Cenomanian transgression in the Basque-Cantabrian Basin (northern Spain) and associated faunal replacement.
Environmental changes and faunal replacement are highly complex processes, in which many factors of diverse origins are involved. As a consequence, any attempt to understand these phenomena requires complementary sedimentological, stratigraphical, and palaeontological evidence. The aim of this paper is to examine the palaeoenvironmental changes occurred during the marine transgression of the Cenomanian in the North of Iberia. New stratigraphic data are presented and discussed, together with a reassessment of previous data. New additions to the fossil record are integrated into the stratigraphy in order to understand the time and nature of the faunal replacement during the Early to Late Cretaceous transition in the North of Iberia; evolutionary implications are briefly discussed.
The Cenomanian stage is characterised by a major firstorder sea-level rise (Haq et al., 1987), which resulted in the flooding of continental areas and in the development of widespread shallow marine depositional settings. This new oceanographic scenario led to faunal turnovers in groups like ammonites (e. g., Wright et al., 1996) and teleostean fishes (e. g., Arratia, 2000). Studies on sequence stratigraphy from separated marine Cenomanian successions with a high-resolution ammonite biostratigraphy have demonstrated that sea-level changes are globally synchronous and therefore eustatic in origin (Anglo-Paris basin, Robaszynski et al., 1998; India and northwest Europe, Gale et al., 2002; southwest Morocco, Kuhnt et al., 2009). Therefore, the signature of global oceanographic changes could be recognized in the sedimentary and palaeontological record of separated sedimentary basins. Our study area is placed in the northern Iberian margin of the Basque-Cantabrian Basin (BCB), an area located between Africa and Europe. Cenomanian sedimentation in the BCB occurred on tectonic blocks with differential subsidence postdating a more active tectonic subsidence phase during the Albian (e. g., Garcia-Mondejar et al., 2004; Floquet, 2004). This led to the development of widespread carbonate ramps with differential stratigraphic records. We present here new faunal data and an updated biostratigraphy-based correlation of shallow-to-deep marine successions of the latest Albian-Cenomanian in the middle part of the Basque-Cantabrian Basin (e. g., Rodriguez-Lazaro et al., 1998; Grafe and Wendler, 2003; Barroso-Barcenilla et al., 2011a, 2011b). This correlation has been the key framework to understand the onset of the great transgression that lasted until Santonian times. A remarkable specimen of a teleostean pachyrhizodontid fish and a new specimen of the ammonite Calycoceras (Newboldiceras) asiaticum spinosum (Kossmat, 1897) are reported from the same level in a carbonate ramp succession in Aiara, west of Amurrio (Araba province, Basque Country, Spain). The fossil fish specimen is the first report of the order Crossognathiformes from the Iberian Peninsula. The stratigraphy of the fish-bearing shallow marine carbonate succession is compiled and revised here in order to provide an accurate stratigraphical and palaeoecological context for the newly reported fauna.
2. Material and methods
2.1. Field work
Herein we provide new data from the latest Albian-Cenomanian succession of the Amurrio and Leioa areas (Fig. 1), consisting of the measurement of partial successions and their correlation to the succession of the Cidad-Puentedy area (Figs. 1-3). We have distinguished the main stratigraphic units in the Amurrio area following the nomenclature of Lotze (1960), and chosen two well outcropped stratigraphic markers for correlation. The stratigraphic markers are the base of a marl-limestone alternation (base of Lower Campillo beds, A in figs. 2 and 3) and the top of a calcarenite interval (basal Hijuela beds, B in figs. 2 and 3). These stratigraphic markers were the key for field and cartography-based correlation with the well dated Villasana Cenomanian succession (e. g., Wiedmann, 1979; Grafe and Wendler, 2003) located west of Amurrio. The new ammonite data have permitted a re-assessment of the ammonite biostratigraphy in the study area. The integration of the biostratigraphical data from the mentioned areas has been the basis for the shallow-to-deep basin correlation (Fig. 3).
The new specimen of ammonite reported here occurred together with fragmentary undetermined inoceramids in fishbearing beds. It is an incomplete internal mould composed of marly limestone as the bearing sediment; this preservation and the lack of tractive sedimentary structures indicates that this specimen is autochthonous. It is deposited in the Museo de Ciencias Naturales de Alava / Arabako Natur Zientzien Museoa (repository MCNA 14392).
New occurrences of Late Albian ammonites near Amurrio (Ziorraga locality) and Ordunte (Balmaseda locality), and in the Leioa area (Ondiz locality) are currently under study and are here only considered to put the Albian-Cenomanian change in the ammonite associations into a proper context.
The fish specimen reported here is labelled Aztarna-1 in the collection of the Asociacion Etnografica Aztarna, located in Landako 8, Amurrio, Araba province, Basque Country, Spain. It was found some decades ago by Felix Murga (1929-2001; priest of Amurrio), in an excavation for a small reservoir in the Izoria locality, near Amurrio, but has never been studied or published. The specimen and its matrix were formerly covered with a thick glue coat. This coat, about 25 years old, was removed with ethanol and a thin brush, occasionally also with a thin surgical blade. After this process, it appeared that the matrix and, unfortunately, the specimen were treated with some heavily abrasive method prior to covering it with glue. This is one of the main reasons for its current poor preservation. In order to try to reveal as many anatomical details as possible, we took special care in photographing the specimen. However, only mechanic preparation, and especially acid treatment, may reveal additional, better preserved parts of the specimen; in particular, transfer preparation would be useful to show the right side, hidden in the matrix.
3. Stratigraphy and geological setting
3.1. Upper Cretaceous stratigraphy
The Upper Cretaceous carbonate succession cropping out near Amurrio (Araba province, Basque Country, Spain) is basically made up of sediments deposited in a large shallow marine carbonate ramp environment developing during a major transgressive episode in the Basque Cantabrian Basin (BCB) (e. g., Floquet, 2004). These large ramps were evolved at the southern margin of the BCB (i. e., the north Iberian passive margin) with marine facies reaching the Iberian basins in the Santonian peak transgression (e. g., Floquet, 2004). The onset of the Late Cretaceous transgression in the earliest Cenomanian occurred with the change of the subsidence style in the BCB from a phase of rifting subsidence (with important crustal thinning; Late Albian) to a phase of post-rift subsidence (less active fault-related subsidence and relative crustal cooling after a major phase of vulcanism during the Late Albian; e. g., Garcia-Mondejar et al., 2004). It finished with the onset of a major regressive episode in the Early to Middle Campanian (e. g., Floquet, 2004).
At the north Iberian margin, this Upper Cretaceous marine carbonate ramp is divided into three distinctive palaeogeographical areas from south to north (e. g., Feuillee, 1967; Lamolda, 1998; Floquet, 2004) (Fig. 1): 1. the Castilian Platform, with coastal to inner marine ramp environments; 2. the Navarre-Cantabrian Trough, with outer marine ramp environments mainly under the storm wave base; and 3. the Basque Trough, with talus to deep marine environments. Hemipelagic to pelagic facies are widespread in the latter two areas. The uppermost Albian to Cenomanian and Lower Turonian succession in the Navarre-Cantabrian Trough (600-800 m thick) is divided into six sedimentary cycles (Grafe, 1996; Grafe and Wendler, 2003), and is interpreted as deposited in a distally steepened ramp (Grafe and Wiedmann, 1993). During the Cenomanian, the Navarre-Cantabrian Trough is separated to the west from the North Cantabrian Basin (Santander Block) by the non-depositional structural high of the Ramales Fault (Lopez-Horgue et al., 2010) (Fig. 1). In the North Cantabrian Basin, Wilmsem (1997) divided the 150-250 m thick Cenomanian succession into six depositional sequences, mainly influenced by the pulsatory nature of the Cenomanian transgression but bounded by two tectoevents at around the Albian-Cenomanian boundary and at the middle Late Cenomanian (Wiese and Wilmsen, 1999).
Floquet (2004) divided the uppermost Albian to Maastrichtian sediments of the BCB into six Transgressive-Regressive (T-R) main sequences. These can be divided into several minor T-R cycles representing ramp progradation phases.
3.2. Biostratigraphy and regional correlation of the Cenomanian stage
Upper Cretaceous sediments of the Basque-Cantabrian Basin bear abundant faunas of planktic foraminifera that traditionally have been used as biostratigraphical indices especially in outer ramp to deep marine facies (e. g., Rodriguez-Lazaro et al., 1998). In shallow marine facies, benthic foraminifera have been also used (e. g., Cherchi and Schroeder, 1998). Regional unconformities are common towards shallower facies associated with important hiatuses and stratigraphic condensation, so that biostratigraphical successions are necessarily incomplete. Early and Middle Cenomanian ammonites are practically absent in more proximal ramp areas of the Navarre-Cantabrian Trough and in the North Castilian Platform due to the diachronous character of the transgression (e. g., section of Hortezuelos, east of Burgos; Wiedmann, 1975). However, these cephalopods do occur in the outer ramp, while becoming almost absent in many stratigraphic intervals of the talus-to-deep marine facies. Accordingly, ammonites of the outer ramp areas with expanded successions and short-gap unconformities (such as the Amurrio area) are highly suitable for biostratigraphical analysis (e. g., southeastern part of the Navarre-Cantabrian Trough; Santamaria and Lopez, 1996).
In this work we present a new proposal of regional correlation of the Cenomanian stage (Figs. 1-4) from inner ramp successions of the North Castilian Platform (Cidad-Puent edey, Burgos province: Wiedmann, 1979; Floquet, 1989; Barroso-Barcenilla et al., 2011b) via outer ramp successions of the Amurrio and Villasana areas in the Navarre-Cantabrian Trough (Feuille, 1967; Lamolda, 1979; Gorostidi and Lamolda, 1991; Rodriguez-Lazaro et al., 2003; Wiedmann, 1979; Grafe and Wiedmann, 1993; new data) to deep marine successions of the Basque Trough (Leioa, Biscay province: Rodriguez-Lazaro et al., 1998; new data). This correlation is based on:
1- biozonation with ammonites after reinterpretation of data of Wiedmann and Kauffman (1978) and Wiedmann (1979) for the coeval Villasana section, the new biostratigraphical proposal of Grafe (1996), the updated biostratigraphy for the Villasana section (Grafe and Wendler, 2003), the new biozonation for the Upper Cenomanian in the Puentedey area (Barroso-Barcenilla et al., 2009; Barroso-Barcenilla et al., 2011a, 2011b), a proposal of correlation to the European biozonation (Kennedy, 1984; Ogg et al., 2004), recent discoveries (Amurrio area, Balmaseda and Leioa, this paper), and comparison with biozones from southeastern areas of the Navarre-Cantabrian Trough (Estella-Lizarra area; Santamaria, 1992; Lopez-Horgue et al., 1999) (Appendix 1);
2-biozonation with planktic foraminifera for the Amurrio and Villasana areas (Wiedmann, 1979; Lamolda, 1979; Martinez et al., 1996; Grafe and Wendler, 2003), for the Leioa section (Rodriguez-Lazaro et al., 1998), and their correlation with ammonite zones after Robaszynski and Caron (1995);
3-recognition of the main stratigraphic divisions of the Cenomanian distinguished in the Villasana area (Lotze, 1960; Wiedmann, 1979; Grafe and Wendler, 2003) and their correlation in the field towards the Amurrio and Altube areas;
4-comparison with the eustatic sea level curve of Gale et al. (2002) and to the European S13C record of Jarvis et al. (2006).
This correlation allows to track the thickness variations of the Cenomanian carbonate ramp sediments of the middle part of the Basque-Cantabrian Basin across three different palaeogeographical areas with distinctive sedimentation and subsidence patterns.
4. Palaeoecology, bioevents and sedimentation
The Cenomanian represents a time of abrupt change in the palaeoceanographic conditions in the BCB, which determined turnovers in the marine faunal composition (e. g. , Lopez-Horgue et al., 1999). A period of progressive transgression that culminates during the Santonian and the change of subsidence led to the development of large shallow marine areas (Fig. 1). Under these new conditions, sea-level falls led to: decrease of the depth of the marine environment, change in the characteristics of the water masses, a likely incursion of shallow marine waters, and condensation/erosion/no deposition in shallow areas. Sea-level falls were not large enough to produce subaerial exposures in these huge ramps, except for coastal areas to the south (see Fig. 1). Accordingly, sealevel rises led to: increase the water depth (if subsidence is [greater than or equal to] 0), likely incursion of deeper oceanic waters and sediment starvation in the deepest areas. Figure 4 shows a 2-D corre lation of the carbonate ramp during the early Middle Cenomanian, highlighting the thickness variations of the Lower to Middle Cenomanian deposits from shallow inner areas to the WSW (Cidad-Puentedey) to outer ramp (around 200 m deep, Amurrio) and deep basinal areas (Leioa).
Deltaic siliciclastic deposits of the uppermost Albian were replaced by a carbonate ramp after the onset of the fast transgression that occurred in the study area during the earliest Cenomanian. In the Leioa area, the volcanism reduced drastically its influence during the Albian-Cenomanian transition, becoming absent during the rest of the Cenomanian and scarce during the Turonian-Santonian interval. Volcanic activity became really important to the southeast of the study area, in the Elgoibar area, for Turonian-Santonian times (e.g., Lamolda et al., 1983; Castanares et al., 1997). In this situation the Leioa area underwent a phase of relative cooling during the early Cenomanian wich, together with the generalized transgression, led to the subsidence and fast deepening of the area. According to Rodriguez-Lazaro et al. (1998), the Leioa area was,during the Cenomanian, dominated by intermediate waters indicative of more than 500 m in depth. Latest Albian submarine volcanic activity in the Leioa area occurred in depths around 100 m (Lopez-Horgue and Bodego, 2012). These bathymetry changes indicate an abrupt increase of the water depth and the drowning of the volcanic area in the basin at the end of the Albian (Leioa), and the progressive increase of the water depth with the shift of the coastal siliciclastic deposits to the south at the beginning of the Cenomanian.
The new ecological conditions mark the disappearance of the ammonite family Brancoceratidae (Mortoniceras and Cantabrigites spp.) in the study area (Leioa and Amurrio areas) during the latest Albian and the appearance and rapid radiation of the family Acanthoceratidae (Graysonites sp., derived from the last Lyelliceratidae) at the beginning of the Cenomanian (in Ordunte area; see fig. 2). These bioevents occurred almost at the same time in Tethyan, European and North-American basins (e. g., Wright et al., 1996; Gale et al., 2011).
Carbonate ramp sedimentation prevails during all of the Cenomanian, but with different stratigraphic records. The stratigraphic record of Early Cenomanian age (4 Ma) shows thickness changes from around 30 m in Puentedey to 160 m in Amurrio and 70 m in Leioa. Middle and Upper Cenomanian sediments in Puentedey (North Castilian Platform; Wiedmann, 1979; bed 1 of Barroso-Barcenilla et al., 2011b) are 50 and 12 m thick respectively. Their coeval sediments in the Amurrio area are 400 m and 200 m thick respectively, and only 45 m and 10 m thick respectively in the basinal area at Leioa. This striking thickness variations depict a condensed shallow marine area, a sediment-starved deep marine area and a highly subsiding Navarre-Cantabrian Trough that received most of the sediments (Figs. 2 and 3). Continuous and increasing subsidence in the Navarre-Cantabrian Trough leading to accommodation creation can explain the progressive preservation of sediments after increasing sedimentation rate from Middle to Late Cenomanian (600 m thick succession in 2.5 Ma) and the maintenance of the overall depth conditions (around 200 m; Grafe and Wendler, 2003).
Sediments of late Middle Cenomanian age from the Leioa area (Fig. 2) contain a low diversity fauna of benthic foraminifera and ostracods, together wih intervals that are free of these faunas (ostracod-free, OF, or benthic-free, BF, interval), indicative of hypoxic to anoxic conditions at the sea bottom that led to faunal turnovers in the ostracod assemblages (Rodriguez-Lazaro et al., 1998). Two important positive excursions in the S13C curve are detected in the same interval in Leioa, indicating the burial of organic matter in that hypoxic bottom (MCE 1a and 1b of Mitchell et al., 1996; RodriguezLazaro et al., 1998).
The fish and ammonite from Aiara occur in the marly limestones of the lower Middle Cenomanian. The incursion of shallow waters into the Leioa area during this time and the related enrichment in nutrients (Rodriguez-Lazaro et al., 1998) suggest the renewal of the oceanic waters.
After this Middle Cenomanian transgression, the long-term increasing trend of the S13C initiated earlier is consistent with a reduced nutrient availability to benthic microorganisms in the Leioa basin area (Rodriguez-Lazaro et al., 1998). This trend is also consistent with the long-term increasing sea level during the Cenomanian that led to the onset of the OAE2 in the latest Cenomanian (Gale et al., 2002; time-scale of Ogg and Hinnov, 2012). The Late Cenomanian transgression may have led to the expansion of the oxygen minimum zone from the basin area (Leioa) to the outer ramp (Amurrio-Aiara), therefore explaining the hypoxic conditions of the shelf bottom indicated by the ostracod assemblages (Rodriguez-Lazaro et al., 2003). Rotalipora spp. show an abrupt decline and extinction prior to the Cenomanian-Turonian boundary (circa 25 m before the C-T boundary in the Menoyo section, near Amurrio, Gorostidi and Lamolda, 1991; circa 8 m after the onset of the Rotalipora decline event in Leioa, RodriguezLazaro et al., 1998; in the M. geslinianum Zone, 2.6 m before the C-T boundary in Puentedey, Barroso-Barcenilla et al., 2011b). The first occurrence of the calcareous nannofossil Quadrum gartneri PRINS and PERCH-NIELSEN is the selected bioevent for the C-T boundary in the Menoyo section (Gorostidi and Lamolda, 1991; Lamolda and Peryt, 1998). The last occurrence of Rotalipora spp., and the occurrence of Mammites nodosoides (SCHLUTER) 80 m above the C-T boundary (Menoyo section; Wiedmann, 1979; Lamolda, 1979) are in agreement with the secondary biostratigraphic markers in the GSSP for the base of the Turonian of Pueblo (Kennedy et al., 2000).
According to a proxy for sea-level change based on planktic-benthic microfossil ratios converted by palaeoslope model, Grafe and Wendler (2003) recognize three major periods of sea-level rise during the Cenomanian of the BCB at 97.5 (Early), 95.2 (latest Middle) and 93.8 ma (latest). Despite the fact that their proxy does not predict major sea-level falls in the Cenomanian, this general transgressive tendency is punc tuated by relative sea-level falls and the record of lowstand deposits. These deposits form the base of Arceo beds above UC3 unconformity and the base of Hijuela beds above UC4 unconformity, in the upper middle to upper Cenomanian, and the base of Cabezas beds above UC5 unconformiy in the topmost Cenomanian (Grafe, 1994; Grafe and Wiedmann, 1993; Grafe and Wendler, 2003; see figure 3). Distributions of benthic foraminifera (typical of outer shelf) and the planktic/benthic ratios (around 50 %) in the Cenomanian of the Villasana area support the above comented relative sea-level changes but no substantial depth-variations (Grafe and Wendler, 2003).
5. Systematic palaeontology
This section presents new invertebrate and vertebrate record of biostratigraphic and palaeoecological significance. These new records, together with the new model presented above, provide a new insight on the faunal replacements associated with this marine transgression.
5.1. Ammonite new record
Suborder Ammonitina Hyatt, 1889 Superfamily Acanthoceratoidea Grossouvre, 1894 Family Acanthoceratidae Grossouvre, 1894 Subfamily Acanthoceratinae Grossouvre, 1894 Genus Calycoceras Hyatt, 1900 Subgenus Newboldiceras Thomel, 1972
Calycoceras (Newboldiceras) asiaticum spinosum (Kossmat, 1897)
1897Acanthoceras newboldi var. spinosa Kossmat, p. 7(114); pl. 2(13), figs. 2, 3; pl. 3(14), fig. 1.
1990 Calycoceras (Newboldiceras) asiaticum spinosum (Kossmat, 1897), Wright and Kennedy, p. 249, pl. 64, fig. 3; pl. 65, fig. 4, and others (with synonymy).
2004 Calycoceras (Newboldiceras) asiaticum spinosum (Kossmat, 1897), Kennedy and Jolkicev, p. 376, pl. 3, figs. 7, 10, 11; pl. 4, figs. 1-5; pl. 5, figs. 6-11 (with additional synonymy).
Referredmaterial. Specimen MCNA 14392: part and counterpart of a crushed fragmentary internal mould corresponding to the end of the phragmocone and most of the body chamber.
Description. Narrow and high ribs cross the venter and are separated by slightly wider interspaces. The best preserved one third of a whorl, corresponding to the body chamber, bears 17 ribs. Primary ribs bear strong spiny umbilical tubercles, less marked inner ventrolateral tubercles and well marked clavate outer ventrolateral and siphonal tubercles. Inner ventrolateral and siphonal tubercles tend to decrease in strength adorally. Secondary ribs with both ventrolateral and siphonal tubercles are intercalated between primaries and do not reach the umbilical shoulder. The reconstructed whorl section is depressed.
Measurements (mm; reconstructed): diameter, 65.0, whorl height, 17.0, whorl width, 21.0.
Discussion. The dense ribbing, style and persistence of the tuberculation together with the polygonal whorl section are features that characterise the C. (Newboldiceras) asiaticum species. The strength of the ribs and that of the umbilical tubercle are typical features of the spinosum subspecies. Despite the preservation of the specimen, the suggested diameter and whorl section together with the ontogenetic changes in the ornament indicate the onset of the adult stage of the specimen in the outermost part, in which inner ventrolateral and siphonal tubercles tend to disappear. The specimen described here differs clearly from the less depressed and less sculptured C. (N.) asiaticum asiaticum subspecies. C. (N.) hippocastanum is a strongly sculptured species but with wider ribs and very depressed whorl section. The specimen is distinctive from other species of C. (N.) which are less sculptured, less depressed and with wider ribbing at a similar growth stage. Among other Acanthoceratinae, a similar shell sculpture is observed only in Eucalycoceras, but the latter differs in its denser ribbing with more separated umbilical and inner ventrolateral tubercles and commonly bullate tubercles, and in its compressed whorl section (e. g., Wright and Kennedy, 1990).
Occurrence. This new specimen occurs in the uppermost part of the "Lower Campillo beds" of the Amurrio-Aiara area The occurrence of this subspecies in the study area indicates a non-basal Middle Cenomanian age: T. acutus Subzone of the A. rhotomagense Zone, and A. jukesbrownei Zone. In equivalent sediments to the west (Valle de Mena area), the "Campillo beds" yield Calycoceras gr. C. newboldi (Wiedmann, 1979). In the same area, C. newboldi spinosum (Kossmat) and C. newboldi madagascariense Collignon are recorded from the overlying "Hijuela beds", dated as early Late Cenomanian (Wiedmann, 1979). This subspecies also occurs in Middle Cenomanian sediments from the Santander area of the Basque-Cantabrian Basin (Wilmsen et al., 1996; Wilmsen, 1997). This species is a component of the great diversification of Acanthoceratidae during the Middle Cenomanian (Wright et al., 1996).
Distribution of the species. This is one of the most widely spread species of Acanthoceratidae occurring in Europe, Asia, North America and Africa characterising the non-basal Middle Cenomanian; in England it also occurs in the lower Upper Cenomanian Calycoceras (Proeucalycoceras) guerangeri Subzone (Wright and Kennedy, 1990).
5.2. New teleostean fish record
Superclass Osteichthyes Huxley, 1880
Class Actinopterygii Klein, 1885
Infraclass Neopterygii Regan, 1923
Division Teleostei Muller, 1844
Order Crossognathiformes Taverne, 1989
Suborder Pachyrhizodontoidei Forey, 1977
Family Pachyrhizodontidae Cope, 1872
Description and comparison
General morphology. The fish specimen (Fig. 6) is in anatomic connection and nearly complete, showing its left side in lateral view. The head is exhibited in its entirety (Fig. 7), the anteriormost part only as an impression; the rest of the skull is complete but poorly preserved, showing very few anatomic details. The abdomen and most of the caudal region are nearly complete (Fig. 6), with the scales shown in lateral view and a good number of vertebral centra protruding through the squamation. The caudal fin is entirely missing.
The anterior contour of the specimen is recognizable; the dorsal and ventral contours posterior to the maximum height are worn out, but they still provide significant information about the overall shape of the fish. The body is markedly fusiform, nearly ovoid (Fig. 6). The head is triangular, very pointed (Fig. 7). Both features correspond to the general morphology typical of most Crossognathiformes, most notably of the Pachyrizodontoidei, among other teleosts.
The preserved portion of the specimen measures about 350 mm from the tip of the snout to the posterior side of the last visible vertebral centrum. The general shape of the body suggests that this vertebral centrum is part of the caudal pedicle, indicating that the preserved length is only slightly shorter than the actual standard length. However, this is the only indication, since the caudal fin, including the ural endoskeleton, are entirely missing. Even so, a conservative estimation suggests that the individual in life probably measured well above 400 mm of total length, with the standard length probably somewhere between 350 and 400. For the rough estimation of the morphometric measures provided below, we use this range of 350-400 mm to provide a minimum estimation of each percentage ratio to the standard length.
The maximum body height is about 104 mm, which results in, at most, 26-30% of the standard length. The head length is 107 mm, resulting on a very similar percentage. The head height, measured from the ventralmost preserved border to the supraoccipital, is about 53 mm. Therefore, the head is about half as high as it is long.
Skull. The skull (Figs. 7, 8) is preserved in dorsolateral view making observable the skull roof but not the ventral region of the head. The imperfect preservation and artificial abrasion of the specimen (Fig. 7A) have resulted on presenting a number of recognizable skull bones, but very few clearly recognizable borders, canals, pores, or other anatomical features. For this reason, the general arrangement of some dermal skull bones can only be estimated (Fig. 7B), but the precise shape, extent, and other features of most of these bones cannot be described in detail.
The anterior (ethmoid) region is preserved as a rough impression only, with no details. The mouth is tightly closed, and this, together with the partially dorsal view in which it is shown, prevents from observing the lower jaw. The infraorbitals cover most of the upper jaw, but we can note that the maxilla is very long, as in all crossognathiforms, and that there is at least one supramaxilla starting about midlength of the maxilla.
The better preserved region is the skull roof, notably the frontals (Figs. 7, 8). They are very long and large, apparently wider anterior to the orbit than posterior to it. The outline of the frontals seems more similar to that of Pachyrhizodus than to any other crossognathiform. As in this genus (Forey 1977, fig. 25), they are long and very broad, with the maximum width just before the orbit, being comparatively narrower in their postorbital region. However, in the Amurrio specimen they do not have the median depression on the epiphyseal region present in Pachyrhizodus, Apsopelix (Teller-Marshall and Bardack, 1978, p.7. fig.1), Goulmimichthys (Cavin, 2001, p.513, fig.2B) and Nardopiscis (Taverne, 2008, p.21, fig.5). The frontals are not depressed but raised along their midline instead, so that the ensemble of both frontals forms an elevated median ridge along most of their length (Figs. 7, 8), as in Rhacolepis (Forey 1977, p.146). The lateral margin of the frontals is excavated at the posterodorsal border of the orbit above the autosphenotic (Fig. 8); this is a diagnostic character of the suborder Pachyrhizodontoidei (Cavin, 2001, p.533). The shape of lateral border of the frontal at the posterodorsal corner of the orbit seems to be part of the lateral expansion of the autosphenotic, although the latter is only very partially visible. Such participation is absent in Rhacolepis (Forey 1977, fig. 10; Maisey 1991, fig. on p.249) and most other crossognathiforms, but is present in Goulmimichthys (Cavin, 2001, p.513, fig.2) and, apparently, Bavarichthys (Arratia and Tischlinger, 2010, fig.5). In addition to the median ridge formed by the elevation of both frontals, each frontal has another conspicuous longitudinal ridge (Fig. 7), probably lodging the supraorbital sensory canal, as in Nardopiscis (Taverne, 2008, p.21, fig.3) and Rhacolepis (Forey 1977, fig.12). Each paired ridge and the median ridge limit a relatively deep, wide depression along most of the length of each frontal. This complex type of relief and the convex but smooth postorbital expansion suggest that there are no radiating ridges on the surface of the frontals.
The parietals are not so well preserved (Fig. 8); they are small bony plates separated from each other by the supraoccipital, whose serrated and curved posterior border suggests the presence of a supraoccipital crest (Fig. 8), apparently quite shorter than in Rhacolepis (Forey 1977, fig.12). The skull is, therefore, lateroparietal. A bony plate postero-lateral to each parietal, and quite larger, must correspond to the extrascapular bones. Some sensory pores indicate the presence of the extrascapular commissure; a single pair of large and wide extrascapulars is apparently present.
The infraorbital region is also quite peculiar (Fig. 7). The first infraorbital seems autogenous, and it largely covers the supramaxilla (e) plus a good extent of the maxilla. More notably, a single bony plate seems to cover the area usually occupied by the second, third, and fourth infraorbitals in Aquilopiscis, Chongichthys, Goulmimichthys, Nardopiscis, Pachyrhizodus, Rhacolepis, and Varasichthys. In the Amurrio fish, there is a clear suture separating this plate from the fifth infraorbital, but there is no other suture within this single bony plate. If so, it would represent a fusion of the second, third, and fourth infraorbitals. This plate is consequently very long, but also very large ventrally and, especially, posteriorly. Fusion of infraorbitals is not unheard of among crossognathiforms. Five autogenous infraorbitals are present in Aquilopiscis (Cumbaa and Murray, 2008, fig.6), Goulmimichthys (Cavin, 2001, fig.5), Varasichthys (Arratia, 2008 fig.3a), and most likely Chongichthys (Arratia, 2008, fig.6a) and Nardopiscis (four infraorbitals plus a dermosphenotic in the position of the fifth infraorbital: Taverne, 2008, fig.3). In turn, infraorbitals two and three are fused in Pachyrhizodus (Forey 1977, fig.30) and Rhacolepis (Forey 1977, fig.20; Arratia, 2008, fig.6b); infraorbitals 4 and 5 are fused in Bavarichthys (Arratia and Tischlinger, 2010, fig.5); and infraorbitals 2 and 3, and, separately, infraorbitals 4 and 5, are fused in Michin (Alvarado-Ortega et al., 2008, fig.2). The only crossognathiform with apparently a similar pattern, fusion of infraorbitals two, three, and four into a single bony plate, is Apsopelix anglicus (Teller-Marshall and Bardack, 1978). The pattern of the latter species, however, should be regarded with caution because of the fragmentation of the infraorbital series in the available specimens.
The posterior infraorbitals are very large. Their posterior border, although not entirely preserved, seems to cover a good part of the dorsal limb of the preopercular bone, more as in Pachyrizodus than as in Bavarichthys or Rhacolepis; however, it does not seem to reach the opercular bone, as in Goulmimichthys (Cavin, 2001).
The opercular bone (Fig. 7) is very large, occupying nearly one third of the head length, more than in most crossognathiforms; for instance, it occupies only about one fifth in Rhacolepis (Forey 1977, fig.20). It is roughly quadrangluar in contour, very much as in Nardopiscis (Taverne, 2008, fig.3). The morphology of the dorsal region of the preopercular bone is unveiled by its slightly uplifted borders. This bone is very narrow, and its limbs form a straight angle with a very small expansion at it. Although it is not well exposed, the anteroventral limb of the preopercular bone seems rather short, as in most crossognathiforms.
Fins, vertebrae, and squamation. Fins are mostly missing, although the pectoral girdle is preserved, and there is also some indication of the position of the dorsal fin. The pectoral girdle is almost entirely, but badly, preserved. The cleithrum is broad, with a broad but short anteroventral expansion. A long, broad plate between the cleithrum and the extrascapular is probably the posttemporal; remains of a smaller supracleithrum seem to be present as well. In articulation with the posterior border of the cleithrum, a narrow scapula and a broad coracoid are visible; the presence of a postcleithrum cannot be confirmed. No remains of the pectoral fin rays are preserved.
Very scarce, tiny basal fragments of the anteriormost fin rays indicate that the dorsal fin is inserted at about 225 mm from the tip of the snout, at about 57-64% of the estimated standard length; that is, behind the mid-length of the body. The ventral border of the body in the posterior part of the caudal region is not preserved, so no traces of the pelvic and anal fins are observed. The caudal pedicle and fin are entirely missing.
Many vertebrae are partially visible protruding through the scales (Fig. 6). There are at least 33 vertebrae; 3-5 more vertebrae must have occupied the spaces before and among the exposed vertebrae. An undeterminable number of caudal vertebrae were present posterior to the last one preserved. It is not possible to estimate how many of the preserved vertebrae are abdominal. Each vertebra appears to be very constricted in the middle. Because matrix covers the lateral sides, a possible relief at the surface of centra cannot be observed. Some neural spines are visible in the posterior part of the specimen, but it is not possible to discern whether the corresponding arcocentra are fused or autogenous.
The scales are generally well preserved (Fig. 6). They are leptoid, apparently cycloid, small and very tightly arranged. Some 23-25 longitudinal scale rows can be estimated in the highest point of the body. About 40 complete transversal rows can be estimated between the posterior border of the pectoral girdle and the point of insertion of the dorsal fin; some 12 incomplete transversal scale rows can be counted between the posterior border of the skull and the first complete transversal row.
Taxonomic assessment. The poor preservation of the specimen, notably the dermal skull, and the lack of most fins, including the caudal endoskeleton, renders comparisons very difficult and strongly advises against a generic assessment of the specimen.
The specimen lacks the caudal endoskeleton, with its essential characters; however, the supraoccipital forming part of the skull roof and the presence of leptoid (not ganoid) scales clearly shows that it is a teleostean fish. Beside the general, typical shape of the body and head, the Amurrio fish seems to present the only unique character of the Crossognathiformes according to Arratia (2008): a single pair of large and well-developed extrascapular bones. However, none of the homoplastic characters that combine to define the order can be checked in the specimen. As pointed above, the frontal margin excavated above the autosphenotic indicates that it is a Pachyrizodontoidei (Cavin, 2001).
Within the Pachyrhizodontoidei, we cannot check any character of the family Pachyrhizodontidae in the Amurrio fish, because all diagnostic characters (Cavin, 2001, p.533) are provided by the caudal fin and endoskeleton, and these are entirely missing in the specimen. However, it does not present the cranial diagnostic characters of the other family, the Notelopidae, that can be checked: fusion of infraorbitals 4+5 and skull roof medioparietal (reversal; Cavin, 2001, p.533). The fish can, therefore, be referred to the Pachyrhizodontidae with great caution, because it does not belong to the other family of the suborder. In any case, this is the first report of a Pachyrhizodontoidei from the Iberian Peninsula.
Within the Pachyrhizodontidae, it resembles Pachyrhizodus and Rhacolepis rather than Goulmimichthys in the fusion of some infraorbitals, although they are not exactly the same (see above). As a matter of fact, fusion of infraorbitals (1 and 2 or 2 and 3) is considered a character typical of the suborder Pachyrhizodontoidei (Forey 1977, pp.128-129; Cavin, 2001, p.533). Fusion of infraorbital bones also occurs in crossognathids, a feature regarded as an evidence of close relationships with pachyrhizodontoids by Taverne (1989), but as a trend present in parallel in both lineages by Cavin (2001). The crossognathids Apsopelix possibly shares with the Amurrio fish a similar infraorbital bones pattern, but Apsopelix differs by several other characters, such as a medial depression at the posterior level of the frontals, a medioparietal skull roof, and the frontals tapering anteriorly (Teller-Marshall and Bardack, 1978).
Among the Pachyrhizodontidae, the new fish is notably similar to Pachyrhizodus megalops, from the Cenomanian of England, and to Rhacolepis, from the Aptian of Brazil, in some particular features of the frontal bones, as presented above. However, the combination of the characters of the frontals of the Amurrio fish seems to be unique; the fusion of infraorbitals 2+3+4 is also unique among all crossognathiform genera.
5.3. Phylogenetic andpalaeobiogeographic comments on Pachyrhizodontoidei
Pachyrhizodontoidei are generally grouped with the Crossognathidae within the Crossognathiformes (Taverne, 1989; Arratia, 2008), although an alternative view considering the crossognathids as basal teleosts and the pachyrhizodontoids as basal euteleosts has also been proposed (Cavin, 2001; Cumbaa and Murray, 2008).
The discrepancy between both phylogenetic patterns makes the recognition of a clear palaeobiogeographical signal difficult . In both alternative phylogenetic hypotheses, however, Rhacolepis, Goulmimichthys, Pachyrhizodus and Aquilopiscis (the latter two genera are not included in Arratia, 2008) form the clade Pachyrhizodontidae, to which the Amurrio fish likely belongs (see above). Although not included in any phylogenetic analysis, Michin csernai is regarded as the basal member of the family Pachyrhizodontidae (Alvarado-Ortega et al., 2008). Kansanus martini, from the Late Cretaceous Niobrara Formation in Kansas, USA, is now referred to Pachyrhizodus sp. (Shimada and Fielitz, 2006). The geographic distribution of pachyrhizodontids is mapped for three time intervals: the Albian, Cenomanian-Turonian, and Coniacian-Maastrichtian (Fig. 9). In the Albian, the genus Pachyrhizodus is present in Europe (P salmonensis) and Australia, (P. marathonensis), and Rhacolepis is present, possibly with two species, in several localities from Brazil. In the Cenomanian, the genus Pachyrhizodus diversified, with five recognized species in the British Lower Chalk; the occurrence of the Amurrio specimen is isochronous with this radiation. Three species of Pachyrhizodus are known in the Cinto Euganeo locality, Italy, which is dated as CenomanianTuronian boundary. In the Turonian, one species of Pachyrhizodus is recorded in the British Middle Chalk, one in the Greenhorn Formation in Nebraska, USA, and another one in the locality of Vallecillo in Mexico. In this stage, the genus Goulmimichtys also occurs, with one species from Goulmima, Morocco, one from Vallecillo, Mexico, and possibly one from the Formation Villeta in Columbia (Paramo-Fonseca, pers. com.). The genus Aquilopiscis is known from the Turonian of Canada. After the Turonian, several occurrences of Pachyrhizodus are recorded in the Late Cretaceous of North America, as well in the Maastrichtian of Europe and New Zealand. Nardopiscis, from the Campanian-Maastrichtian of Nardo, Italy, may represent another occurrence (Taverne, 2008), but its phylogenetic position among the Pachyrhizodontoidei remains unclear.
The interpretation of the distribution of the pachyrizodontids in time and space is difficult because the phylogenetic relationships between the Pachyrhizodus species, as well as the monophyly of the genus, are unclear, and because the quality of the fossil record is very variable in time and space. For instance, the richness of the fish record from the British Chalk may be responsible for the diversification of the genus Pachyrhizodus observed in these deposits, and a similar situation occurs for the observed diversification of the genus in the Coniacian-Campanian of North America. However, some general trends can be detected, supplementing the preliminary pattern proposed by Cavin (2008). The genus Pachyrhizodus, if monophyletic, is the most specious genus of the family. All species occurred on northern landmasses, except one in the Albian of Australia and one in the Maastrichtian of New Zealand. These southern occurrences are not surprising if we consider this region, the easternmost extremity of Gondwana, as largely opens towards the Tethys. However, the absence of this genus in the very rich fish assemblages from the Cenomanian of the Lebanon results on a discontinuous distribution of the genus throughout the Tethys. The pachyrhizodontid representatives in Western Gondwana appear to differ from the taxa in Laurasia, with Rhacolepis in the Early Cretaceous and Goulmimichthys in the Turonian. The latter is known from a species in Mexico, which belongs to Laurasia, but in a locality showing affinities with the Gondwanian realm. Rather than focusing on the palaeobiogeographical affinities alone, it looks as if Pachyrhizodus was a taxon from temperate environments, whereas Michin, Rhacolepis, and Goulmimichthys were genera from more tropical environments. Interestingly, the Amurrio fish shows characters of both Rhacolepis and Pachyrhizodus, and was found in a locality situated in a rather low palaeolatitude compared to that of most Pachyrhizodus species.
The palaeobiogeographical observations mentioned here do not constitute a tested evolutionary scenario, but are rather hypotheses to be tested in further studies.
6. Conclusions: integration of the new data
The multidisciplinary approach to the Late Cretaceous marine transgression in Iberia presented in this paper integrates known and new stratigraphical and fossil record (ammonite and fish) data from the Cenomanian carbonate ramp succession deposited in the northern Iberian margin of the BasqueCantabrian Basin. The Albian-Cenomanian transition marks the onset of a progressive transgression and the diminishing of a striking differential subsidence, leading to larger areas of similar subsidence and sedimentary rate. The progressive flooding of the Iberian margin until the Santonian is at the origin of large shallow marine areas. A proposal of correlation of the Cenomanian ramp successions from shallowest areas in the south to a deep marine basin in the north has been supported by the revision of the known and new biostratigraphical data. This correlation has permitted to depict the striking differences in thickness. Very thin deposits (around 80 m) originated in shallower areas that underwent episodic erosion/no deposition/condensation, especially during lower sea-levels. The thickest succession (almost 800 m) was recorded in the subsiding Navarre-Cantabrian Trough. Thin condensed deposits (less than 140 m) formed in a sedimentstarved deeper basin. Oceanographic changes described in the deep marine area by Rodriguez-Lazaro et al. (1998) and those described by Grafe and Wendler (2003) have been used in connection to stratigraphy in order to understand the environmental changes.
Ammonites underwent a striking turnover within Acanthoceratoidea at the Albian-Cenomanian transition, with the extinction of Brancoceratidae before the Cenomanian and the appearance and rapid radiation of Acanthoceratidae at the beginning of the Cenomanian from a limited stock of Lyelliceratidae. In the studied area, more work is needed to accurately draw these changes; however, evidences support that this ammonite turnover occurred during the onset of the Late Cretaceous transgression, the deepening of the basin and the change from deltaic and deeper marine volcanic environments to marine carbonate ramps. The new specimen of Calycoceras (Newboldiceras) asiaticum spinosum described here is a component of an important diversification in Acanthoceratidae that took place at the Early-Middle Cenomanian transition. The association to the new fish in the same bed is of high biostratigraphic importance.
The new teleostean fish from the Middle Cenomanian is the first reported record of the order Crossognathiformes from the Cretaceous of the Iberian Peninsula. It lived in a distal shallow marine area, being the oldest evidence of another relevant faunal replacement in this part of Europe. During most of the Mesozoic, the fish faunas from the Tethys Sea (Western Tethys Ocean) and its continental domains were essentially formed by basal neopterygians. Such relatively primitive, non-teleostean forms constitute the basis of the typical marine Jurassic faunas from classic sites like Cerin (France; e.g., Saint-Seine, 1949) and Solnhofen (Germany, e.g., Frickhinger, 1994). These Jurassic faunas include taxa such as Amiiformes, Pycnodontiformes, and Ginglymodi. Ecologically, these fishes were the specialized ones: ichthyofagous, durophagous, insectivorous, and so on. Undisputed teleosteans did appear early in the Jurassic (Arratia, 2000, 2004); during that period and the Early Cretaceous, their diversity increased and their main basal evolutionary lineages appeared. However, they were mostly, if not exclusively, very generalized forms, small to middle-sized, fusiform bodied, with small or no teeth, and with a buccal apparatus typical of a suction mode of feeding. In the westernmost part of the Western Tethys Ocean and its continental domains, teleosteans occupied, for a very long time, the lowest levels of the fish trophic pyramid, with no recognizable specialized forms. Specialized groups such as pycnodonts and amiiforms managed to keep teleosteans out of their niches for a remarkably long time, an indication that the evolutionary novelties of the Teleostei per se were not enough to grant them immediate dominion in specialized niches until drastic changes in the environment did occur (Poyato-Ariza, 2005). In this sense, the fish faunas turnover in Western Europe during the EarlyLate Cretaceous would be linked to major transgression episodes, when specialized forms of basal neopterygians were replaced by teleosteans. The latter would be, from then on, the essential component of all bony fish faunas until today. The new Pachyrhizodontidae from Spain is, therefore, the oldest evidence of modern actinopterygian ichthyofaunas in Iberia. In this context, this finding is remarkable because it corroborates that the phenomenon of the faunal replacement taking place during the Late Cretaceous in this part of Europe is linked to a major marine transgression, a specific evidence that confirms general predictions based on previous ecomorphological studies (Poyato-Ariza, 2005; Poyato-Ariza and Martin-Abad, 2013). As a consequence, it confirms that, during the Mesozoic, teleosteans required major environmental changes for displacing more basal neopterygians from the most specialized niches of the trophic pyramid.
This work is a contribution to the University of the Basque Country (UPV/EHU) research project EHU09/11, and to the project CGL2013-42643-P of the Ministerio de Ciencia e Innovacion de Espana. Financial support has been also provided by the University of the Basque Country (UPV/EHU) Research Group IT834-13. The photographs of this difficult fish specimen were painstakingly prepared and taken by Zarela Herrera at the Servicio de Fotografia Paleontologica of the Universidad de Zaragoza (Spain). Inaki Rojo Legarra assisted during the field work. Goreti and Ramon from the Asociacion Etnografica Aztarna are acknowledged for the kind loan of the fish specimen. The revisions of Kai-Uwe Grafe and an anonymous reviewer substantially improved the final version of the paper.
Appendix 1.- Ammonite and foraminifera species of biostratigraphic value in the study zone. Astobiza from Rat (1959). W-a to h from Wiedmann (1979), given with their original designation of this author. B from Barroso-Barcenilla et al. (2011). Ziorraga, Balmaseda and Ondiz sites are new localities with Late Albian ammonites under current study. Ammonite associations (see figs. 2 and 3 for stratigraphical occurrences) Astobiza (Altube area; Rat, 1959) (1 in fig. 2) Stoliczkaia aff. dispar S. aff. rhamnonota S. gardonica Ziorraga (Zi; Altube area) (2 in fig. 2; see also fig. 3) Stoliczkaia sp. Mariella sp. Mortoniceras (Durnovarites) sp. Balmaseda (near Ordunte) (3 in figure 2) Stoliczkaia sp. Ondiz (On; Leioa area) (see fig. 3) Mortoniceras (Durnovarites) sp. Cantabrigites sp. Anisoceras sp. Stoliczkaia sp. Izoria (Amurrio area) (see figs. 2 and 3) Calycoceras (Newboldiceras) asiaticum spinosum (KOSSMAT) Villasana area (W-a to f; corresponding 10a to 10f of Wiedmann, 1979) (see figs. 2 and 3) W-a (4 in fig. 2) Graysonites sp. Hypoturrilites mantelli (SHARPE) Orbitolina (Mesorbitolina) aperta (ERMAN) Orbitolina (Orbitolina) concava quatarica HENSON W-b Mantelliceras mantelli (J. SOW.) M. menabense COLLIGNON M. tuberculatum (MANTELL) Tunesites cf. latelobatum (COLLIGNON) Forbesiceras largilliertianum (d'ORBIGNY) Praeglobotruncana stephani (GANDOLFI) Rotalipora appenninica (RENZ) R. reicheli mOrNOD R. brotzeni (SIGAL) R. greenhornensis (MORROW) W-c Mantelliceras hyatti SPATH M. costatum (MANTELL) Calycoceras gr. newboldi (KOSSMAT) R. reicheli MORNOD R. greenhornensis (MORROW) Praeglobotruncana stephani (GANDOLFI) W-d Calycoceras newboldi (KOSSMAT) C. subgentoni (SPATH) Rotalipora cushmani (MORROW) Hedbergella paradubia (SIGAL) R. reicheli MORNOD R. greenhornensis (MORROW) Praeglobotruncana stephani (GANDOLFI) W-e Calycoceras gr. newboldi (KOSSMAT) Calycoceras cf. choffati (KOSSMAT) Eucalycoceras spathi COLLIGNON R. E. pentagonum (JUKES-BROWNE) E. rowei (SPATH) Rotalipora cushmani (MORROW) Praeglobotruncana turbinata (MORNOD) globotruncanoides SIGAL W-f Lotzeites lotzei WIEDMANN Calycoceras newboldi spinosum (KOSSMAT) C. newboldi madagascariense COLLIGNON C. paucinodatum (CRICK) Eucalycoceras gothicum (KOSSMAT) Rotalipora cushmani (MORROW) Praeglobotruncana turbinata (MORNOD) Cidad (W-g and h; both in locality 12 of Wiedmann, 1979) (see fig. 3) W-g Orbitolina (Conicorbitolina) conica (d'ARCHIAC) Orbitolina (Orbitolina) concava quatarica HENSON (Orbitolina (O.) sefini HENSON sensu Grafe, 1994) W-h Orbitolina (Conicorbitolina) conica (d'ARCHIAC) Puentedey (B-a to d; corresponding beds of Barroso-Barcenilla et al., 2011) (see fig. 3) B-a (bed 1 and lower part of bed 2) Acanthoceras rhotomagense (BRONGNIART) Calycoceras (C.) sp. B-b (upper part of bed 2, bed 3 and bed 4) Neolobites vibrayeanus (d'ORBIGNY) Euomphaloceras euomphalum (SHARPE) Calycoceras (C.) naviculare (MANTELL) Metoicoceras mosbyense COBBAN B-c (beds 5, 6 and 7) M. geslinianum (d'ORBIGNY) B-d (bed 8 and part of 9) Spathites (Jeanrogericeras) subconciliatum (CHOFFAT) Fagesia catinus (MANTELL) Spathites (Jeanrogericeras) robustus (WIEDMANN) Parapuzosia (Austiniceras) sp. Vascoceras cauvini CHUDEAU
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M.A. Lopez-Horgue (1), FJ. Poyato-Ariza (2), L. Cavin (3), D.D. Bermudez-Rochas (4)
(1) Estratigrafia eta Paleontologia, Zientzia eta Teknologia Fakultatea, University of the Basque Country UPV/EHU, Sarriena z/g, 48940 Leioa, Basque Country, Spain (2) Unidad de Paleontologia, Departamento de Biologia, Universidad Autonoma de Madrid, Cantoblanco, 28049-Madrid, Spain (3) Department of Geology and Palaeontology, Museum d'Histoire Naturelle, CP6434, 1211 Geneve 6, Switzerland (4) Area de Didactica de las CC. Experimentales, Facultad de Educacion, Universidad de Cantabria, Avda. de los Castros s/n, 39005-Santander, Spain
e-mail addresses: firstname.lastname@example.org (M.A.L.-H.., corresponding author); email@example.com (FJ.P.-A.); Lionel.Cavin@ville-ge.ch (L.C.); david. firstname.lastname@example.org (D.D.B.-R.)
Received: 18 October 2013 / Accepted: 3 September 2014 / Available online: 30 October 2014
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|Title Annotation:||texto en ingles|
|Author:||Lopez-Horgue, M.A.; Poyato-Ariza, F.J.; Cavin, L.; Bermudez-Rochas, D.D.|
|Publication:||Journal of Iberian Geology|
|Date:||Dec 1, 2014|
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