca. 30 mm, described by Meneghini (1885), coincide with the second ontogenetic stage described by Santantonio (1986), i.e., the beginning of periumbilical tuberculation together with mid-flank depression of ribbing. These two traits seem to be in co-variance.

(iv) Typical bituberculation comprising spiny-perpendicular and spiny-tangential elements above 45 mm (Meneghini 1885) agrees with the third ontogenetic stage of Santantonio (1986), who added comments that support co-variation in shell features.

(v) Ontogenetic stages and variability affecting sculpture expression (timing for change from bullae to periumbilical tubercles included) as described by Santantonio (1986).

(vi) Occurrence of subtly ribbed clavi and “cordone spirale” in relation with good preservation, in particular the appearance of the latter as a groove on inner moulds of phragmocones and body chambers (Santantonio 1986).

(vii) Identification of the precise stratigraphic range of 5. aesinense (Meneghini, 1885) within the Lower Tithonian (Santantonio 1986; genus-level interpretation according to this author).

(viii) Phenotypic expression of dimorphism. Interpreted on the basis of shell size without significant incidence in sculpture (Santantonio 1986), as commonly assumed for Lower Tithonian simoceratins (e.g., Geyssant 1988). No apertural structures are accurately known for macroconchs, and they are unknown in microconchs (in coincidence with Geyssant 1988). The sole reference to peristome in Tithonian simoceratins was made by Geyssant (1979: 15–16, text-fig. 15, pl. 2: 3), who envisaged a microconchiate peristome in correspondence with a small, pointed adorai projection separating dorsal and ventral concavities at the end of the shell in her Upper Tithonian genus Baeticoceras Geyssant, 1979, a younger synonym of Cordubiceras Olóriz and Tavera, 1979, as recently recognised by Benzaggagh et al. (2010).

Extensive reference to interpretations of Meneghini's (1885) species at the species level and higher ones is given above. At present, we interpret that “S. cfr. volanense Oppel, 1863 sp. var. aesinense” Meneghini, 1885 represents a widespread species, or species complex, inhabiting epioceanic environments in western Tethys but also, less commonly, epicontinental shelves in the area and the Americas, where geographical differentiation existed (see below).

Systematic palaeontology

Class Cephalopoda Cuvier, 1798
Order Ammonoidea Zittel, 1884
Suborder Ammonitina Hyatt, 1889
Superfamily Perisphinctoidea Steimann in Steimann and Doderlein, 1880
Family Simoceratidae Spath, 1924
Subfamily Simoceratinae Spath, 1924
Genus Pseudovolanoceras Cecca, 2002
Type species. Simoceras aesinense (Meneghini, 1885): Pelagic cephalopod limestone in central Appenines, Marche, Italy; Lower Tithonian.

  • Remarks.—Cecca (2002a: 363–364) erected Simoceras (Pseudovolanoceras) for the Simoceras aesinense (Meneghini, 1885) (sensu Santantonio, 1986) species group in Europe and the Americas, and designated the Meneghini (1885) species as type-species. The Mexican species Volanoceras chignahuapense Cantú-Chapa, 1990 was considered a younger synonym, while the Argentinean species V. krantzense Cantú-Chapa, 1990 was accepted as a separate taxon at the species level.

  • Pseudovolanoceras aesinense chignahuapense (Cantú-Chapa, 1990)
    Figs. 3A–E, 4A–G, 5A–D, 6C, 7, 8A, B.

  • ?1973 Simoceras cf. S. volanense (Oppel 1863); Verma and Westermann 1973: 196, pl. 37: 2a, b.

    1990 Volanoceras chignahuapense sp. nov.; Cantú-Chapa 1990: 41, fig. 2a–d.

    1999 Simoceras aesinense (Meneghini, 1885); Cecca 1999: 7, 26 (partim).

    2000a Simoceras aesinense chignahuapense (Cantú-Chapa, 1990); Villaseñor et al. 2000a: A469.

    ?2000b Simoceras group of aesinense (Meneghini, 1885); Villaseñor et al. 2000b: 257.

    2002 Volanoceras aesinense (Meneghini, 1885); Schweigert et al. 2002: 8, non pl. 1: 1–4 (partim).

    2002a Simoceras (Pseudovolanoceras) aesinense (Meneghini, 1885); Cecca 2002a: 364 (partim).

  • Material.—Twenty-one specimens labelled IGM 6085-2a and IGM 9541 to IGM 9559.

  • Measurements.—See Appendix 1. For approximate values note (*) for values obtained from specimens, or (**) when taken from illustrated specimens.

  • Emended diagnosis.—Loosely coiled shells. Simple ribs with more or less distinct reinforcement of ventral extremes on the inner whorls, and then two rows of tubercles. Low expression of geminate ribs on the flanks in macroconchs. Variable weakening of sculpture on the outer whorl in microconchs. Periumbilical tubercles indistinct to more or less bulliform to pointed structures. Peripheral tubercles elongated longitudinally, more or less flared with occasional riblets, connected by longitudinal ridge on well preserved shells, and the associated groove on preserved inner moulds. Macro- and microconchiate individuals. Lappets in microconchs and unknown adorai structures in macroconchs. Suture line incompletely known.

  • Description.—Twenty-one specimens and fragments with a size range of 23.12 mm to 95.2 mm, preserved as imprints except IGM 9543a, a crushed phragmocone with partial body chamber preservation in volume; the probably near-complete IGM 9544 gathered from a concretion; IGM 9548a, which is a flattened inner mould with only partial preservation of body chamber in volume; and IGM 9555, a fragmentary inner mould preserved in volume with shell remains and part of the body chamber. Note that flattening and related distortions probably determined the bias in some of the parameters and, therefore, curves showing the course of coiling and whorl height could be slightly affected.

    Coiling is variable at smaller shell diameters (U/D = 37–59%) but tighter than above 20-30 mm shell diameter, except in the extremely evolute IGM 9541 (Fig. 4B), looser above 30 mm (U/D = 49–64%), and decreasing slightly during ontogeny (Fig. 5A, B).

    Due to defective preservation, there are few precise data about the umbilical wall and the whorl section. When preservation in volume was possible, the umbilical wall seen to be gently vertical with rounded edge, or indistinct because of the gentle convexity of flanks towards the line of whorl-overlapping.

    Due to common shell and/or mould crushing, equivalent estimation applies to whorl thickness. However, specimens preserved in volume allow for identification of subrectangular whorl sections. Thus, IGM 9555 shows a subrectangular whorl section with rather convex flanks (Fig. 3A); IGM 9543a allows for partial reconstruction of the body chamber showing subrectangular whorl section in correspondence with peripheral tubercles, and an oval whorl section between tubercles. A similar whorl-section design is found between ribs in other specimens, and gently convex flanks determine the maximum whorl-width placed close to the mid-flank.

    Whorl-height values vary on the inner whorls (< 35 mm), and tend to stabilise through ontogeny (Fig. 5C). Thus, there are specimens in which whorl height values sharply decrease below 20 mm in shell size, then rise to ca. 25–30 mm and diminish at greater shell diameters (e.g., IGM 9551a, IGM 9544, IGM 9545a, IGM 9546a), although cases showing near-constant values were also identified (e.g., IGM 6085-2a).

    Recognition of constrictions is variable, which might result from their usual course parallel to ribbing combined with the effect of flattening, but certainly provides information about inter-population biodiversity in constriction number, excavation and across flank course. Constrictions are more prorsiradiate in the nuclei. Thus two subsets of specimens were identified according to:

    (i) Subtle constrictions, which are gently prorsiradiate between 20 mm and 27 mm of shell diameter but, while rare, seem to be better developed later in ontogeny (e.g., IGM 9545a shows a deep constriction, concave towards the aperture close to the end of the preserved imprint; Fig. 3C).

    (ii) Constrictions are more frequent and well developed, concave to the aperture and more excavated, especially on the outer whorl (e.g., IGM 9541, IGM 9543a); two to three constrictions per complete whorl in the middle whorls (e.g., IGM 9544), and three to four on the outer whorl; a constriction close to the end of the inner mould is the pre-apertural one, which is comparatively radial and straight (e.g., IGM 6085-2a).

    Sculpture typically varies throughout ontogeny, and therefore, counting periumbilical ornamentation per half-a-whorl (PS/2 in Appendix 1) provides data on relative crowding during ontogeny, whatever its precise type. Figures 5D and 7 reveal initial, progressive decreases in crowding of sculpture and then a trend to stabilisation later in ontogeny. In general, on the inner whorls up to 16–22 mm in shell size, ribs are wider than the inter-rib spaces, simple, radial to slightly prorsiradiate, and slightly enlarged towards shell periphery. Their ventrolateral ends are reinforced as small, rounded tubercles, which are partially covered by the next whorl. Favourable but differential observation for analysing sculpture in the nucleus is found in some specimens. Up to 11 mm ribs are simple, prorsiradiate, slightly concave towards the aperture, wider than the inter-rib spaces and enlarge progressively toward the venter (IGM 6085-2a). However, rib crowding can persist up to 29–30 mm (e.g., IGM 9545a). Ventrolateral undulation due to the enlargement of clavi can occur from around 10 mm in shell size (e.g., IGM 9541, IGM 9544), and accentuates progressively to show typical Pseudovolanoceras aesinense (Meneghini, 1885)—typology with well-developed clavi, which are sometimes only evidenced through their impressions. At 19–20 mm the crowding of ribs diminishes, and ribs are much more swollen (IGM 6085-2a, IGM 9543a); but this observation could be partially obscured by preservation between 13–18 mm (IGM 6085-2a) and, therefore, the increasingly wide-convex relief could be more progressive than in IGM 9543a. Typical P. aesinense (Meneghini, 1885)—typology is seen ca. 20 mm in shell size and later in ontogeny (even in eroded specimens; e.g., IGM 9541), although it is doubtful to conclude about the incipient ribs' reinforcement close to the umbilical edge (e.g., observed in IGM 9544). A generalised change in sculpture occurs at around 30 mm with a marked increase in the enlargement of rib expansion towards the ventral extreme; ventrolateral clavi develop superimposing undulation on whorl junctions, and some cases of subtle periumbilical reinforcement of ribs in microconchs and stronger in macroconchs were observed (i.e., IGM 9545a and 9545b, IGM 9546a and 9546b, IGM 9546-2, IGM 9550b, IGM 9551a, IGM 9555).

    In microconchs, a difference in rib crowding occurs and is considered as inter-population variability. Significant but variable weakening of the sculpture is typical (e.g., IGM 6085-2a, IGM 9543a, IGM 9544). It starts from 36–37 mm onwards in IGM 6085-2a, preceded by two sinuous ribs, which are wider towards the venter—i.e., the outer half-a-whorl preserved is comparatively smooth except for well developed peripheral tubercles elongated longitudinally. In contrast, IGM 9543a shows slight periumbilical reinforcement of two ribs around 32 mm in shell size, but the final part of the preserved inner mould reveals the ventral region in volume just after a deep constriction with a rounded posterior edge and acute anterior one. Of special relevance is recognition in IGM 9543a and IGM 9544 of a very shallow groove between two successive ventrolateral tubercles elongated longitudinally (Fig. 4C1 G3). This groove corresponds to the equivalent one characterising the well preserved inner mould of species P. aesinense (Meneghini, 1885), and is therefore interpreted as evidence of “cordone spirale” (sensu Santantonio 1986). Also relevant is the occurrence of riblets in clavi (Fig. 4G2), first appearing at 12.5 mm in diameter in IGM 9544 (Fig. 4G4), and likewise identified in IGM 9546a. This ornamentation seems to be related to, or forced by, clavi enlargement from around 13 mm in shell size, which accentuates progressively and is well developed with typical P. aesinense (Meneghini, 1885) typology from around 17 mm. In general, no ventral regions are observable due to flattening (horizontal settling dominant), and crushed flanks in moulds make it less probable to recognise the groove that corresponds to the “cordone spirale” (sensu Santantonio 1986).

    In macroconchs, there is a generalised reinforcement of the sculpture from shell diameter of 37 mm to 45 mm onwards. Taking into account the common severe flattening, it is mainly evidenced by enlarged undulation on the whorl periphery, but in some cases periumbilical bullae or tubercles are affected (IGM 9545a, IGM 9547a, IGM 9551a, IGM 9554). The incomplete and comparatively coarse sculptured IGM 9545a shows relative smoothing on the outer whorl, with accentuated weakening of sculpture and a deep constriction concave to the aperture with prominent anterior edge (Fig. 3C, D). In the largest IGM 9547a, the outer whorl shows accentuation of inter-tubercle space that is concomitant with well-expressed periumbilical bullae and large peripheral tubercles. Given the state of preservation in almost all specimens, it is difficult to differentiate between blunt ribs and bullae or tubercles, which more or less progressively replace each other on the umbilical edge during ontogeny. However, the well and preserved in-volume IGM 9555 shows periumbilical spiny tubercles.

    Body chamber recognition is obscured by common leaf-preservation in siltstones, but some cases of crushed phragmocones and filled body chambers preserved in-volume are known (e.g., IGM 9548a, IGM 9543a). Specimens collected from concretions are more favourable, even for local preservation of suture lines (e.g., IGM 9555). In general, preserved body chamber length extends from one- to three-quarters of the outer whorl (e.g., IGM 9543a, IGM 9544).

    Nearly complete peristomial structures are first reported for microconchiate simoceratins in Mexico and the Americas. IGM 9546a shows pre-apertural constriction, comparatively radial and straight, which precedes the peristome with short, wide lappets that show convex corrugations inside (Fig. 4D, E). IGM 6085-2a preserves the pre-apertural constriction, which is wide, comparatively radial and straight, and also precedes the peristome with short, wide lappets that show convex corrugations inside (Fig. 4A). The occurrence of lappets in Pseudovolanoceras aesinense chignahuapense (Cantú-Chapa, 1990) validates the hypothesis of dimorphism in Simoceratinae (e.g., Geyssant 1979; Santantonio 1986). Geyssant (1979) interpreted as microconchiate peristome the mid-flank pointed adorai projection separating two concavities identified in Baeticoceras (younger synonym of Cordubiceras Olóriz and Tavera, 1979), and envisaged the possibility of this projection being a rough-draft of lappet occurrence. Santantonio (1986) envisaged the existence of macroand microconchs in S. aesinense (Meneghini, 1885), although he did not identify peristomial structuring for the Meneghini (1885) species and morphologically close ones. Thus, the reported evidence of lappeted peristome in P. aesinense chignahuapense (Cantú-Chapa, 1990) demonstrates a genus-level difference in peristomial structures for Tithonian microconchiate simoceratins.

    The suture line preserved in specimens IGM 9555 and IGM 9544 (Fig. 8A, B) is simple and clearly similar to other suture lines of Pseudovolanoceras aesinense (Meneghini, 1885) species, or species complex, at similar diameters (see Santantonio 1986: fig. 3b, d, f).

  • Remarks.—The state of preservation forces serious limitations on the precise analysis of dominant ammonite imprints, including the description and comparison of delicate sculptures in the Mexican specimens [IGM 9547a, IGM 9546-2, interpreted as Pseudovolanoceras sp. cf. aesinense (Meneghini, 1885)]. The material described shows qualitative and quantitative features that clearly accord with those characterising the European species P. aesinense (Meneghini, 1885) (Figs. 6, 7; Appendix 1) here reinterpreted as belonging to the genus Pseudovolanoceras Cecca, 2002 (see also Cecca 2002a). Of special relevance is the simple ribbing identified below 22 mm in shell diameter, and the change in sculpture around 30 mm that results in the typical pattern of sculpture of P. aesinense (Meneghini, 1885) with undulating periphery and variable reinforcement of periumbilical sculpture, generally coarser from around 40 mm onwards. However, earlier development of clavi, lower reinforcement of periumbical sculpture, and typical weakening of flank sculpture on the outer whorl characterises microconchs of P. aesinense chignahuapense (Cantú-Chapa, 1990) in the studied area, a trait related to an accentuated decrease in rib density throughout ontogeny (Figs. 5D and 7).

    All these differential traits are here interpreted as revealing local phenotype divergence from European representatives of the Meneghini (1885) species. In addition, observed traces consistent with occasional preservation (due to unfavourable dominant fossilisation in siltstones) of “cordone spirale” related structures (e.g., Santantonio 1986) in the material analysed (e.g., IGM 9543a, IGM 9544, IGM 9555) reinforce its interpretation as closely related to Pseudovolanoceras aesinense (Meneghini, 1885). The occurrence of riblets in external tubercles supports this hypothesis, since this bizarre sculpture was also identified in well preserved specimens of European P. aesinense (Meneghini, 1885) (e.g., Bernoulli and Renz 1970; Santantonio 1986). These two particular features, which are known in the European species, are consistent with the favoured interpretation of relationships at the subspecies level. In addition to these qualitative and crucial phenotype traits for species identification, quantitative ones (Figs. 57) reinforce the interpretation of these Mexican simoceratins as closely related to the European species P. aesinense (Meneghini, 1885). As commented above, microconchs are not distinguishable on the exclusive basis of shell size (e.g., Santantonio 1986 for incomplete specimens of P. aesinense [Meneghini, 1885]) or small, pointed adorai projections at the mid-flank (e.g., Geyssant 1979 for microconchs of the younger Cordubiceras), but on the occurrence of real lappets, which are reported for the first time from subfamily Simoceratinae. Although based on a comparatively incomplete observation obtained from the Mexican material analysed (less common macroconchs collected) macroconchiate specimens show sculpture in agreement with stages above 40 mm described in Santantonio (1986).

    The revision made of previous interpretations of Mexican simoceratins together with comments about the original description of “Simoceras cf. volanense Oppel, 1863 var. aesinense” in Meneghini (1885: 376) and later interpretations of Simoceras, Volanoceras, or Pseudovolanoceras aesinense (Meneghini, 1885) (Santantonio 1986; Cecca 1999, 2002a; Villaseñor et al. 2000a, b; Schweigert et al. 2002), as well as the precise analysis of cast (Krantz 1928) and types (Verma and Westermann 1973) revealing occurrence of traces related to the “cordone spirale” (Fig. 3F, G), lend support to our interpretation of the occurrence of Tethyan species P. aesinense (Meneghini, 1885) in Mexico and the Americas. In fact, the synonymy list (mainly restricted to papers with illustration and unequivocal references) given in Appendix 2 demonstrates the special relevance given to variability in shell features that previously was underestimated; this led to different, comparatively restricted and/or general interpretations of the Meneghini (1885) species (e.g., Fözy 1988; Cantú-Chapa 1990; Cecca 2002a; Schweigert et al. 2002). Based on the conceptual approach presented (see Notes on Simoceratinae chapter), we agree with contemporaneous interpretations which more or less clearly accept the occurrence of P. aesinense (Meneghini, 1885) or P. aesinense-like forms as the typical simoceratins in the Americas, despite their being submitted to differential interpretations at the genus level (e.g., Fözy 1988; Cantú-Chapa 1990; Cecca 2002a; Schweigert et al. 2002).

    As underlined earlier, the Argentinean specimen described by Krantz (1928) is without a doubt morphologically close to species P. aesinense (Meneghini, 1885) (Figs. 6, 7), even showing traces of the “cordone spirale” (sensu Santantonio 1986) as deduced from the plastic-cast examined (Fig. 3F). The intra-species variability we assume allows us to interpret this specimen as representing less constricted, heavier shell phenotypes showing coarser sculpture, most probably related to great size (as usually identified in neritic ammonites; cf. extreme phenotypes and the platform effect in Olóriz 1985; Olóriz et al. 1988; among others).

    With the assumption of age-compatibility (e.g., Santantonio 1986; Olóriz and Tavera 1979; Cecca 1999, 2002a; Parent and Capello 1999; Villaseñor et al. 2000a, b; Schweigert et al. 2002), we interpret the Argentinean specimen as a local phenotype expression of Pseudovolanoceras aesinense (Meneghini, 1885)—i.e., the geographic subspecies Pseudovolanoceras aesinense krantzense (Cantú-Chapa, 1990).

    The Cuban nucleus illustrated by Imlay (1942) is difficult to interpret, but the style of ribbing is easily comparable with that of species P. aesinense (Meneghini, 1885) (see above) rather than S. volanense Oppel, 1863, as interpreted by Imlay (1942). In fact, the latter species developed finer, bifurcate ribbing in the nucleus and then simple ribs with no equivalent difference in width across the flanks at the same ontogenic stage. The record of more complete individuals from Mexico, as demonstrated by the slightly larger individual from Puebla (species Volanoceras chignahuapense in Cantú-Chapa 1990) and the material described here from the Mazatepec area, reinforce this interpretation. The Cuban specimen would represent the first stage described by Santantonio (1986) for the species Simoceras aesinense (Meneghini, 1885) (genus level interpretation according to this author).

    As noted above, the small V. chignahuapense in Cantú-Chapa (1990) is here reinterpreted at the genus and subspecies levels (Pseudovolanoceras aesinense chignahuapense [Cantú-Chapa, 1990]), based on the occurrence of simple ribbing in the nucleus and the delicate imprint of the “cordone spirale” (see above). Its sculpture accords closely with the second stage characterised by Santantonio (1986) for shells of Simoceras (here Pseudovolanoceras) aesinense Meneghini, 1885 below 40 mm in size, except for earlier and comparatively accentuated “flared” external tubercles. On the assumption of confidence in the precise evaluation of the chambered part made by Cantú-Chapa (1990), his specimen could be a mature but nearly complete microconch—i.e., it is not a nucleus.

    The type of the Mexican specimen described by Verma and Westermann (1973) from the Alamitos section in northcentral Mexico is slightly distorted, inducing doubts as to its interpretation; hence new material would be of great importance for this purpose. Later interpretations (see above) concluded close relationships with the here interpreted P. aesinense (Meneghini, 1885) (e.g., Cecca 1999; Olóriz et al. 1996, 1999; Villaseñor et al. 2000a, b) or P. krantzense (Cantú-Chapa, 1990) (Schweigert et al. 2002). Taking into account the intra-species variability here interpreted for P. aesinense (Meneghini, 1885), including its geographical subspecies (see above), and the occurrence of traces of “cordone spirale” obscured by granular-phosphatic sediment preservation (Fig. 3G), two of the most typical “differences” argued for species level separation of this specimen become irrelevant. Thus, constrictions are astonishingly similar to those described by Meneghini (1885: 337), and variability in both periumbilical reinforcements and the timing of development (e.g., early outlined by Santantonio 1986) would clearly diminish problems when reinterpreting the specimen collected from Sierra de Catorce (north-central Mexico). In addition, close analysis of a plastic-cast of the Argentinean specimen and the type described by Verma and Westermann (1973) reveals closer resemblance of the latter with P. aesinense (Meneghini, 1885) in inner whorls coiling and ribbing, together with closer resemblance with the type described by Krantz (1928) in outer whorl sculpture and whorl section at the same shell size. All these observations support its reinterpretation as an intermediate phenotype between those identifiable in the types analysed by Meneghini (1885) and Krantz (1928), both of which are here held to evidence separate records of the same species resulting from biogeographical dynamics. As for the biochronostratigraphical interpretation of the Verma and Westermann (Verma and Westermann 1973) type gathered from the Rancho Los Alamitos section, San Luis Potosí, bed-by-bed sampled ammonite assemblages from the Virgatosphinctinae Beds allowed Olóriz et al. (1996, 1999) to identify discontinuous accumulation, most probably ranging from the late Virgatosimoceras albertinum/Neochetoceras darwini to the earliest Richterella richten chronozones in the Mediterranean Tethys. Thus, the most probable age for the Verma and Westermann (1973) type corresponds to the Semiformiceras semiformel Haploceras verruciferum Chronozone in the Secondary Standard for Mediterranean Tethys (e.g., Geyssant 1997).

  • Biochronostratigraphy.—The specimens described of Pseudovolanoceras aesinense chignahuapense (Cantú-Chapa, 1990) were collected from beds 21b, 22b and 25 in the Apulco section MT-2 and bed 11 form the Apulco section MTQ. In bed 21b of the Apulco River section MT-2 they are assembled to Simocosmoceras pszczolkowskii apulcoensis (Villaseñor and Olóriz 2001; Villaseñor et al. 2003), and in bed 11 of the nearby Apulco section MTQ registered together with Pseudhimalayites steinmanni (Haupt, 1907) (Villaseñor and Olóriz 2004). Housaites butti (Imlay, 1942) (Villaseñor and Olóriz 2009) was collected from the same stratigraphic interval in these two sections, and associated ammonites are Sublithacoceras, Parapallasiceras, Danubisphinctes (e.g., López-Caballero 2006) and haploceratids (Haploceras, Pseudolissoceras, and others) under study at present. The mentioned ammonite assemblages belong to a stratigraphic interval that correlates with an undetermined level within the Semiformiceras semiformel Haploceras verruciferum Chronozone in the Mediterranean Tethys.

  • Fig. 3.

    Simoceratin ammonoid Pseudovolanoceras aesinense chignahuapense (Cantú-Chapa, 1990) [M]. A. Left-side view of IGM 9555 from MTQ section, bed 11; arrows showing body chamber, and incipient longitudinal furrow between tubercles (see text for allusion to “cordone spirale”). BE from the Apulco section (MT-2). B. Left-side view of IGM 9547a, bed 22b. C. IGM 9545a, bed 22b. D. IGM 9545b, bed 22b. E. IGM 9548a, bed 21b. F. Simoceras aff. volanense Oppel, 1863 [type of Krantz 1928: pl. 3: 7; GPIBO 1 = Pseudovolanoceras aesinense krantzense (Cantú-Chapa, 1990)]; slightly oblique, right-side view of plastic mold; arrows for longitudinal furrow between tubercles (see text for allusion to “cordone spirale”). G. Simoceras cf. S. volanense (Oppel, 1863) [type of Verma and Westermann 1973: pl. 37: 2; IGM 2764 = Pseudovolanoceras aesinense (Meneghini, 1885) transitional form between Pseudovolanoceras aesinense chignahuapense (Cantú-Chapa, 1990) and Pseudovolanoceras aesinense krantzense (Cantú-Chapa, 1990)], close up view; arrows for longitudinal furrow between tubercles (see text for allusion to “cordone spirale”).


    Fig. 4.

    Simoceratin ammonoid Pseudovolanoceras aesinense chignahuapense (Cantú-Chapa, 1990) [microconch]. AF. From the Apulco section (MT-2). A. Right-side view of IGM 6085-2a showing lappet, bed 21b. B. Right-side view of IGM 9541; eroded and slightly distorted specimen, bed 21b. C. IGM 9543a, close-up view showing incipient longitudinal furrow between tubercles (C1) (see text for allusion to “cordone spirale”); right-side view (C2), bed 25. D, E. IGM 9546a and b, both from the same flattened inner mould. D. Imprint of the left side. E. Left-side view; arrows for lappet and tubercles showing riblets, bed 25. F. Left-side view of IGM 9542a, bed 21b. G. IGM 9544; G1, right-side view, arrow showing the last suture line preserved; G2, close-up view from the body chamber showing tubercles with riblets (arrows); G3, ventral view showing longitudinal furrow between tubercles, arrows indicate the trace of the “cordone spirale” (see text for allusion to “cordone spirale”); G4, close-up view of inner whorls showing tubercles with riblets (arrows); from MTQ section, bed 11.


    Fig. 5.

    Bivariate plots for shell features of simoceratin ammonoid Pseudovolanoceras aesinense chignahuapense (Cantú-Chapa, 1990) against shell diameter of Mexican, Cuban and Argentinean specimens. A. Umbilicus size (U). B. Size ratio between the umbilicus and shell diameter (U/D). C. Size ratio between whorl height and shell diameter (Wh/D). D. Periumbilical sculpture per half-a-whorl (PS/2). Shell diameter (D).


    Fig. 6.

    Bivariate plots for shell features of simoceratin ammonoid Pseudovolanoceras aesinense chignahuapense (Cantú-Chapa, 1990) and Pseudovolanoceras aesinense (Meneghini, 1885)against shell diameter in American and European assemblages. A. Umbilicus size (U). B. Size ratio between the umbilicus and shell diameter (U/D). C. Size ratio between whorl height and shell diameter (Wh/D). Shell diameter (D).


    Fig. 7.

    Periumbilical sculpture per half-a-whorl against shell diameter (PS/D) (shadow area indicates tubercles as inner sculpture) in simoceratin ammonoid Pseudovolanoceras aesinense chignahuapense (Cantú-Chapa, 1990) and Pseudovolanoceras aesinense (Meneghini, 1885).


    Fig. 8.

    Simoceratin ammonoid Pseudovolanoceras aesinense chiagnahuapense (Cantú-Chapa, 1990), suture lines. A. IGM 9555 [M], last incomplete suture at 70 mm of shell diameter. B. IGM 9544 [m], incomplete suture at 26.19 mm of shell diameter.


    Remarks on palaeobiogeography

    The occurrence of Lower Tithonian simoceratins in the Americas has been known since the early 20th century, and their relation with European (Tethyan) species has been progressively accepted. On the basis of present information, the occurrence of simoceratin species in the Americas is interpreted as relating the arrival of Tethyan (ubiquitous) taxa to available shelf environments in these areas, a phenomenon that largely involved ammonites throughout Jurassic times. This scenario is compatible with a general model for interpreting patterns of ammonoid biogeography (Olóriz 1985, 1990), identified in the Americas (Mexican areas included) under a rather variable degree of understanding (see Olóriz 1985, 1987, 1990, 1992; Leanza and Olóriz 1987; Olóriz et al. 1988, 1990; 1999; Leanza and Zeiss 1992; Cecca 1999; Parent and Capello 1999; Villaseñor et al. 2000a, 2003; Parent 2001; Villaseñor and Olóriz 2001, 2004, 2009, Parent et al. 2006, among others, for precise appliance of the model and/or compatible interpretations). A conceptual complement to this template is provided by assuming biogeographic dynamics as recognised from present cephalopods (e.g., Norman 2003; Yoshida et al. 2006; Bolstad 2009; Gillanders et al. 2009) and the potential application to past cephalopod records (e.g., Olóriz et al. 2006; Olóriz and Villaseñor 2010; and references therein)—see Notes on Simoceratinae chapter above.

    The occurrence of simoceratins in the Americas is associated with the most significant flooding recorded during the Early Tithonian (e.g., Olóriz et al. 1997, 1999; Villaseñor et al. 2003; and see Parent 2001 for biogeographic expansion of genus Pseudolissoceras). Support for this interpretation in Argentina are the records of Pseudovolanoceras aesinense krantzense (Cantú-Chapa, 1990) (Krantz 1928) together with Pseudhimalayites steinmanni (Haupt, 1907) (Krantz 1928) or with Pseudolissoceras zitteli Burckhardt, 1903 (Parent 2001), and of Simocosmoceras adversum andinum (Leanza and Olóriz, 1987), with Pseudhimalayites steinmanni (Haupt, 1907) (Leanza and Olóriz 1987), the latter reinterpreted as Pseudhimalayites subpretiousus (Uhlig, 1878) by Parent (2001). In Cuba, the only support available is the occurrence of P. aesinense (Meneghini, 1885) (nucleus illustrated by Imlay 1942) and Simocosmoceras sp. = Simocosmoceras pszczolkowskii Myczyński, 1989 (Myczyński 1989, 1990) according to the biochronostratigraphic interpretation made by Villaseñor and Olóriz (2001; see also Parent 2001). Villaseñor and Olóriz (2001) first described the occurrence of this genus in Mexico, later identified as Simocosmoceras pszczolkowskii apulcoensis Villaseñor, Olóriz, González-Arreola, 2003 (Villaseñor et al. 2003).

    In Mexico, there are data and interpretations in accordance with the hypotheses related to the model mentioned above (Olóriz 1985, 1990), compatible as well with interpretations in the palaeobiogeographical overview provided by Cecca (1999). Of special relevance are: (i) the single specimen of Simoceras cf. S. volanense (Oppel, 1863) reported by Verma and Westermann (1973) from Sierra de Catorce; (ii) the biochronostratigraphic interpretation of the encasing Virgatosphinctinae Beds in Olóriz et al. (1999); (iii) the interpretation of these deposits as related to the Early Tithonian flooding mentioned above (Olóriz 1992; Olóriz et al. 1996, 1999; Villaseñor et al. 2000b); (iv) the interpretation of the specimen of Sierra de Catorce as evidence of the occurrence of S. aesinense (Meneghini, 1885) in Mexico (e.g., Geyssant 1988; Cecca 1999; Oláriz et al. 1999; Villaseñor et al. 2000b), here reinterpreted as P. aesinense (Meneghini, 1885), an intermediate phenotype between subspecies P. aesinense chignahuapense (Cantú-Chapa, 1990) and P. aesinense krantzense (Cantú-Chapa, 1990); (v) the reinterpretation of the record of a microconchiate simoceratin in Puebla (Cantú-Chapa 1990) as P. aesinense chignahuapense (Cantú-Chapa, 1990) and its close relationships to earlier interpretations concluding in close P. aesinense (Meneghini, 1885) affinity or even belonging to the latter species (e.g., Cecca 1999, 2002a; Villaseñor et al. 2000a, b; Schweigert et al. 2002); (vi) the combined record of Simocosmoceras and simoceratins in the Mazatepec area (Villaseñor and Olóriz 2001; Villaseñor et al. 2003); and (vii) the record of Pseudhimalayites steinmanni (Haupt, 1907) and the simoceratin species P. aesinense (Meneghini, 1885) (Villaseñor and Olóriz 2004; see above for their combined record in Argentina). All this information evidences the inter-related occurrence of Early Tithonian floodings in the Americas and the occurrence of Tethyan simoceratin species, here interpreted at the genus level as belonging to Pseudovolanoceras.

    Whereas Mexico-Caribbean records of simoceratins (Pseudovolanoceras) and Simocosmoceras, assembled or not with Pseudhimalayites, accord with the hypothesis of faunal influence via the Hispanic Corridor, the record of Pseudovolanoceras aesinense krantzense (Cantú-Chapa, 1990) in Argentina, together with records of Simocosmoceras, Pseudhimalayites, and Pseudolissoceras within the Pseudolissoceras zitteli Biozone requires a more intricate configuration supporting the known palaeobiogeographic pattern of distribution of the species, or species complex, Pseudovolanoceras aesinense (Meneghini, 1885), in accordance with the assumed pattern of marine currents (e.g., Leanza and Olóriz 1987 for Simocosmoceras).

    The palaeobiogeographical pattern known for American simoceratins accords with the model proposed by Olóriz (1985, 1990), which was later acknowledged by Cecca (1999) and is compatible with more recent overviews on palaeobiogeographical interpretations (e.g., Cecca 2002b). Accordingly, incursions of peripheral populations of widespread cephalopods species, here the case of Pseudovolanoceras aesinense (Meneghini, 1885), into American neritic shelves would have occurred when and where these were available during relative sea-level rises, regardless of their palaeogeographic location within the range of marine influence of Tethyan water-masses, but according to the pattern of marine currents (e.g., Olóriz et al. 1997, 1999, 2000; Villaseñor et al. 2003; Olóriz and Villaseñor 2006). Widespread species, or species complexes without relevant phenotype differences, would be subjected to metacommunity and metapopulation dynamics (formally first proposed for ammonites by Olóriz et al. 2006, and treated in depth by Olóriz and Villaseñor 2010), and fragmentation of bioeographic ranges would depend on environmental dynamics. Aside from expatriation, rare relevant post-mortem transportation, and their combination, (perhaps the case of the single specimen registered of species V. schwertschlageri [Schneid, 1915], which is allocated inside giant Aspidoceras, as noted by Schweigert et al. 2002), vicariancy (fragmentation) and/or temporary, ancillary, selective vicariance (e.g., Olóriz et al. 2008) better explains local records of low-swimming cephalopods showing multispecies assemblies containing a variable percentage in combining local (i.e., endemics) and Tethyan and/or Tethyan-like taxa (i.e., ubiquitous colonisers with persistent phenotype expression).

    In this context, the explanation of Mexico-Caribbean records agrees with the role usually assumed for the Hispanic Corridor, but providing a regional example of the general dynamics, which supports the model proposed by Olóriz (1985, 1990) and its complement derived from information from present cephalopods (e.g., Olóriz and Villaseñor 2010). Hence, faunal expansion during flooding of neritic shelves forced phenotype deviation in simoceratin colonisers of Argentinean shelves (see Parent 2001 for Pseudolissoceras). Faunal capture resulting in subspeciation processes is here favoured to explain the occurrence of comparatively massive shells in Pseudovolanoceras aesinense krantzense (Cantú-Chapa, 1990), and other deviations such as those registered in eastern Mexico P. aesinense chignahuapense (Cantú-Chapa, 1990). Both of these cases reinforce the implications of Olóriz's (1985, 1990) model in terms of palaeobiologic response to a palaeobiogeographic dynamics promoting in situ evolution (e.g., Olóriz and Villaseñor 1999 for potential Early Tithonian example of species flock in neritic northcentral Mexico, and Olóriz et al. 2000 for a lower level phenotype influence in the same area). The Argentinean case reveals extreme phenotype expression, which cannot be related to hypermorphosis but rather to early innovation promoting massive shells without conclusive evidence, at present, of relative gigantism. Mexican records indicate phenotype deviation throughout the combination of heterochronic processes (acceleration) in microconchs, interpreted as resulting in allometric heterochrony (sensu McKinney 1988) since no precise information exists about the growth rate and age in these ammonites, and post-embryonic, late innovation.

    The case-study could thus reveal early phases of selective vicariance owing to the coeval co-existence of new and ancestral forms in a restricted part of the biogeographic range of the latter, with possible niche subdivision (ecospace reorganisation) and species fragmentation inside a heterogeneous environmental/palaeogeographical complex.

    On the basis of all the above, future research is encouraged to realise bed-by-bed sampling followed by palaeobiological and eco-evolutive interpretations of these ammonites in Mexico and Tethyan areas within the framework of a combined geo-biological approach.


    We acknowledge Fabrizio Cecca (University of Pierre et Marie Curie, Paris, France) and Andrzej Wierzbowski (University of Warsaw, Warsaw, Poland) for comments on the early draft of this paper. Martin Sander (Curator of Paleontology, Institut für Paläontologie Bonn, Germany) kindly provided us the cast of the type specimen described by Krantz (1928). Consuelo Macias and Antonio Altamira (both Institut of Geology, UNAM) assisted with photography, and Jane Sanders (Granada, Spain) provided linguistic assistance. This research was supported by PAPIIT IN 109208, CONACYT, Project 27555T, the Institute of Geology UNAM (Mexico), and Spanish MICINN projects BTE2001-3029, CGL2005-01316, CGL2008-05251-E/BTE, and CGL2008-3007 within the framework of the EMMI Group of the University of Granada (RNM 178, Junta de Andalucia, Spain).



    T. Adatte , W. Stinnesbeck , H.W. Hubberten , and J. Remane 1992. The Jurassic-Cretaceous boundary in Northeastern and Central Mexico. A multistratigraphical approach. III Congreso geologico de España y VIII Congreso Latinoamericano de Geología, Salamanca, Actas 4: 23–29. Google Scholar


    M. Benzaggagh , F. Cecca , and I. Rouget 2010. Biostratigraphic distribution of ammonites and calpionellids in the Tithonian of the internal Prerif (Msila area, Morocco). Palaöntologische Zeitschrift 84: 301–315. [CrossRef] Google Scholar


    D. Bernoulli and O. Renz 1970. Jurassic carbonate facies and new ammonites fauna from western Greece. Eclogae Geologicae Helvetiae 63: 573–607. Google Scholar


    K.S. Bolstad 2009. Systematics of the Onychoteuthidae Gray, 1847 (Cephalopoda: Oegopsida). Cephalopod International Advisory Council—CIAC Symposium Vigo, Spain, Symposium session: Systematics, Biogeography and Biodiversity, Abstracts, 33. Cephalopod International Advisory Council, Vigo. Google Scholar


    J.H. Callomon 1969. Dimorphism in Jurassic ammonites. In : G.E.G. Westermann (ed.), Sexual Dimorphism in Fossil Metazoa and Taxonomic Implications, 111–121. International Union of Geological Sciences, Serie A 1. E. Schweizerbart'sehe Verlagsbuchhandlung, Stuttgart. Google Scholar


    J.H. Callomon 1992. Upper Jurassic, especially Mexico. In : G.E.G. Westermann (ed.), The Jurassic of the Circum Pacific, Part 4, Biochronology, Ammonite Zones of the Circum-Pacific Region , 261–272. Cambridge University Press, New York. Google Scholar


    A. Cantú-Chapa 1967. El limite Jurásico—Cretácico en Mazatepec, Puebla. Estratigrafía del Jurásico de Mazatepec, Puebla (México). Instituto Mexicano de Petróleo, Sección Geología, Monografía 1: 3–24. Google Scholar


    A. Cantú-Chapa 1971. La Serie Huasteca (Jurásico Medio-Superior) del Centro-Este de México. Revista del Instituto Mexicano del Petróleo 3: 17–40. Google Scholar


    A. Cantú-Chapa 1989. Precisiones sobre el limite Jurásico-Cretácico en el subsuelo del Este de Máxico. Revista de la Sociedad Mexicana de Paleontología 2: 26–65. Google Scholar


    A. Cantú-Chapa 1990. Volanoceras chignahuapense sp. nov., amonita del Titoniano inferior de Puebla, Centro de México. Revista de la Sociedad Mexicana de Paleontología 3: 41–45. Google Scholar


    J. Caracuel , F. Olóriz , and C. Sarti 1998. Updated biostratigraphy of the Kimmeridgian and Lower Tithonian at Lavarone (Trente Plateau, Italy). Correlation for epioceanic western Tethys. Geologica et Palaeontologica 32: 235–251. Google Scholar


    F. Cecca 1999. Palaeobiogeography of Tethyan ammonites during the Tithonian (latest Jurassic). Palaeogeography, Palaeoclimatology, Palaeoecology 147: 1–37. [CrossRef] Google Scholar


    F. Cecca 2002a. Family Simoceratidae Spath, 1924. In : G. Pavia and S. Cresta (eds.), Revision of Jurassic Ammonites of the Gemmellaro Collections. Quaderni del Museo Geologico «G.G. Gemmellaro» 6: 363–364. Google Scholar


    F. Cecca 2002b. Palaeobiogeography of Marine Fossil Invertebrates. 273 pp. Taylor and Francis, London. Google Scholar


    F. Cecca , S. Cresta , and M. Santantonio 1983. Ammoniti del Malm dell'Appennino Marchigiano conservate nel Museo del Servizio geologico d'Itallia. Bolletino del Servizio Geologico d'Italia 102 (for 1981): 109–132. Google Scholar


    F. Cecca , S. Cresta , G. Pallini , and M. Santantonio 1986. Biostratigrafia ed ammoniti del Dogger — Malm di Colle Tordina (Monti della Rossa, Appennino Marchigiano). Bolletino del Servizio Geologico d'ltalia 104 (for 1983–1984): 177–204. Google Scholar


    R. Colacicchi and G. Piallini 1967. Dati a conferma di una lacuna dovuta ad emersione nel Giurese di Monte Cucco (Appennino Umbro). Bolletino della Societe Geologique d'Italia 86: 179–192. Google Scholar


    I. Fözy 1987. Upper Jurassic ammmonite biostratigraphy in the Transdanubian Central Range (Hungary). Preliminary results. Annales Universitatis Scientiarum Budapestinensis de Rolando Eötvös nominatae 27: 67–78. Google Scholar


    I. Fözy 1988. Tithonian ammonites (Oppelidae, Haploceratidae and Simoceratidae) from the Transdanubian Central Range, Hungary. Annales Universitatis Scientiarum Budapestinensis de Rolando Eötvös nominatae 28:43–119. Google Scholar


    I. Fözy 1990. Ammonite succession from three Upper Jurassic sections in the Bakony Mts. (Hungary). In : G. Pallini , F. Cecca , S. Cresta , and M. Santantonio (eds.), Atti III Convengo Internazionale Fossili, Evoluzione Ambiente, 323–339, Pergola, Italy. Google Scholar


    I. Fözy , M. Kézmér , and I. Szente 1994. A unique Lower Tithonian fauna in the Gerecse Mts., Hungary. Palaeopelagos, Special Publication 1: 155–165. Google Scholar


    J.R. Geyssant 1979. Evolution, Systematics and Dimorphism of a new genus of ammonite: Baeticoceras (Ammonitina, Simoceratinae) in the Upper Tithonian of the Betic Range. Palaeontographica 166: 1–36. Google Scholar


    J.R. Geyssant 1982. L'équilibre intermittent: une modalité dévolution présente chez les Simoceratidae (ammonites du Tithonique). 9e Réunion Annuelle des Sciences de la Terre, Paris, 275. Société Géologique de France, France. Google Scholar


    J.R. Geyssant 1985. Révision taxonomique de genre d'ammonite Téthysien Simoceras et création d'un nouveau genre Volanoceras (Ammonitina, Simoceratidae). Geobios 18: 677–680. [CrossRef] Google Scholar


    J.R. Geyssant 1988. Diversity in Mode and Tempo of evolution within one Tithonian ammonite family, the Simoceratids. In : J. Wiedmann and J. Kullmann (eds.), 2nd International Cephalopod Symposium, Cephalopods Present and Past , 79–88. Schweizerbart'sehe Verlagsbuchhandlung, Stuttgart. Google Scholar


    G. Geyssant 1997. Tithonien. In : E. Cariou and P. Hantzpergue (coords.), Biostratigraphie du Jurasique Ouest-Européen et Méditerranéen. Zonations parallèles et distribution des invertébrés et microfossiles. Groupe Français Etude Jurassique. Bulletin du Centre de Recherches Elf Exploration-Production, Mémoir 17: 98–102. Google Scholar


    B.M. Gillanders , M.C. de Vries , and S.C. Donnellan 2009. Giant Australian cuttlefish: population structure, a species complex and potential impacts. Cephalopod International Advisory Council—CIAC Symposium Vigo, Spain, Symposium session: Genetics and Evolution, Abstracts , p. 38. Cephalopod International Advisory Council, Vigo. Google Scholar


    R. Hernández de la Fuente 1996. Sedimentología y diagénesis del Kimmeridgiano en la región de Jonotla, Puebla y Tlacolula, Veracruz. 82 pp. Unpublished M.Sc. thesis. Universidad Nacional Autónoma de Mexico, Mexico. Google Scholar


    R.W. Imlay 1942. Late Jurassic fossils from Cuba and their economic significance. Bulletin of the Geological Society of America 53:1417–1477. Google Scholar


    F. Krantz 1928. La Fauna del Titono superior y medio de la parte meridional de la provincia de Mendoza. Actas de la Academia Nacional de Ciencias, República de Argentina 10: 1–57. Google Scholar


    H.A. Leanza and C.A. Hugo 1977. Sucesión de ammonites y edad de la Formación Vaca Muerta y sincrónicas entre los paralelos 35° y 40° l.s. Cuenca Neuquina-Mendocina. Revista de la Asociación Geológica Argentina 32:248–264. Google Scholar


    H. Leanza and F. Olóriz 1987. Presencia del género Simocosmoceras Spath (Cephalopoda, Ammonoidea) en el Tithoniano Andino y su significado paleobiogeografico. Ameghiniana 24: 203–209. Google Scholar


    H. Leanza and A. Zeiss 1990. Upper Jurassic Lithographic Limestones from Argentina (Neuquen Basin): Stratigraphy and Fossils. Facies 22: 169–186. [CrossRef] Google Scholar


    H. Leanza and A. Zeiss 1992. On the ammonite fauna of the Lithographic Limestones from the Zapala region (Neuquén Province, Argentina), with the description of a new genus. Zentralblatt für Geologie und Paläontologie 1: 1841–1850. Google Scholar


    H. Leanza and A. Zeiss 1994. The “Lithographic limestones” of Zapala (Central Argentina) and their Ammonite fauna. Geobios, Mémoire Spéciel 16: 245–250. [CrossRef] Google Scholar


    I. López-Caballero 2006. Estudio bioestratigráfico de la fauna de ammonites del Jurásico Superior del área de Mazatepec, Puebla. 125 pp. Unpublished under-graduate thesis, Universidad Nacional Autónoma de México, Mexico. Google Scholar


    I. López-Caballero , A.B. Villaseñor , and F. Olóriz 2007. Sobre una asociacion de ammonites del jurásico superior (Tithonico) de Mazatepec, Puebla, México. In : E. Díaz-Martínez and I. Rábano (eds.), 4th European Meeting on the Palaeontology and Stratigraphy of Latin America. Cuadernos del Museo Geominero 8: 245–249. Google Scholar


    E. López-Ramos 1979a. Geología de México. 2. 3a edición. 454 pp. Edición Escolar, México. Google Scholar


    E. López-Ramos 1979b. Geología de México. 3. 3a edición. 453 pp. Edición Escolar, México. Google Scholar


    M.L. McKinney 1988. Classifying heterochrony: allometry, size, and time. In : M.L. McKinney (ed.), Heterochrony and Evolution , 17–34. Plenum Press, New York. Google Scholar


    G. Meneghini 1885. Nuove ammoniti dell'Appennino Centrale raccolte dal Reverendo Don A. Moriconi. Memoire Atti della Societa Toscana di Scienze Naturali 6: 363–382. Google Scholar


    R. Myczyński 1989. Ammonite biostratigraphy of the Tithonian of western Cuba. Annales Societatis Geologorum Poloniae 59: 43–125. Google Scholar


    R. Myczyński 1990. Simocosmoceras Spath (Perisphinctidae, Ammonitina) in the Lower Tithonian of the Sierra del Rosario (Western Cuba). In : G. Pallini , F. Cecca , S. Cresta , and M. Santantonio (eds.), Atti III Convengo Internazionale Fossili, Evoluzione Ambiente, 401–403. Pergola, Italy. Google Scholar


    G.J. Nelson , and N.I. Platnick 1981. Systematics and Biogeography: Cladistics and Vicariance. 567 pp. Columbia University Press, New York. Google Scholar


    U. Nicosia and G. Pallini 1977. Hermatypic corals in the Tithonian pelagic facies of Central Appennines. Evidences of Upper Jurassic sea-level changes. Geologica Romana 16: 243–261. Google Scholar


    M. Norman 2003. Cephalopods a World Guide: Octopuses, Argonauts, Cuttlefish, Squid, and Nautilus. 320 pp. Conch Books, Hackenheim, Germany. Google Scholar


    F. Olóriz 1978. Kimmeridgiense-Tithonico inferior en el sector central de las cordilleras Béticas. Zona Subbética. Paleontología. Bioestratigrafía. 758 pp. Unpublished Ph.D. thesis, Colección Tesis Doctorales de la Universidad de Granada, no. 184, Granada. Google Scholar


    F. Olóriz 1985. Paleogeography and ammonites in the Upper Jurassic. Outlines for a pattern. In: G. Pallini (ed.), Atti I Convengo di Pergola Fossili, Evoluzione, Ambiente, 1–9. Comitate Centenario Raffaele Piccinini, Pergola, Italy. Google Scholar


    F. Olóriz 1987. El significado biogeográfico de las plataformas mexicanas en el Jurásico superior. Consideraciones sobre un modelo eco-evolutivo. Revista de la Sociedad Mexicana de Paleontología 1: 219–247. Google Scholar


    F. Olóriz 1990. Ammonite Phenotypes and Ammonite Distributions. Notes and Comments. In : G. Pallini , F. Cecca , S. Cresta , and M. Santantonio (eds.), Atti III Convengo Internazionale Fossili, Evoluzione Ambiente , 417–426, Pergola, Italy. Google Scholar


    F. Olóriz 1992. North-central and eastern Mexico. In : G.E.G. Westermann (ed.), The Jurassic of the Circum-Pacific, Part 3, Regional Geology and Stratigraphy, Meso-America , 100–107. Cambridge University Press, New York. Google Scholar


    F. Olóriz and J.M. Tavera 1979. Nuevo Simoceratinae—Simoceras (Cordubiceras) — en la base del Tithonico superior de las Cordilleras Béticas (Zona Subbética). Tecniterrae 29: 1–5. Google Scholar


    F. Olóriz and A.B. Villaseñor 1999. New microconchiate Hybonoticeras from Mexico. Geobios 32: 561–573. [CrossRef] Google Scholar


    F. Olóriz and A.B. Villaseñor 2006. Ceratosphinctes (Ammonitina, Kimmeridgian) in Mexico: from rare but typical inhabitant of west-Tethyan epioceanic and epicontinental waters to a geographically widespread ammonite genus. Geobios 39: 255–266. Google Scholar


    F. Olóriz and A.B. Villasenor 2010. Ammonite biogeography: from descriptive to dynamic, ecological interpretations. In : K. Tanabe , Y. Shigeta , T. Sasaki , and H. Hirano (eds.), Cephalopods-Present and Past , 253–265. Tokai University Press, Tokyo. Google Scholar


    F. Olóriz , M. Boughdiri , and B. Marques 2006. Remarks on relative phenotype stability in two Tithonian ammonite species first described from the Tunisian Dorsale—a preliminary approach to interpreting metapopulation dynamics in ammonites. Neues Jahrbuch für Geologie und Paläontologie 241: 287–302. Google Scholar


    F. Olóriz , B. Marques , and L. Moliner 1988. The platform effect: an example from Iberian shelf areas in the Lowermost Kimmerdigian. In : R.B. Rocha and A.F. Soares (eds.), Proceedings Second International Symposium on Jurassic Stratigraphy I, 545–562. Instituto Nacional de Investigaçâo Cientifica, Lisbon. Google Scholar


    F. Olóriz , A.B. Villasenor , and C. González-Arreola 1997. Factors controlling Upper Jurassic ammonite assemblages in North-Central Mexico. Lethaia 30: 337–351. [CrossRef] Google Scholar


    F. Olóriz , A.B. Villasenor , and C. Gonzalez-Arreola 2000. Geographic control on phenotype expression. The case of Hybonoticeras mumdulum (Oppel) from the Mexican Altiplano. Lethaia 33: 157–174. [CrossRef] Google Scholar


    F. Olóriz , A.B. Villaseñor , and I. López-Palomino 2008. Middle Oxfordian ammonite biostratigraphy of the Lower Santiago Formation at Tamán, San Luis Potosí, Mexico—with notes on Mexico-Caribbean ochetoceratins. Revista Mexicana de Ciencias Geológicas 25: 261–283. Google Scholar


    F. Olóriz , A.B. Villaseñor , C. González , and G.E.G. Westermann 1990. Las plataformas mexicanas durante el Jurásico superior. Un ejemplo de áreas de recepción en biogeografía. In : J. Civis Llovera and J.A. Flores Villarejo (eds.), Actas de Paleontología, Salamanca 1990: 277–287. Google Scholar


    F. Olóriz , A.B. Villaseñor , C. González-Arreola , and G.E.G. Westermann 1996. Interpreting updated ammonite biostratigraphy. The Upper Jurassic—Lowermost Cretaceous in the Alamitos area. Sierra de Catorce, San Luis Potosí (North-central Mexico). In : F. Olóriz and F.J. Rodríguez-Tovar (eds.), Fourth International Symposium Cephalopods Present and Past, Abstracts , 134–136. Universidad de Granada, Granada. Google Scholar


    F. Olóriz , A.B. Villaseñor , C. González-Arreola , and G.E.G. Westermann 1999. Ammonite biostratigraphy and correlations in the Late Jurassic—Earliest Cretaceous La Caja Formation of North-Central Mexico (Sierra de Catorce, San Luis Potosí). In : F. Olóriz and F.J. Rodríguez-Tovar (eds.), Advancing Research on Living and Fossil Cephalopods , 463–492. Kluwer Academic/Plenum Publishing Corporation, New York. Google Scholar


    A. Oppel 1862–63. Ueber jurassische Cephalopoden. Palaontologische Mitteilungen aus dem Museum des Koenigliche Bayer, Staates 3: 127–266. Google Scholar


    F. Ortega-Gutiérrez , L.M. Mitre-Salazar , J. Roldán-Quintana , J.J. Aranda-Gomez , D. Morán-Zenteno , S.A. Alaniz-Álvarez , and A.F. Nieto-Samaniego 1992. Texto explicativo de la quinta edición de la carta geológica de la república mexicana Escala 1: 2000000. Universidad Nacional Autonoma de México, Mexico. Google Scholar


    H. Parent 2001. The Middle Tithonian (Upper Jurassic) ammonoid fauna of Cañadón de los Alazanes, Southern Neuquén-Mendoza Basin (Argentina). Boletín del Instituto de Fisiografía y Geología 71: 19–38. Google Scholar


    H. Parent and O.D. Capello 1999. Amonites del Tithoniano inferior de Casa Pincheira, Mendoza (Argentina). Revue de Paléobiologie 18: 347–353. Google Scholar


    H. Parent , A. Scherzinger , and G. Schweigert 2006. The earliest ammonite faunas from the Andean Tithonian of the Neuquen-Mendoza Basin, Argentina-Chile. Neues Jarhbuch für Geologie und Palaontologie Abhandlungen 241: 253–267. Google Scholar


    M. Ridley 1989. The cladistic solution to the species problem. Biology and Philosophy 4: 1–16. [CrossRef] Google Scholar


    F. Rossi 1984. Ammoniti del Kimmeridgiano superiore-Berriasiano inferiore del Paso del Furlo (Appennino umbro-marchigiano). Memorie della Società italiana di Scienze naturali e del Museo civico di Storia naturale di Milano 23: 73–136. Google Scholar


    M. Santantonio 1986. Simoceras volanense (Oppel), Simoceras aesinense Meneghini e forme affini nel Titonico inferiore dell'Appennino umbromarchigiano. In : G. Pallini (ed.), Atti I Convengo Internazionale Fossili, Evoluzione Ambiente. Comitato Centenario Raffaele Piccinini , 11–23. Pergola, Italy. Google Scholar


    T. Schneid 1915. Die Ammonitenfauna der Obertithonischen Kalke von Neuburg A. D. Geologische und Paläontologische Abhandlungen, Neue Folge, Band 13: 305–400. Google Scholar


    G. Schweigert , A. Scherzinger , and H. Parent 2002. The Volanoceras lineage (Ammonoidea, Simoceratidae)—a tool for long-distance correlations in the Lower Tithonian. Stuttgarter Beitrage zur Naturkunde, Serie B (Geologie und Palaontologie) 326: 1–43. Google Scholar


    A. Seilacher , F. Andalib , G. Dietl , and H. Gocht 1976. Preservational history of compressed Jurassic ammonites from southern Germany. Neues Jahrbuch für Geologie und Paläontologie, Abhandlungen 152: 307–356. Google Scholar


    W. Stinnesbeck , T. Adatte , and J. Remane 1993. Mazatepec (Estado de Puebla, México) — Reevaluación de su valor como estratotipo del Límite Jurásico—Cretácico. Revista Española de Micropaleontología 24: 63–79. Google Scholar


    M. Suter 1990. Geología de la hoja de Tamazunchale, Estado de Hidalgo, Querétaro y San Luis Potosí. 57 pp. Instituto de Geología, Universidad Nacional Autónoma de México, Mexico. Google Scholar


    A. Templeton 1989. The meaning of species and speciation: A genetic perspective. In : D. Otte and J. Endler (eds.), Speciation and its Consequences, 3–27. Sinauer, Sunderland (MA). Google Scholar


    L. Van Valen 1976. Ecological species, multispecies, and oaks. Taxon 25: 233–39. [CrossRef] Google Scholar


    H. Verma and G.E.G. Westermann 1973. The Tithonian (Jurassic) ammonite fauna and stratigraphy of Sierra Catorce, San Luis Potosí, Mexico. Bulletins of American Paleontology 63: 107–320. Google Scholar


    A.B. Villaseñor and F. Olóriz 2001. Combined record of Simocosmoceras and Simoceras (Ammonitina) in Mexico. International Conference on Paleobiogeography and Paleoecology, Abstracts, 131–132. Cassa di Risparmio di Parma & Piacenza, Gruppo Intesa, Piacenza and Castell' Arquato. Google Scholar


    A.B. Villaseñor and F. Olóriz 2004. First occurrence of genus Pseudhimalayites Spath (Ammonitina) in Mexico. 6th International Symposium Cephalopods Present and Past, Abstracts, 151–152. Fayetteville, Arkansas. Google Scholar


    A.B. Villaseñor and F. Olóriz 2009. Caribbean Lower Tithonian ammonites from central-east Mexico. Geobios 42: 117–132. [CrossRef] Google Scholar


    A. B. Villaseñor , F. Olóriz , and C. González-Arreola 2000a. Simoceras aesinense (Meneghini). A biomarker for significant floodings during Early Tithonian. Annual Meeting of the Geological Society America, Abstracts with Programs, A-469. Geological Society of America, Incorporated, Reno, Nevada. Google Scholar


    A.B. Villaseñor , F. Olóriz , and C. González-Arreola 2000b. Recent advances in Upper Jurassic (Kimmeridgian—Tithonian) ammonite biostratigraphy from North-Central Mexico based on new collected ammonite assemblages. GeoResearch Forum 6: 249–262. Google Scholar


    A.B. Villaseñor , F. Olóriz , and C. González-Arreola 2003. First record of the genus Simocosmoceras Spath, 1925. Ammonitina, in Mexico. Biostratigraphic and palaeobiogeographic interpretation. GFF 125: 49–56. Google Scholar


    M.M. Yacobucci 1999. Plasticity of developmental timing as the underlying cause of high speciation rates in ammonoids. An example from the Cenomanian Westen Interior Seaway of North America. In : F. Olóriz and F.J. Rodríguez-Tovar (eds.), Advancing Research on Living and Fossil Cephalopods, 59–76. Kluwer Academic/Plenum Publishers, New York. Google Scholar


    M. Yoshida , K. Tsuneki , and H. Furuya 2006. Phylogeny of selected Sepiidae (Mollusca, Cephalopoda) on 12S, 16S, and COI Sequences, with comments on the taxonomic reliability of several morphological characters. Zoological Science 23: 341–351. [CrossRef] Google Scholar


    K.A. Zittel 1870. Die Fauna der älteren cephalopodenführenden Tithonbildungen. Palaeontographica 2 (Supplement 1): 1–192. Google Scholar


    Appendix 1

    Appendix 1

    Measurements of Pseudovolanoceras aesinense chignahuapense (Cantú-Chapa, 1990), Pseudovolanoceras aesinense krantzense (Cantú-Chapa, 1990), and European specimens of Pseudovolanoceras aesinense (Meneghini, 1885) (e.g., Santantonio, 1986; Cecca et al. 1981, 1986; Schweigert et al. 2002).




    Appendix 2

    Annotated synonymy list for Pseudovolanoceras aesinense (Meneghini, 1885) including the geographic subspecies mentioned in text; exclusive for citations with illustrated specimens.

    Pseudovolanoceras aesinense (Meneghini, 1885)

    • 1870 Simoceras volanense Oppel, 1863; Zittel 1870: 95, pl. 32 [supplement: pl. 8]: 7 [macroconch; only outer whorls?], non 8, 9. From Lower Tithonian pelagic cephalopod limestone in central Apennines (Monte Catria, Marche), Italy.

    • 1885 Simoceras cfr. volanense Oppel, 1863 sp. (var. aesinense nov.); Meneghini 1885: 376, pl. 20: 4a–d [macroconch]. From Lower Tithonian pelagic cephalopod limestone in central Appenines, Marche, Italy.

    • 1928 Simoceras aff. volanense Oppel, 1863; Krantz 1928: 13, pl. 3: 7 [macroconch]. From the Lower Tithonian, Pseudolissoceras ziteli Chronozone (= Semiformiceras semiforme/Haploceras verruciferum Chronozone) calcareous horizons/concretion in the Vaca Muerta Fm., southern Mendoza, Argentina.

    • 1942 Simoceras sp. juv. cf. S. volanense (Oppel, 1863); Imlay 1942: 1445, pl. 3: 2, 3 [juvenile, incomplete micro- or macroconch]. From the Lower Tithonian black to gray, siliceous, shaly and locally sandy Vinales Limestone Fm. in Santa Clara Provinve, Central Cuba.

    • 1967 Aspidoceras phoenicium Gemmellaro, 1871; Colacicchi and Pialli 1967: 184–186, figs. 2e, 3b [macroconchs]. From Lower Tithonian, fossil rich interval (lumachella) in Monte Cucco, central Appenines; Umbria, Italy.

    • 1970 Simoceras sp. group of S. volanense (Oppel, 1863); Bernoulli and Renz 1970: 600, pl. 5: 4–6 [macroconch]. From Lower Tithonian condensed, pelagic cephalopod limestone in Louros Valley, western Greece.

    • 1973 Simoceras cf. S. volanense (Oppel, 1863); Verma and Westermann 1973: 196, pl. 37: 2a, b [macroconch]. From phosporitic, silty limestones (Virgatosphinctinae Beds) in Sierra de Catorce, north-central Mexico.

    • 1977 Aspidoceras phoenicium Gemmellaro, 1871; Nicosia and Pallini 1977: pl. 2: 9 [macroconch]. From Lower Tithonian cephalopod limestones in central Appenines, Umbria-Marche, Italy.

    • 1978 Simoceras (Simoceras) volanense schwertschlageri (Schneid, 1915); Olóriz 1978: 224, pl. 20: 3?, 6? (partim) [macroconchs]. From the upper Haploceras verruciferum Chronozone nodular limestone and the uppermost Haploceras verruciferum-to-lower-most Richterella richteri chronozones cephalopod-rich pelagic limestone (condensed horizon?) in the Middle and Internal Subbetic (southern Spain), respectively.

    • 1983 Simoceras (Simoceras) volanense (Oppel, 1863); Cecca et al. 1983: 119, pl. 3: 1a, b [macroconch]. From the Lower Tithonian pelagic cephalopod limestone in central Appenines, Marche, Italy.

    • 1984 Simoceras (Simoceras) volanense (Oppel, 1863); Rossi 1984: 115, pl. 35: 12 [macroconch]. From the Lower Tithonian cephalopodrich pelagic limestone (Grigio Ammonitico) in central Appenines, Umbria-Marche, Italy.

    • 1986 Simoceras aesinense Meneghini, 1885; Santantonio 1986: 15, pl. 1: 1–4 [figs. 13 macroconchs; fig. 4 microconch], pl. 2: 1–4, 6. [figs. 2, 3 and 6 macroconchs; figs. 1, 4 microconchs]. From Lower Tithonian S. semiforme/H. verruciferum Chronozone pelagic cephalopod limestones in central Appenines and nodular limestones in southern Alps Italy.

    • 1986 Simoceras aesinense Meneghini, 1885; Cecca et al. 1986: 196, pl. 7: 1, 3 [macroconchs]. Lower Tithonian S. semiforme/H. verruciferum Chronozone pelagic cephalopod limestone in central Apeninnes, Marche, Italy.

    • 1987 Simoceras aff. volanense (Oppel, 1863); Fözy 1987: pl. 1: 1 [= Fözy 1988: pl. 10: 2; macroconch]. From Lower Tithonian S. semiforme/H. verruciferum Chronozone red nodular limestone in Bakony Mountains, Hungary.

    • 1988 Volanoceras (Volanoceras) aesinense (Meneghini, 1885); Fözy 1988: 73, pl. 8: 3, 4 [macroconchs; fig. 4 = Fözy 1990: pl. 3: 2], pl. 9: 1–3 [macroconchs], pl. 10: 2 [= Fözy 1987: pl. 1: 1; macroconch]. From Lower Tithonian S. semiforme/H. verruciferum Chronozone red nodular limestone in the Bakony and Gerecse Mountains, Hungary.

    • 1990 Volanoceras (Volanoceras) aesinense (Meneghini, 1885); Fözy 1990: 327, pl. 3: 2 [= Fözy 1988: pl. 8: 4; macroconch]. From Lower Tithonian S. semiforme/H. verruciferum Chronozone red nodular limestone in Bakony Mountains, Hungary.

    • 1990 Volanoceras chignahuapense Cantú-Chapa, 1990: 41, fig. 2a–d [microconch]. From Lower Tithonian loosed calcareous concretion in the Tamán Fm., Sierra Madre, eastern Mexico].

    • ?1994 Volanoceras cf. aesinense (Meneghini, 1885); Fözy et al. 1994: 156, 158, pl. 2: 16 [fragmented nucleus of inconclusive interpretation]. From Lower Tithonian S. semiforme/H. verruciferum Chronozone, crinoid-ammonite coquina packestone (Hierlatz limestone) in the Gerecse Mountains, Hungary.

    • 1998 Simoceras aesinense Meneghini, 1885; Caracuel et al. 1998: 240, 244, pl. 2: 4 [macroconch]. Lower Tithonian S. semiforme/H. verruciferum Chronozone red nodular limestone in the Venetian Alps, Italy.

    • 2002 Volanoceras aesinense (Meneghini, 1885); Schweigert et al. 2002: 8, pl. 1: 1–4 [figs. 13 macroconchs; fig. 4 fragmented nucleus of macro- or microconch]. Lower Tithonian S. semiforme/ H. verruciferum Chronozone red nodular limestone in External Subbetic (southern Spain), pelagic cephalopod limestone in central Apennines (Italy), and the Rogoźnik Coquina Mb. of the Czorsztyn Fm. in Polish Carpathians (Poland).

    • 2002 Volanoceras krantzense Cantú-Chapa, 1990; Schweigert et al. 2002: 9, pl. 2: 1, non 2 (= fig. 1 in the plate caption) (partim) [macroconchs]. From the Lower Tithonian, Pseudolissoceras zitteli Chronozone (= S. semiforme/H. verruciferum Chronozone) calcareous horizon/concretion in the Vaca Muerta Fm., southern Mendoza, Argentina.

    Ana B. Villaseñor, Federico Olóriz, and Celestina González-Arreola "Lower Tithonian Microconchiate Simoceratins from Eastern Mexico: Taxonomy, Biostratigraphy, and Palaeobiogeography," Acta Palaeontologica Polonica 56(1), 133-158, (1 March 2011).
    Received: 22 March 2010; Accepted: 26 July 2010; Published: 1 March 2011
    Upper Jurassic
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