A new genus of coccolepidid fishes (Actinopterygii, Chondrostei) from the continental Jurassic of Patagonia
Article number: 16.1.7A
Copyright Palaeontological Association, February 2013
Submission: 3 September 2012. Acceptance: 30 January 2013
Jurassic freshwater fish faunas are still poorly known, with the only assemblage of that age known from southern South America being the "Almada fauna" of the Cañadón Calcáreo Formation (Oxfordian-Tithonian) of Chubut, Argentina. This fauna is composed mainly by abundant teleosts and a much rarer basal actinopterygian, originally described as †Oligopleurus groeberi and currently usually placed in the genus †Coccolepis. This taxon is here redescribed on the basis of the original specimens and more numerous and better preserved new material from several localities within the Cañadón Calcáreo Formation. The species shows several differences to other coccolepidid taxa, including the apomorphic presence of a sensory canal in the gular plate, and cannot be referred to a known genus. Thus, a new genus name, †Condorlepis gen. nov., is proposed. The detailed anatomical description of †Condorlepis gen. nov. groeberi provides further evidence for the chondrostean affinities of the Coccolepididae and their close relationships with the Acipenseriformes, since this species shows six characters that were hitherto considered to be autapomorphies of the latter clade. A comparison of the Almada fauna with other Gondwanan Jurassic freshwater fish faunas shows close similarities with the roughly contemporaneous fauna of Talbragar, Australia, which also includes an abundant basal teleost and coccolepidids. In contrast, there are marked differences with the faunas of the Early to Middle Jurassic Kota Formation of India, the Late Jurassic to Early Cretaceous Stanleyville beds of the Democratic Republic of the Congo, and the probably Late Jurassic Tacuarembó Formation of Uruguay, in which basal, non-teleostean neopterygians and sarcopterygians are abundant.
Adriana López-Arbarello. Bayerische Staatssammlung für Paläontologie und Geologie, Richard-Wagner-Strasse 10, D-80333 München, Germany.
and Museo Paleontológico Egidio Feruglio, Av. Fontana 140, 9100 Trelew, Argentina
Emilia Sferco. Laboratorio de Paleontología Evolutiva de Vertebrados, Departamento de Geología, Facultad de Ciencias Exactas y Naturales, Universidad de Buenos Aires, Ciudad Universitaria, Pabellón II, 1428 Buenos Aires, Argentina
and Museo Paleontológico Egidio Feruglio, Av. Fontana 140, 9100 Trelew, Argentina
Oliver W.M. Rauhut. Bayerische Staatssammlung für Paläontologie und Geologie, Richard-Wagner-Strasse 10, D-80333 München, Germany.
and Museo Paleontológico Egidio Feruglio, Av. Fontana 140, 9100 Trelew, Argentina
and Department of Earth and Environmental Sciences and GeoBioCenter, Ludwig-Maximilians-University, Richard-Wagner-Strasse 10, 80333 Munich, Germany
Keywords: New genus; Chondrostei; Coccolepididae; Patagonia; Upper Jurassic; freshwater fishes
Final citation: López-Arbarello, Adriana, Sferco, Emilia, and Rauhut, Oliver W.M. 2013. A new genus of coccolepidid fishes (Actinopterygii, Chondrostei) from the continental Jurassic of Patagonia, Palaeontologia Electronica Vol. 16, Issue 1; 7A 23p. https://doi.org/10.26879/348
Due to a bias in the fossil record, Jurassic freshwater fish faunas are rather scarce and only a few are known worldwide: several poorly known fish assemblages in Asia (Chang and Miao, 2004) and North America (Wilson and Bruner, 2004), the fish assemblages from the Morrison Formation (Kimmeridgian-Tithonian) in the USA (Kirkland, 1998), the fishes from the Early Jurassic Kota Formation, India (Prasad et al., 2004), the continental sequence of the Late Jurassic to Early Cretaceous Stanleyville Beds, Democratic Republic of the Congo (Myers et al., 2013), the Talbragar Beds (Tithonian) in Australia (Woodward, 1895), the Tacuarembó Formation in Uruguay (Late Jurassic-earliest Cretaceous?; Soto et al., 2012), and the Cañadón Calcáreo Formation (Oxfordian-Tithonian) in central Chubut in Argentina (López-Arbarello et al., 2008).
The Almada Fauna is preserved in the lowermost part of the Cañadón Calcáreo Formation (Oxfordian-Tithonian) and it is mainly composed of very well-preserved and abundant teleosts, representing a single species, and numerous specimens representing a small chondrostean. Other actinopterygians, probably non-teleostean neopterygians, are also present, but much less represented and poorly preserved. The present article is focused on the study of the chondrosteans from the Almada Fauna, which were originally described as †Oligopleurus groeberi Bordas, 1943, and later moved to the genus †Coccolepis (Bocchino, 1978).
López-Arbarello et al. (2002) first reported on the close phylogenetic relationships between coccolepidids (including †Coccolepis bucklandi and †"Coccolepis" groeberi, the latter representing a new genus, described herein) and the Acipenseriformes, and Hilton et al. (2004) also suggested possible affinities of †Coccolepis with the chondrosteans as defined by Patterson (1982), i.e., the group including the Acipenseriformes (sturgeons and paddlefishes) and their fossil relatives. The history of acipenseriforms can be traced back to the Early Jurassic (Hilton and Forey, 2009). The history of the two recent acipenseriform families Polyodontidae and Acipenseridae is known back to the Early Cretaceous (~Hauterivian; Grande et al., 2002) and Middle Jurassic (Choudhury and Dick, 1998), respectively. However, the fossil record of the group is very patchy, especially in Mesozoic rocks, and, except for a few recently revised species (Grande and Bemis, 1991; Grande et al., 2002; Grande and Hilton, 2006), most of the other fossil taxa are rather poorly understood (Hilton and Grande, 2006). The fossil relatives of the Acipenseriformes within Chondrostei are still debated and not well established (Stensiö, 1921, 1932; Nielsen, 1949; Patterson, 1982; Grande and Bemis, 1996). Pending a cladistics analysis of the relationships of †"Coccolepis" groeberi, this contribution is dedicated to the taxonomy of this basal chondrostean from the Jurassic of Patagonia, including the description of the new genus and a discussion of its systematic position. A comparison between the Almada Fauna and the other Jurassic freshwater ichthyofaunas is also included.
Institutional abbreviations. MACN, Museo Argentino de Ciencias Naturales "Bernardino Rivadavia," Buenos Aires, Argentina; MPEF-PV, Vertebrate paleontology collection at the Museo Paleontológico Egidio Feruglio, Trelew, Argentina.
Anatomical abbreviations:ao, antorbital bone; ang, angular bone; a.p.psph, anterior process of parasphenoid; br, branchiostegal ray; cl, cleithrum; cla, clavicle; c.fu, caudal fulcra; d, dentary; d.a, dorsal arcual ossification; dpt, dermopterotic; dsph, dermosphenotic; e, epural; ex, extrascapular bone; fr, frontal; fr.fu, fringing fulcra; gu, gular plate; h1, first hypural; h.a, haemal arch; h.s, haemal spine; hy, hyomandibular bone; io, infraorbital bone; io.c, infraorbital sensory canal; m.c, mandibular sensory canal; m.r, middle radial; mx, maxilla; na, nasal bone; n.a, neural arch; op, operculum; pa, parietal bone; pcl: postcleithrum; php, parhypural; pmx, premaxilla; pop, preoperculum; pp, parapophysis; p.r, proximal radial; pro, postrostral bone; psp, parasphenoid; ptt, posttemporal bone; r, radials; ro, rostral bone; s, scale; scl, supracleithrum; sct, scute; sn, supraneurals; so.c, supraorbital sensory canal; sop, suboperculum; sr, sclerotic ring; v.a, ventral arcual ossification. An 'l' and 'r' between brackets after the abbreviations indicates left and right elements, respectively.
The fishes belong to the so-called Almada fauna (López-Arbarello et al., 2008) of north-central Chubut province. The type locality of this fauna is placed at Puesto Almada, Estancia El Torito, some 20 km north of the village of Cerro Cóndor, at the Ruta Provincial N° 12 in the valley of the Chubut River (Figure 1, Figure 2). Although the "estratos de Almada" (Almada beds) have long been known for their abundant and well-preserved fishes (Piatnitzky, 1936; Bordas, 1943; Bocchino, 1967, 1978), their exact stratigraphic placement and referral to a geological unit have so far remained controversial. Sometimes considered to be a local unit of Late Cretaceous age (e.g., Tasch and Volkheimer, 1970; Bocchino, 1978), they have recently often been included in the Cañadón Asfalto Formation (e.g., Turner, 1983; Silva Nieto et al., 2002; Cabaleri et al., 2010a, 2010b), a mainly lacustrine unit that is widely exposed further south along the Chubut River valley (Stipanicic et al., 1968; Figure 1) and to which a Middle-Late Jurassic (Callovian-Oxfordian) age has traditionally been assigned (Tasch and Volkheimer, 1970; Page et al., 1999; Silva Nieto et al., 2002).
The "estratos de Almada" are part of the infillings of the Cañadón Asfalto Basin, a large-scale hemigraben structure that developed in the course of the initial rifting of the supercontinent of Gondwana during the Triassic and Early Jurassic and suffered some compressive stresses in the Neogene (Figari and Courtade, 1993; Figari, 2005). Figari and Courtade (1993; see also Page et al., 1999; Figari, 2005) subdivided the sedimentary infill of this basin in a sequence stratigraphic approach into four megasequences (megasequence 0 to megasequence III), representing different phases in the evolution of the basin, with sediments and volcanic rocks ranging from the Early Jurassic to the Late Cretaceous. According to their scheme, the "estratos de Almada" belong to megasequence II, whereas the Cañadón Asfalto Formation sensu Stipanicic et al. (1968) belongs to the megasequence I, with both sequences being separated by a slight angular unconformity. These authors accepted the Callovian-Oxfordian age for the megasequence I (Cañadón Asfalto Formation sensu Stipanicic et al., 1968), but argued for a latest Jurassic to Early Cretaceous age for their megasequence II, citing biostratigraphic evidence from unpublished internal reports of the oil company YPF as source for this date. Confusingly, Figari and Courtade (1993) nevertheless used the name "upper section of the Cañadón Asfalto Formation" for this unit.
Silva Nieto et al. (2002) also maintained the "estratos de Almada" in the Cañadón Asfalto Formation, but argued that the lower and upper section of this formation were concordant and both represented a Callovian-Oxfordian age. The two sections were formally denominated as Las Chacritas and Puesto Almada Members, respectively, by Silva Nieto et al. (2003), and this scheme was followed by Cabaleri et al. (2005, 2010a, 2010b), Cabaleri and Armella (2005), and Gallego et al. (2011). However, these authors noted an increasing discordance in age between the two members, with new bio- and chronostratigraphic evidence indicating a Bajocian-Bathonian age for the Las Chacritas Member (Volkheimer et al., 2008; Cabaleri et al., 2010b) and an Oxfordian-Tithonian age for the Puesto Almada Member (Cabaleri et al., 2010a, 2010b; Gallego et al., 2011). Nevertheless, both members were maintained in the Cañadón Asfalto Formation.
In a geological study of an area northeast of the type locality of Puesto Almada, Proserpio (1987) defined a new geological unit, the Cañadón Calcáreo Formation, of presumably Late Jurassic to Early Cretaceous age. Though they maintained the denomination as "upper section of the Cañadón Asfalto Formation," Figari and Courtade (1993) noted that this Cañadón Calcáreo Formation is equivalent to their megasequence II, in which they also included the "estratos de Almada" (see also Cortiñas, 1996; Page et al., 1999; Figari, 2005). Following this revision, and based on own observations in the field, Rauhut (2003, 2006a, 2006b), López-Arbarello (2004), Rauhut et al. (2005), López-Arbarello et al. (2008), and Carballido et al. (2011) referred to this unit as Cañadón Calcáreo Formation, including the "estratos de Almada" (Figure 1). Although Volkheimer et al. (2008, 2009) accepted the referral of the "estratos de Almada" to the Cañadón Calcáreo Formation, assigning an Early Cretaceous (Valanginian) age to this unit based on palynological evidence from the type section of this unit, the same authors later (Cabaleri et al., 2010a; Gallego et al., 2011) returned to the use of the name "Puesto Almada Member of the Cañadón Asfalto Formation" for the "estratos de Almada..." The argument for this change was that a Late Jurassic (Tithonian) chronostratigraphic date obtained from the type locality at Puesto Almada (Cabaleri et al., 2010b) was at odds with the assumed Early Cretaceous age of the Cañadón Calcáreo Formation. Curiously, however, they did not apply the same logic to the conflicting dates of the Las Chacritas and Puesto Almada members, though the time difference between the radiometric Tithonian age of Puesto Almada and the assumed Valanginian age of the type section of the Cañadón Calcáreo Formation is considerably less than that between the former and the radiometrically obtained Bajocian-Bathonain age for the Las Chacritas Member (≈9 m.y. versus ≈20 m.y.; Gradstein et al., 2004) of the Cañadón Asfalto Formation.
Extensive fieldwork in the Jurassic rocks of the middle Chubut valley by one of us (OWMR) in collaboration with the Museo Paleontológico Egidio Feruglio in the past 12 years has yielded new data on the geology of the "estratos de Almada," their distribution and their assignment to a certain geological unit. First, larger scale excavations in the classical fish localities at Puesto Almada and Estancia Limonao, on the other side of the Chubut River (Figure 2), confirmed that the main fish beds exposed in these two localities represent the same layer. Furthermore, we collected samples of tuff layers at Puesto Almada and the Cañadón Calcáreo type locality that yielded equivalent ages of c. 157.4 Ma (Oxfordian; Cúneo et al., 2013). The succession of the geological sequence containing the fish beds is equivalent in all of the localities, though the thickness of the different layers may vary, probably due to deposition on an existing paleorelief of rocks of the Lonco Trapial Group. In places where the contact with the underlying unit is exposed, such as in a small canyon west of Puesto Almada and at the entrance of the Cañadón Los Chivos, the sequence starts with a coarse conglomerate that unconformably overlies the Lonco Trapial Group. The conglomerate is an orthoconglomerate composed of angular to well-rounded clasts of reworked Lonco Trapial Group and varies considerably in thickness. The lower part of the sequence above the conglomerate is dominated by lacustrine shales and mudstones, with intercalations of sandstones and tuffites. The fish beds are placed in the upper part of this section. Thick sandstone channels a few meters above the fish beds mark the change to more fluvial conditions in the upper part of the sequence, which is dominated by sandstones (often with channel structures and cross-bedding), tuffites and tuffs. This general sequence is equivalent to that of the Cañadón Calcáreo type locality (see Volkheimer et al., 2009), and a visit to this locality in 2009 also led to the discovery of fish remains in the lacustrine shales in the lower part of this section. Furthermore, we collected samples of tuff layers at Puesto Almada and the Cañadón Calcáreo type locality that yielded equivalent ages of 155.5 Ma (Oxfordian-Kimmeridgian; Cúneo et al., 2013). Finally, Zavattieri et al. (2010) analyzed more extensive palynological samples from the Cañadón Calcáreo type section and came to the conclusion that the latter is no younger than Tithonian in age. Thus, we consider the "estratos de Almada" to be equivalent to the Cañadón Calcáreo Formation of Proserpio (1987). Volkheimer et al. (2009) argued that the Cañadón Calcáreo Formation at its type locality is overlain in an erosional unconformity by the Chubut Group. However, our own observations in the field indicate that this presumed unconformity actually represents a local formation of an erosional basis of a river channel and cannot be traced laterally over larger distances. Thus, we consider all of the rocks at the Cañadón Calcáreo type locality to represent the same sedimentological sequence, as did Proserpio (1987) and Figari (2005), with the latter assigning a total thickness of some 1400 m to this profile.
Regardless of the referral of the Almada fauna to a particular geological unit, a Late Jurassic age for this fauna can by now be regarded as well established. Analysis of a tuff some 50 m above the fish beds from the locality Punta Biotita (Figure 2), in a small canyon west of Puesto Almada, resulted in a Tithonian age (147±3 Ma; Khoukarsky, personal commun. in Rauhut, 2006b), which is identical to an age reported from the type locality by Cabaleri et al. (2010a; this date might refer to the same tuff sample as the date noted by Rauhut [2006a], since these authors note that the sample for dating was provided by O. Rauhut. In this case, the sample is not derived from Puesto Almada, as noted by Cabaleri et al., but from a locality some 1000 m further to the west). On the other hand, dating of a tuff collected by one of us (OWMR) in the Puesto Almada area, also some 30 m above the fish beds, resulted in an uppermost Oxfordian-lowermost Kimmeridgian age (Cúneo et al., 2013). Thus, more data is needed to establish the exact age within the Upper Jurassic.
Apart from the Almada fish fauna, vertebrate remains from other parts of the Cañadón Calcáreo Formation include a new species of crocodile from the fluvial beds above the fish layers at Puesto Almada (Pol et al., 2011), the sauropod dinosaurs Tehuelchesaurus (Rich et al., 1999; Carballido et al., 2011), Brachytrachelopan (Rauhut et al., 2005) and an undeterminate brachiosaurid (Rauhut, 2006a), as well as undescribed remains of theropod dinosaurs and temnospondyl amphibians (OWMR pers. obs.). Fragmentary turtle remains reported from this formation by Rauhut (2006a) and described by Sterli (2009) are now considered to come from the Lower Cretaceous Los Adobes Formation (OWMR and Diego Pol, pers. obs.).
The fishes mainly occur in the southern part of the outcrop area of the Cañadón Calcáreo Formation (Figure 1), which has a total of up to 60 m of lacustrine sediments at its base. Fish remains occur in various layers, but are especially abundant in a single layer (about 80 cm) near the top of the lacustrine sequence.
This main fish-bearing stratum of the Cañadón Calcáreo Formation is found in at least seven localities (Figure 2): Puesto Almada (Estancia Farías), Punta Biotita (some 1000 m west of Puesto Almada), Estancia Limonao, two localities at the entrance of the Cañadón Los Chivos, Cañadón Las Minas, and Sierra de la Manea. Most of these localities are placed on both sides of the Chubut River, up to 8 km distant from one another. Only in the most distant locality of La Manea, which is placed some 30 km away from Puesto Almada, several layers with abundant fish remains appear, intercalated with desiccation cracks.
Although these localities are distant from one another, they bear a remarkably uniform fish composition. All of the fish-bearing layers contain the teleost †Luisiella feruglioi (new combination after Sferco, 2011), the chondrostean †Condorlepis gen. nov., and a diverse array of dominantly teleost species (Figure 3). A predator-prey relationship between †Luisiella feruglioi and †Condorlepis gen. nov. is suggested by the occurrence of †Condorlepis specimens with teleost remains in their digestive system and the frequent association of both taxa.
†Luisiella feruglioi is the principal component of the fish fauna, representing more than the 85% of the fishes; †Condorlepis gen. nov. is represented by less than 10%. Although this is the generalized case, in the Estancia Limonao, the specimens of †Condorlepis gen. nov. make up to 25% of the total number of fishes. Other actinopterigyans (indeterminate, though certainly not referable to †Luisiella or †Condorlepis) are rare and appear exclusively in Sierra de la Manea and Estancia Limonao (Figure 3). In Sierra de la Manea, †Luisiella feruglioi represents up to 80% and †Condorlepis gen. nov. 10-15% of the total fish fauna, with this genus accounting for up to 50% of the fish fauna in some layers in this locality (Figure 3.2).
The remarkably uniform fish composition found in all the studied localities of the Cañadón Calcáreo Formation suggests that a single lake or a series of smaller interconnected lakes were present. Additionally, the absence of fossil plants and tetrapods supports the hypothesis of a single large lake. The main mass occurrence of fishes in a single, tuffacious layer indicates a mass-mortality event, possibly triggered by volcanic activity.
Subclass ACTINOPTERYGII Cope, 1887
Infraclass ACTINOPTERI Cope, 1871
Series CHONDROSTEI Müller, 1844
Family †COCCOLEPIDIDAE Berg, 1940
Diagnosis (emended from Berg, 1940 and Hilton et al., 2004). Chondrostean fishes with the following combination of characters: dermal bones of the skull roof and maxilla ornamented with small and regularly distributed tubercles or sharply pointed denticles; anterior abdominal scales are of the amioid-type; nasal bones contact only anteriorly, posteriorly separated by postrostral; small postrostral bone not reaching the rostral; maxilla with large postorbital plate; supracleithrum is as large or larger than cleithrum.
Included genera. †Coccolepis Agassiz, 1843, from the Late Jurassic of Solnhofen, Germany; †Sunolepis Liu, 1957, from the Late Jurassic or Early Cretaceous of Yumen, Gansu Province, China; †Plesiococcolepis Wang, 1977, from the Early Jurassic of Lingling-Hengyang, Hunan Province, China; †Iyalepis Sytchevskaya, 2006, from the Early to Middle Jurassic Cheremkhovskaya Formation of Baikal Region in Siberia; †Morrolepis Kirkland, 1998, from the Late Jurassic Morrison Formation, USA; †Condorlepis gen. nov., from the Late Jurassic (Oxfordian-Tithonian) Cañadón Calcáreo Formation, Chubut Province, Argentina.
Genus †COCCOLEPIS Agassiz, 1843
Emended diagnosis. Coccolepidid fish with the following combination of characters: dermal bones of the skull roof, scales, and fin rays ornamented with mostly regularly arranged sharply pointed, posteriorly directed denticles; lower jaw long and very slender; fringing fulcra present in pectoral and caudal fins only.
Type species. †Coccolepis bucklandi Agassiz, 1843, from the Late Jurassic of Solnhofen, Germany.
Other accepted species. †Coccolepis liassica Woodward, 1890, from the Early Jurassic (Sinemurian) of Dorset, England; †C. andrewsi Woodward and Sherborn, 1890, from the earliest Cretaceous Lower Purbeck Beds at Wiltshire, England; †C. australis Woodward, 1895, from the Late Jurassic (Tithonian) Talbragar Beds in Australia; †C. macroptera Traquair, 1911, from the Early Cretaceous of Bernissart, Belgium; †C. aniscowitchi Gorizdro-Kulczycka, 1926, from the Late Jurassic Kara-Tau, Kazakhstan; †C. woodwardi Waldman, 1971, from the Early Cretaceous of Koonwarra, Victoria, Australia.
Genus †CONDORLEPIS gen. nov.
Derivation of name. The new generic name is a combination of the name Cerro Cóndor, which is the small village closest to the type locality, and the Greek "lepis", a scale.
Diagnosis. As for the type and so far only known species.
Type species. †Oligopleurus groeberi Bordas, 1943
†Condorlepis groeberi (Bordas, 1943) n. comb.
1943 †Oligopleurus groeberi Bordas: Physis 19(53): 317, pl. 2.
1978 †Coccolepis groeberi Bocchino: 310-317, fig. 2, pl. 2.
1987 †Coccolepis groeberi Cione and Pereira: 289-290, pl. 2, pl. 5: fig. B.
Lectotype. MACN 14434, moderately well-preserved, almost complete specimen missing the posterior half of the caudal fin (Estimated TL 126 mm; Figure 4.1).
Paralectotype. MACN 14433, incomplete specimen including a well-preserved caudal fin and almost complete anal fin (Figure 4.2).
Referred specimens. MACN 14432, 18551 (including 18630A, 18552 and 18553), 18561, 18562, 18575; MPEF-PV 1496-5A, 1556-6, 1731, 1732, 1733, 1766, 1767, 3958, 10504-507.
Diagnosis. Coccolepidid fish with the following combination of characters: dermal bones of the skull roof, maxilla and scales, but not fin rays, ornamented with small and irregularly distributed tubercles; small rostral; lower jaw long and slender, but robust; suboperculum, branchiostegal and gular plates ornamented with low concentric striae; gular plate small and rounded, traversed by a sensory canal; supracleithrum longer than cleithrum; small, oval postcleithrum; fringing fulcra present in caudal fin only.
Type locality. According to Bordas (1943: 316) the type specimens were found in "Valle medio del Río Chubut, en el lote 24 sección Ii, cerca de la casa de Marcos Almada, aguas arriba del Paso de los Indios (Territorio del Chubut)" [central Río Chubut valley, in the lote 24 section Ii, close to the house of Marcos Almada, upstream from the Paso de los Indios (Territory of the Chubut)]. The house of Marcos Almada is known as Puesto Almada, Estancia El Torito, and is located some 20 km north of the village of Cerro Cóndor, at the Ruta Provincial N° 12 in the valley of the Chubut River (Figure 2).
Type horizon. "Estratos de Almada," basal lacustrine section of the Cañadón Calcáreo Formation (Late Jurassic: Oxfordian-Tithonian).
Like other chondrostean fishes, †Condorlepis groeberi (Bordas, 1943) n. comb. is a very slender fish, with the peculiarity that the body is deepest at the relatively large head and gradually decreases in depth posteriorly, ending in a strongly heterocercal tail with a very long body lobe that culminates in a short cercus-like extension (Figure 4, Figure 5). The total length (TL) of the complete specimens (MPEF-PV 1731, 1732, 1733, 3958, and 1767) varies between 85 and 116 mm. The total length of the lectotype (MACN 14434) is about 126 mm, estimated according to the ratio of the head length relative to the total length calculated for the complete specimens (Table 1). The largest specimen is also incompletely preserved and its total length is estimated as 185 mm (MPEF-PV 1766). The head is longer than deep (on average HD/HL = 0,81; Table 1) with the orbit placed in the anterior half of the skull, the snout is blunt and the suspensorium is very inclined (Figure 6). The length of the head measured from the anterior border of the nasals to the posterior border of the operculum at a level right before the articulation of the supracleithrum and the cleithrum is on average 23% of the TL (range: 21–24%, n=6). The maximum depth of the postcranium is immediately behind the pectoral girdle and represents around 17% of TL (range: 17–18%, n=5). The pelvic fins are placed at 39% of TL (range: 35–43, n=6), and the dorsal and anal fins are placed at 44% of TL (range: 42–47%, n=6) and 58% of TL (range: 54–65, n=6), respectively. The ranges of variation for these proportions are not related to the size of the specimens (Table 1).
The preservation of the skull is generally rather poor and most of the bones are crushed. In many cases the real borders of the bones are incompletely preserved and their outline has been reconstructed. Despite such difficulties, besides the general gross morphology, the specimens have revealed several anatomical details and features that are systematically important.
Snout and skull roof. The snout is formed by a small rostral, which is traversed by the ethmoidal commissure, a relatively small anamestic postrostral and paired nasals (Figure 7, Figure 8, Figure 9). The shape of the nasals resembles an inverted bottle with a broad and largest dorsal portion, and a narrow ventral neck and the bone is traversed by the anterior portion of the supraorbital sensory canal (Figure 8). Lateral to the path of the canal, the dorsal portion of the nasal is ornamented with relatively broad parallel ridges. The two nasals are separated dorsally, but they meet at the midline along the ventral, narrow portion. Between the dorsal portions of the nasals, a median anamestic bone is sutured to the anterior border of the frontals (Figure 8.2). Although this bone does not reach the rostral ventrally, it is probably homologous to the postrostral bone of †Birgeria and other basal actinopterygians.
The skull roof has a perfectly rounded profile (MACN 14434; Figure 6) and is oriented in antero-ventral to postero-dorsal direction. The frontals are the largest bones in the roof of the skull (Figure 6, Figure 7, Figure 9). They do not extend beyond the anterior rim of the orbit and consist of approximately equally large orbital and postorbital portions. The two frontals meet at the dorsal midline in an almost straight suture (MPEF-PV 1731, 1732). Posterior to the frontals, the two parietals are approximately quadrangular. The fronto-parietal and the inter-parietal sutures are almost straight. The dermopterotics are very large, sutured to the lateral border of the parietals and extending forwards suturing to the postorbital portion of the frontal and reaching close to the orbital margin. There is a single pair of narrow, laterally elongated extrascapulars suturing the parietals and dermopterotics posteriorly. The extrascapulars are widest at their lateral borders and narrow towards the midline. Posterior to the extrascapulars there is a single pair of large posttemporal bones. Frontals, parietals, dermopterotics, extrascapulars, and posttemporals are ornamented with densely and irregularly arranged tubercles.
The supraorbital sensory canal runs from the nasals posteriorly almost straight and parallel to the inter-frontal suture, and ends in the anterior portion of the parietal (Figure 7, Figure 9). The temporal canal runs through the latero-ventral margins of the posttemporal, extrascapular and dermopterotic bones and turns upwards rather abruptly at the anterior margin of the dermopterotic to meet the infraorbital canal in the dermosphenotic bone. The extrascapular bones are further traversed by the supratemporal commissure.
Circumborbital bones. Three slender sclerotic bones are preserved in MPEF-PV 3958 (Figure 9), but the total number was probably four. Starting at the ethmoidal commissure, the infraorbital sensory canal is contained in the antorbital, five infraorbital bones and the dermosphenotic. The antorbital bone, which is best preserved in MPEF-PV 3958 and 10504, is Y-shaped and carries the junction between the ethmoidal commissure and the supraorbital and infraorbital canals (Figure 7, Figure 8, Figure 9). The first infraorbital bone is small and subrectangular, longer than deep, and is located at the anteroventral corner of the orbit. Two other infraorbitals form the ventral margin of the orbit, these two infraorbitals are longitudinally elongated, the first of them being short, a little longer than deep, but the second is long and a little deeper posteriorly. The fourth infraorbital is located at the posteroventral corner of the orbit, it extends into the dorsal margin of the orbit and is expanded posteriorly (the dorsal portion of this bone is not preserved in MPEF-PV 1731). The posterior border of the orbit is completed by one small and tubular infraorbital bone and the dermosphenotic, which is also small and tubular, and is almost dorsoventrally oriented. Supraorbital bones are absent.
Jaws. The upper jaw is formed by very small premaxillae and large maxillae (Figure 6, Figure 9, Figure 10). The premaxillae are generally not preserved, but MPEF-PV 1731 preserves a small and very slender premaxilla articulating with the right maxilla (Figure 10.1). This small premaxilla is approximately five times longer than deep and bears small conical teeth. The maxillae have a very thin infraorbital portion and a widely expanded postorbital portion. The infraorbital portion tapers anteriorly and has posteriorly divergent slightly convex ventral and slightly concave dorsal margins. The postorbital portion of the maxilla is incompletely preserved in the studied specimens, but it can be reconstructed. The dorsal portion is best preserved in the disarticulated maxilla in MPEF-PV 1496-5A (Figure 10.2). Behind the orbit, the dorsal border of the maxilla bends abruptly upwards, forming a rectangular postorbital plate, which is almost 3 times higher than the maxillary infraorbital portion at its maximal height. The dorsal border is convex, curving in posteroventral direction, and the posterior border is straight and inclined posteriorly. The anterior and posterior borders divert upwards, with the posterior border more posteriorly inclined than the anterior border. The ventral border of the postorbital portion is concave and, thus, the ventral border of the maxilla taken as a whole is sinuous, turning from convex to concave.
The lower jaw is poorly preserved in the studied specimens. A coronoid process of the neopterygian type is absent and the lateral surface is mainly made up by the large dentary (Figure 7, Figure 9). The mandibular sensory canal runs very close to the ventral margin of the bone and exits the dentary before the symphysis. The dentary and maxilla bear two rows of conical teeth: a lateral row of very minute conical teeth and a medial row of larger and sharp conical teeth. Other bones or details of the lower jaw are not discernable.
Palatoquadrate and parasphenoid. Of the palatoquadrate only the very elongated and sharply pointed dermopalatine bones are observable. The anterior portion of the dermopalatines resembles the anterior portion of the maxillae very closely and bears a single row of conical teeth, which are similar to the large medial maxillary teeth.
The parasphenoid is well preserved in several specimens. Like in other chondrosteans, the orbital portion of the parasphenoid is broad and presents a distinct median anterior process and large ascending processes (Figure 7, Figure 9, Figure 10.1).
Opercular bones and hyoid arch. The preoperculum is very narrow and inclined, resembling the shape and position of the underlying hyomandibula, but narrowing posteroventrally (Figure 6). The operculum is quadrangular in shape and notably smaller than the suboperculum (Figure 6, Figure 7). The suboperculum is fan-shaped with an undulated surface and has a broad anterodorsal process.
A series of numerous branchiostegal rays is incompletely preserved in the studied specimens, although almost complete series, with 11 and 12 plates preserved in MPEF-PV 1731 and 3958 (Figure 7, Figure 9). The total number of branchiostegals remains unknown. Each branchiostegal is plate-like and ornamented with a central shallow dome and concentric ridges. Anterior to the series of branchiostegals there is a single gular plate, which is very small, shorter than broad, with an almost straight posterior border (Figure 9). It is also ornamented with concentric ridges and it is transversally traversed by the mandibular sensory canals. The mandibular sensory canal from one side enters the gular plate from the dentary, runs into a gular commissure, and exits to the dentary on the other side (MPEF-PV 3598).
Among the elements of the hyoid arch, only the hyomandibula is visible. Like in †Birgeria, the hyomandibula consists of a laterally compressed dorsal, almost horizontal shank, and a ventral, posteroventrally inclined shank (Figure 7, Figure 9). The dorsal shank is c. 1.3 times longer than the ventral shank. The generally rod-like hyomandibula is narrower in the middle, expanding both proximally and distally, and the transition between the dorsal and ventral shanks is very gradual. There is no opercular process or foramen for the truncus hyoideomandibularis.
Vertebral column and caudal fin. Only dorsal and ventral arcual elements are ossified in the vertebral column of †Condorlepis, and the notochord is persistent (Figure 4, Figure 5, Figure 6, Figure 11). There are ~34-35 preural vertebrae, including 21-23 abdominal vertebrae (Table 1). It has not been possible to identify a parhypural with certainty. Therefore, our criterion to distinguish between ural and preural vertebrae is as follows: we identify the last preural vertebra as the vertebra with a complete neural arch and spine and the first enlarged and laterally compressed haemal spine.
In the abdominal region of †Condorlepis, the arcual ossifications consist mainly of separate ventral and dorsal arcocentra (Figure 11.1). Although ribs are not ossified, each ventral arcocentrum forms a short, but distinct parapophysis. The dorsal arcual ossifications are high and laterally compressed, constricted in the middle and expanded both dorsally and ventrally. The ventral portion of these basidorsal ossifications clearly corresponds to the neural arches, and we interpret the dorsal portion as paired neural spines. All of the abdominal neural spines are paired in MACN 18630 and MPEF-PV 1731 (Figure 11.2), but the condition is variable and the neural spine is unpaired and relatively short in the last abdominal vertebra in MPEF-PV 3958, and in MPEF-PV 1733 and 1556-6 the neural spines of the two first caudal vertebrae are paired. The first haemal arch is small and has no haemal spine (Figure 11.2).
The caudal vertebrae are also only formed by arcual ossifications consisting of neural and haemal arches and spines. These neural spines are mostly unpaired, but one or two neural spines in the caudal peduncle might be paired (MPEF-PV 1731, 1733, 3958; Figure 12.2). Nine neural ural arches and 11 epurals are ossified in the ural region in MPEF-PV 1731. We interpret these latter elements as true epurals (i.e., detached neural spines) sensu to Schultze and Arratia (1989) because they are directly associated with the neural arches and no neural spine is ossified in the ural region (Figure 12). The ural skeleton is completed with numerous enlarged and laterally compressed hypurals. Twelve hypurals are visible in most of the specimens, but the exact number of hypurals is unknown because the most posterior elements are hidden below the scales of the body lobe.
There is a complete series of 14-18 rod-like supraneurals (Table 1; Figure 4, Figure 5, Figure 6, Figure 11) between the skull and the dorsal fin. Up to two supraneurals might be located under the first dorsal pterygiophores, but this condition is variable and independent of the total number of supraneurals.
The caudal fin is heterocercal and ends in a short cercus-like extension of the body lobe, which extends beyond the last lepidotrichia and is covered with tiny scales (Figure 4.2, Figure 13.1). This structure is much shorter than the cercus (=caudal filament) of Scaphirhynchus species or Pseudoscaphirhynchus kaufmanni (Hilton et al., 2011) and the lateral line apparently ends right behind the last fin ray at the base of the cercus-like extension. The scale covering of the body lobe reaches up to the base of the eighth to the sixth hypural. The caudal fin web is made up of c. 60 lepidotrichia and is deeply excavated, with the dorsal lobe longer than the ventral lobe, which forms a rounded distal end (Figure 4; MACN 14433, MPEF-PV 1767). All caudal fin rays are evenly segmented from their bases. The following features concerning the pattern of caudal fin rays are best preserved in MPEF-PV 1731 and, thus, although the pattern is the same in all of the studied specimens, precise numbers are based on this specimen only. The first ventral caudal fin ray articulates with the parhypural and is very short and unbranched (Figure 12). The following eight rays increase in length, gradually forming the ventral margin of the fin, and are also unbranched. The ninth ray gives three branches, which also increase gradually in length and contribute to the ventral margin of the fin. The distal ends of these marginal fin rays intercalate with numerous slender fringing fulcra (Figure 13.2). One ventral caudal fulcrum precedes the ventral caudal fin rays that insert onto the body directly in front of the parhypural. In the dorsal lobe, one unpaired dorsal caudal fulcrum and c. 44 paired caudal fulcra formed the dorsal margin of the body lobe.
Dorsal and anal fins. The dorsal and anal fins are made up of numerous tightly packed lepidotrichia (Figure 4, Figure 5, Figure 14). Resembling the case of the ventral margin of the caudal fin, the most anterior dorsal and anal rays are unbranched and form the leading edge of these fins, with the first dorsal rays being very short and the few following rays gradually increasing in height. All dorsal and anal fin rays are evenly segmented from their bases. There are no fringing fulcra in the dorsal or anal fins.
There is a single series of radials supporting the dorsal and anal fin rays in the smaller specimens, but larger specimens (e.g., MPEF-PV 1731, 1733, 3958, 10506, MACN 18630) have proximal and middle radials ossified separately (Figure 14). The total number of dorsal and anal pterygiophores varies between 19-21 and 18-21, respectively (Table 1). One elongated oval scute lays on the skin preceding the dorsal and anal fins.
Pectoral girdle. The pectoral girdle consists of a triangular supratemporal, a large, dorsoventrally elongated supracleithrum, a distinctly oval postcleithrum and a massive cleithrum and clavicle and is generally very similar to the pectoral girdle in other fossil chondrosteans (e.g., †Birgeria, †Peipiaosteus, †Chondrosteus) (Figure 7, Figure 9, Figure 15). The posttemporal is large and posteroventrally elongated, with a rounded posteroventral border. The supracleithrum has rounded anterodorsal and posteroventral borders, an almost straight anteroventral border and a convex posterodorsal border, and it is extremely long, the supracleithrum being longer than the cleithrum and notably longer than in other known chondrosteans. The lateral line runs through the anteroventral region of the posttemporal, enters the dorsal portion of the supracleithrum, and exits this bone at about half of its length. A small rounded postcleithrum, ornamented with concentric ridges, articulates at the distal end of the supracleithrum.
The dorsal portion of the cleithrum is inclined posteroventrally and tapers toward the distal end. Its ventral end is short and stout, with a posterior border that is straight and nearly vertical. The clavicle is massive and triangular. The pectoral fin consists of at least six elongated radials (MPEF-PV 1731), numerous fin rays, and a pectoral spine (Figure 15). The exact number of rays is unknown, but all rays are evenly segmented from their bases. There are no fringing fulcra in this fin.
Pelvic fins. Like in other chondrosteans, the pelvic fins are of the primitive kind, with c. 17 radials supporting the numerous and tightly packed fin rays (Figure 4, Figure 5). As in the other fins, the fin rays are evenly segmented from their bases, and the leading rays are unsegmented and gradually increase in height.
Squamation. The body of †Condorlepis groeberi is covered with amioid-type scales (Figure 16, Figure 17), as is the case in †Coccolepis bucklandi (Schultze, 1966). Also resembling this latter taxon, the scales in †Condorlepis bear numerous sharp, pointed denticles, but they are not arranged in rows like in the European species. The lateral line is enclosed in a well-ossified duct contained in normal body scales up to the base of the body lobe, where it is contained in small tubular scales and bends sharply following the bases of the caudal fin rays.
Systematic position of †Condorlepisgroeberi
López-Arbarello et al. (2002) presented a phylogenetic hypothesis according to which †Condorlepis groeberi (Bordas, 1943) n. comb. and †Coccolepis bucklandi Agassiz, 1843 are sister groups and closely related to the Acipenseriformes within a monophyletic Chondrostei. Supporting these hypotheses, the detailed anatomical study of †Condorlepis groeberi led to the identification of several phylogenetically potentially important characters shared between these taxa. †Condorlepis groeberi and †Coccolepis bucklandi share a peculiar ornamentation of the dermal bones of the skull and the scales, the same kind of amioid-type scales, the small postrostral bone located between the dorsal halves of the nasals and a particularly large supracleithrum. The same or similar conditions have only been reported for other fishes referred to the family Coccolepididae (Woodward, 1890, 1891, 1895, 1915; Waldman, 1971; Kirkland, 1998).
Supporting the position of †Condorlepisgroeberi as a stem taxon to the Acipenseriformes within a monophyletic Chondrostei, the Patagonian Jurassic species share the following features with the Acipenseriformes: parasphenoid with a median anterior process (Hilton et al., 2011: character 17); opercle smaller than suboperculum (Hilton et al., 2011: character 22); anterior margin of subopercle with anteriorly directed anterodorsal process (Hilton et al., 2011: character 27); single ventral caudal fulcrum (Hilton et al., 2011: character 52); presence of a pectoral fin spine (Hilton et al., 2011: character 53); and the lateral line bending upwards and continuing in the body lobe following the bases of the caudal fin rays. Additionally, †Condorlepis shares with †Birgeria and the Polyodontidae the very long and narrow supracleithrum, and with these fishes and several acipenserids the relative size of the supracleithrum, which is as large or larger than cleithrum. In †Condorlepis the antorbital bone is peculiarly shaped, resembling an inverted Y, as is the case with the most anterior lateral bone in the infraorbital series of Acipenser or †Peipiaosteus. The general shape of this Y-shaped bone in living acipenseriforms, its association to the sensory canals, and its developmental pattern (Jollie, 1980) indicates homology with the antorbital of other actinopterygians like Amia. This hypothesis of homology has been questioned by Hilton (2002). However, it is only the far anterior position of this Y-shaped bone and the impossibility to establish one-to-one correspondence of all the rostral canal elements in living acipenseriforms with bones of other actinopterygians, which challenges the hypothesis of its homology with the antorbital. A similar question of homology applies to the anterior bones in the infraorbital series of ginglymodians (López-Arbarello, 2012).
Despite sharing several characters with the acipenseriforms, †Condorlepis groeberi cannot be referred to the Acipenseriformes because it lacks the following synapomorphies of this clade: palatoquadrates with symphysis between pars autopalatina (Hilton et al., 2011: character 30; Grande and Bemis, 1996: character B1); premaxillary and maxillary bones absent (Hilton et al., 2011: character 32; Grande and Bemis, 1996: character B8).
Comparisons with the Other Continental Fish Faunas from the Jurassic of Gondwana
Most Jurassic freshwater fish assemblages of the Northern Hemisphere are rather poorly understood and distinct fish faunas have rarely been delimited (Kirkland, 1998; Chang and Miao, 2004; Wilson and Bruner, 2004; Foster and Heckert, 2011). Thus, a comparison of the Almada Fauna with contemporaneous Laurasian ichthyofaunas is not possible. Among the Jurassic fish assemblages from Gondwana, the fishes from the Early Jurassic Kota Formation, India, include two hybodontoid sharks, one coelacanth, two dapediids, two ginglymodians, and two possible halecomorphs (Prasad et al., 2004; López-Arbarello et al., 2008). The continental part of the Stanleyville Group in the Democratic Republic of Congo (Late Jurassic-Early Cretaceous; Myers et al., 2011) has yielded mawsoniid coelacanths, two basal neopteygians of uncertain relationships, a ginglymodian, and several basal teleosts or teleosteomorphs (Saint-Seine and Casier, 1962; Taverne, 2011a, 2011b). In South America, the Late Jurassic-earliest Cretaceous? Tacuarembó Formation of Uruguay includes a paleoichthyofauna represented by hybodontid sharks (Perea et al., 2001), ceratodontiform dipnoans (Soto and Perea, 2010), a mawsonid coelacanth (Soto et al., 2012) and ginglymodians (Walther, 1932; López-Arbarello et al., 2008; Perea et al., 2009). In contrast, the Almada Fauna includes one species of teleost, †Luisiella feruglioi, the chondrostean †Condorlepis groeberi, and poorly preserved basal actinopterygians of uncertain relationships. Therefore, even though the relationships among the teleosts and teleosteomorphs present in all these faunas are still unknown, the absence of chondrichtyans, coelacanths, dipnoans, and ginglymodians, and the presence of a chondrostean make the composition of the Almada Fauna notably different from the above mentioned Jurassic freshwater fish faunas of Gondwana.
In contrast, the fish fauna of the Cañadón Calcáreo Formation is remarkably similar to that of the Talbragar Beds in Australia (Woodward, 1895). The Talbragar Fauna also includes a single teleost, †Cavenderichthys talbragarensis (Woodward, 1895), a single chondrostean, †Coccolepis australis Woodward, 1895, four teleosteomorph ("pholidophoriformes") aphnelepid species (†Aphnelepis australis, †Aetheolepis mirabilis, †Archaeomaene tenuis and †Madariscus robustus) and one fragmentary remain of a coelacanth. Also, the geological settings and taphonomic background of the two faunas are similar. The Talbragar fishes also occur in a single horizon within the stratigraphic column, representing an event of mass mortality due to volcanic activity within a freshwater environment (Bean, 2006).
†Luisiella feruglioi shares very similar morphological features with †Cavenderichthys talbragarensis and the two species are phylogenetically closely related (Sferco and López-Arbarello, 2010). Furthermore, †Condorlepis groeberi and †Coccolepis australis are members of the same chondrostean family Coccolepididae, and a thorough revision of the latter species might suggest that it is closely related to the Almada coccolepid. These systematic affinities suggest close biogeographic relationships between the Argentinean and the Australian localities. Whether this similarity indicates the presence of a distinctive Middle-Late Jurassic southern Gondwanan (Patagonia-Antarctica[?]-Australia) fish fauna (maybe determined by latitudinal setting) or might simply have palaeoenvironmental reasons can only be tested by the discovery of new freshwater fish faunas from that age.
The authors are deeply grateful to E. Ruigómez for his permanent assistant including the best mate of Trelew. Thanks are extended to A. Báez, S. M. Alvarez and A. Kramarz for assistance during work at the MACN. Special thanks are due to E. Hilton and S. tamberg for their valuable suggestions and criticisms on an early version of the article. The research has been financed by the German Research Foundation (http://www.dfg.de/) through the projects DFG Ra 1012/9-1 to O. Rauhut and DFG LO1405/3-1 to A. López-Arbarello. E. Sferco has been financed by the Consejo Nacional de Investigaciones Científicas y Técnicas, Argentina, and the German Academic Exchange Service (DAAD), Germany.
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