Ariid sea catfishes from the coeval Pirabas (Northeastern Brazil), Cantaure, Castillo (Northwestern Venezuela), and Castilletes (North Colombia) formations (early Miocene), with description of three new species
Ariidae catfish are described from the early Miocene Pirabas Formation in northeastern Brazil, Cantaure and Castillo formations in northwestern Venezuela, and Castilletes Formation in North Colombia. A skull from the Pirabas Formation is described as Cathoropsgoeldii, n. sp. and an otolith is identified as Cathorops sp. The otoliths from Cantaure, Castillo and Castilletes formations are described as Cantarius nolfi n. sp. and Bagreprotocaribbeanus n. sp. These coeval lithostratigraphic units reflect the Proto-Caribbean conditions and the shallow water tropical palaeoenvironment during the Miocene, particularly associated with marine coastal lagoon and estuarine influence.
Ariidae (sea catfish) comprises 30 living genera and 138 species (Eschmeyer 2013; Betancur-R. et al. 2007; Marceniuk and Menezes 2007), including 16 fossil species described from Africa (six), the Americas (three), Asia (one), and Europe (six) ranging in age from the upper Cretacous to the Pliocene (Frizzell 1965; Huddleston and Savoie 1983; Ferraris 2007). This high diversity seems to be the product of a rapid evolution and high diversification. The taxonomy of the fossil species from the Proto-Caribbean region has been difficult and mostly remains in open nomenclature due to fragmentary or poor preservation (Nolf 1976; Nolf and Stringer 1992; Nolf and Aguilera 1998; Aguilera and Rodrigues de Aguilera 1999, 2001, 2004; Landini et al. 2002). Recently, Bogan and Agnolin (2011) and Aguilera and Marceniuk (2012) described new extinct species from South America. Ariid catfishes form a well-diagnosed monophyletic group of primarily marine fishes (Gayet and Meunier 2003; Betancur-R 2009; Marceniuk et al. 2012a, b) and numerous characters preserved in the fossil skull are useful for identification of genera and species (Arratia 2003). In addition, ariids are one of the few siluriform groups that can be recognized by isolated otoliths.
The fossils studied here were collected from the early Miocene Pirabas (Maury 1925), Cantaure (Hunter and Bartok 1974), Castillo (Wheeler 1960), and Castilletes (Renz 1960) formations. These formations belong to the palaeobiogeographic Gatunian Province (Landau et al. 2008; Aguilera et al. 2011), and the corresponding fossil records are the product of evolutionary events in the Proto-Caribbean.
The objective of this paper was to describe a fossil ariid skull from the early Miocene Pirabas Formation (Brazil) and otoliths (lapilli) from early Miocene Pirabas (Brazil), Cantaure, Castillo (Venezuela), and Castilletes (Colombia) formations.
Materials and methods
Ten otoliths (lapilli) of Bagreprotocaribbeanus n. sp. and 50 otoliths (lapilli) of Cantarius nolfi n. sp. were collected from Cantaure Formation outcrops and from subsurface locations in the San José de Cocodite section from the Cantaure Formation on the Paraguaná Peninsula (11°56′32″S, 70°01′07″W), Falcón State, Venezuela (Figs. 1b, 2b).
Eight otoliths (lapilli) of Bagreprotocaribbeanus n. sp. and nine otoliths (lapilli) of Cantarius nolfi n. sp. were collected from an outcrop in the east of the Cocinetas Basin, Alta Guajira Peninsula (11°56′44.8″N, 71°21′51.7″W), Colombia (Figs. 1d, 3b).
Otolith measurements, features and remarks
Features and remarks
Cantarius nolfi n. sp., Holotype UNEFM-PF-3223
Cantaure Fm., Artisan well (early Miocene), Venezuela.
Cantarius nolfi n. sp., Paratypes UNEFM-PF-3224-1 to 3224-6
Cantaure Fm., Artisan well (early Miocene), Venezuela.
Cantariuss nolfi n. sp., Paratypes UNEFM-PF-3225-1 to 3225-6
Cantaure Fm., outcrop (early Miocene), Venezuela.
Cantarius nolfi n. sp., Paratypes MPEG-1524-V-1 to 1524-V-6
Cantaure Fm., outcrop (early Miocene), Venezuela.
Cathorops sp. MPEG-1523-V
Pirabas Fm., outcrop (early Miocene), Brazil.
Bagreprotocaribbeanus n. sp. Holotype UNEFM-PF-3226
Cantaure Fm., outcrop (early Miocene), Venezuela.
Bagreprotocaribbeanus n. sp. Paratypes UNEFM-PF-3227-1 to 3227-9
Cantaure Fm., outcrop (early Miocene), Venezuela.
Bagreprotocaribbeanus n. sp. Paratypes MPEG-1525-V-1 to 1525-6
Cantaure Fm., outcrop (early Miocene), Venezuela.
Amphiarius rugispinis (Valenciennes) UNEFM PR-073
Antero distal margin swelled. Weak Amp pointed posterior margin. Both the distal and mesial, angulated. Sharp Add. Indistinct Mic. This lapillus can be distinguished from that of Arius grandicassis in being weak Amp, swelled anterodistal margin, and angulations on the distal and mesial margins.
Aspistor quadriscutis (Valenciennes) UNEFM PR-088
Macula-shaped. Caudal margin tapered. Add sharp. Md clear. Pseudocauda of Msd expanded. Anterodistal margin swelled.
Bagre bagre (Linnaeus) UNEFM PR-09
Clam-shaped. Umbo located on the center of the dorsal surface. Posteromesial margin deep. Amp is long. Mic is shallow. This lapillus resembles both lapilli of B. marinus and M. panamensis but, barely it is distinguishable in having a longer Amp and deep posteromesial margin.
Bagre marinus (Mitchill) UNEFM PR-086
Clam-shaped with circular margin. Amp sharply protrusion. Pe as small denticle. Antero-mesial margin having a small sharp dent.
Bagre panamensis (Gill) DU-P1018
Clam-shaped with compressed circle. Amp sharp and long. Pe as small denticle. Umbo located on the center of dorsal surface.
Genidens barbus (Lacépède) FURG-uncathalog
Macula-shaped. Straight anterior margin. Angulated caudal margin. Small Amp rounded. Umbo located on the anterior part of the dorsal surface.
Genidens planifrons (Higuchi, Reis & Araújo) FURG-uncathalog
Macula-shaped. Straight anterior margin. Pseudocauda of Msd expanded. Sharp Mic. Weak Md. Protruded Amp. Umbo located on the center of the dorsal surface. This lapillus can be distinguished from that of G. barbus in having longer Amp and sharp Mic.
Cathorops wayuu Marceniuk et al. UNEFM PR-10
Macula-shaped, rather rectangular. Anterior margin incurves. Dorsal surface is smoothly convex, while ventral surface is concave. Deep Add continuing to anterior margin. In ariids species of South America, this lapillus shows specific form exceedingly.
Notarius grandicassis (Valenciennes) UNEFM PR-089
Macula-shaped. Swelled. Small Amp. Pointed posterior margin. The distal margin rounded, while the mesial margin angulated. Deep Add. Pseudocauda of Msd expanded.
Notarius kessleri (Steindachner) UNEFM PR-081
Macula-shaped. This lapillus resembles that of Arius quadriscutis (Valenciennes). Anterior margin is incurved.
Notarius planiceps (Steindachner) UNEFM PR-08
Macula-shaped. This lapillus resembles that of Arius grandicassis Valenciennes. Swelled anterodistal margin.
Sciades dowii (Gill) UNEFM PR-079
Clam-shaped. Long Amp. Posteromesial margin is expanded to oblique back. Large Amp. Posterior end is sharp. This lapillus resembles that of S. guatemalensis (Günter).
Sciades felis (Linnaeus) UNEFM PR-013
Umbo located on the anterior part of the dorsal surface. Pseudocauda of Msd expanded sharply. Mic moderately entered.
Sciades guatemalensis (Günther) UNEFM PR-090
Clam-shaped. Tapered anterior part. Umbo located on the center of the dorsal surface.
Sciades herzbergii (Bloch) UNEFM PR-054
Clam-shaped. Protruded Amp. Deep postero-mesial margin. Distal margin circular smoothly. Mic moderately deep. Umbo located on the center of the dorsal surface.
Sciades parkeri (Traill) UNEFM PR-070
Clam-shaped with high distal margin. Large Amp. Mic sharply deep entered. Posteromesial margin extended like a lobe. Umbo located on the center of the dorsal surface.
Sciades passany (Valenciennes) UNEFM PR-071
Round-shaped. Protruded Amp. Weak Mic.
Sciades proops (Valenciennes) UNEFM PR-085
Clam-shaped. Umbo located on the anterior part of the dorsal surface. Mic weak. This lapillus resembles well that of Selenaspis herzbergii, but its Msd is different in having a weak Mic.
Sciades seemani (Günther) DU-F1017
Clam-shaped. Umbo located on the center of dorsal surface. Mic indistinct. This lapillus resembles well that of Selenaspis herzbergii.
Pirabas Formation (Brazil)
The Pirabas Formation (Maury 1925), early Miocene, extends along the Pará, Maranhão, and Piauí States of northern Brazil, and consists of carbonate rocks of an offshore platform environment (grainstone and consolidated packstone, stratified wackestone packstone and laminated mudstone). In addition, littoral facies (shoreface/foreshore), marginal lagoons, restricted platform environments (gray to olive mudstone and conglomeratic sandstone), and mangrove estuarine lagoons (dark mudstone, massif or laminated) have been recorded (Góes et al. 1990; Rossetti 2001; Rossetti and Góes 2004; Costa 2011). The formation is rich in fossils and was studied for the first time by Ferreira-Penna (1876). The planktonic foraminifera association from the Pirabas Formation (Petri 1957; Fernandes 1984, 1988; Ferreira et al. 1978; Fernandes and Távora 1990; Távora and Fernandes 1999) correlates with the early Miocene N4–N5 global biozones (Blow 1969). The early contributions of White (1887) and Maury (1925) are the basal references in respect to mollusk, bryozoan, and coral research, followed by the contributions of Petri (1954, 1957) on foraminifera, Beurlen (1958a, b) on crustaceans, Santos (1958, 1967) on echinoids, Santos and Travassos (1960) on fishes, and Paula-Couto (1967) on sirenians. Many other references, summarized in Rossetti and Góes (2004) and Távora et al. (2010) provide additional descriptions, records, and/or reviews of different fossil taxa. The Atalaia shale and mudstone section (Fig. 2a) from where the fossils were obtained represents the upper-most segment of this formation, just below the early to middle Miocene Barreira Formation. The palaeoenvironment along the Atalaia section is interpreted as a transition tidal platform, with infaunal and epifaunal invertebrate richness associated with high algal and seagrass productivity (photic zone) on the biocalcirudite deposit, where the mollusk assemblage was fossilized in “live” position. Biocalcilutite, also rich in fossils, overlays the biocalcirudite rock and represents a sublittoral palaeoenvironment that was exposed to waves and tidal influence. Then, gray laminated mudstones occur abruptly over the biocalcilutite, where the tidal platform is in this section replaced by very shallow coastal lagoon sediments associated with a rapid burial rate of siliciclastic deposits from the continental drainage. Marly overlayer the mudstone and the palaeoenvironment can be interpreted as brackish. The green laminated mudstone with thalassinoid bioturbations and leaves indicate an inter-tidal palaeoenvironment, and the black mudstone with leaves and trunks represents a marginal lagoon with mangrove vegetation. The top of the section consists of biocalcirudite rocks deposited in a tidal platform (photic zone), with abundant broken shells and echinoids as a consequence of the marine tropical storm effects in the shallow sublittoral.
Cantaure Formation (Venezuela)
The Cantaure Formation (Hunter and Bartok 1974), early Miocene, can be found approximately 10 km west of Pueblo Nuevo Town on the Paraguaná Peninsula, Falcón State, Venezuela. Outcrops of the formation are exposed west of Casa Cantaure and consist of silty shales interbedded with thin algal limestones and shell beds (Hunter and Bartok 1974). There is an unexposed unit of Cantaure Formation that is 48 m thick and can be accessed by a local artisan well (Fig. 2b). The section consists mainly of silty to medium sandstone, intercalated with massive mudstone. The formation has been assigned to the late early Miocene Burdigalian based on planktonic foraminifera and calcareous nannofossil biostratigraphy (Díaz de Gamero 1974; Rey 1996). A diverse fossil fauna, particularly rich in mollusks, decapods, and fishes, has been identified along the Cantaure section (Jung 1965; Thomas and MacDonald 1970; Nolf and Aguilera 1998; Aguilera 2010; Aguilera and Lundberg 2010; Aguilera et al. 2010). These fossils are indicative of a tropical-marine, clear shallow-water coastal environment of normal salinity (Jung 1965; Díaz de Gamero 1974; Nolf and Aguilera 1998; Aguilera and Rodrigues de Aguilera 2001).
Castillo Formation (Venezuela)
The Castillo Formation (Wheeler 1960, 1963) dates as late Oligocene to early Miocene (Lorente 1997) and is situated in the western Falcón Basin, northwestern Lara State, Venezuela. The outcrop of the formation from where the fossils were obtained is exposed at Cerro La Cruz near La Mesa Town, on the southern flank of the Serranía La Baragua, and consists of marls, sandstones, and claystones (Fig. 3a). Wheeler (1960) suggested an early Miocene age for the exposures of the Castillo Formation in the area studied in this paper. The palaeoenvironment is interpreted as near-shore marine and includes diverse assemblages of mollusks, crustaceans, fishes, turtles, crocodiles, and terrestrial, aquatic and marine mammals (Sánchez-Villagra et al. 2000; Sánchez-Villagra and Clack 2004; Johnson et al. 2009).
Castilletes Formation (Colombia)
The Castilletes Formation (Renz 1960; Rollins 1965) outcrops in the Alta Guajira Peninsula (Irving 1972), northern Colombia. Its deposits are characterized by marly limestones, clays, calcareous and non-calcareous sandstones, and conglomerates. Toward the base of the formation, the limestones are coarsely textured, marly, argillaceous, sandy fossiliferous, and fairly indurated (Fig. 3b). The clays are silty, brown to buff, gray, greenish gray, and reddish, with some sandy intercalations (Rollins 1965). Toward the top, sandstones and conglomeratic sandstones are more common, often poorly sorted, and matrix-supported in channel lenses. The unit rests conformably on the Jimol Formation while the upper contact is not exposed. The Castilletes Formation is ~340 m thick in the study area. The unit was deposited in a very shallow marine environment (Rollins 1965) intermixed with continental facies produced by progradation of a fan delta. The Castilletes Formation is rich both in marine and terrestrial fossils including plants, mammals, crocodiles, turtles, bivalves, gastropods, crabs, and fishes. The otoliths were found near the base of the Castilletes Formation (stratigraphic meter 40) in marly limestone beds. Dating of Castilletes Formation is still controversial. Renz (1960) suggests an early Miocene age for the basal sediments based on Miogypsinaantillea (Cushman), Bürgl (1960) estimated middle Miocene age at the unit base and Rollins (1965) proposes a Miocene to early Pliocene age. Based on fish otolith occurrence and the close relationship between teleostean assemblage faunas with Cantaure and Castillo formations we suggest an early Miocene age in agreement with Renz (1960).
Institutional and collection abbreviations DU: Duke University, USA; FURG: Universidade Federal de Rio Grande, Brazil; INVEMAR: Instituto de Investigaciones Marinas de Punta de Betín, Colombia; MPEG: Museu Paraense Emilio Goeldi, Brazil; OPC: Otolith collection-Fumio Ohe, Japan; STRI: Smithsonian Tropical Research Institute, Panamá; UNEFM PR: Universidad Nacional Experimental Francisco de Miranda, Venezuela; USNM: National Museum of Natural History, Smithsonian Institution, USA.
Comparative material examined Amphiarius rugispinis (Valenciennes), UNEFM PR-04, UNEFM PR-073, Orinoco Delta, Atlantic; Aspistor quadriscutis (Valenciennes), UNEFM PR-012, UNEFM PR-019, UNEFM PR-068, Orinoco Delta, Atlantic; Bagre bagre (Linnaeus), UNEFM PR-09, Venezuelan Gulf, Caribbean; B. marinus (Mitchill), UNEFM PR-011, Gulf of Venezuela, Caribbean; B. panamensis (Gill), STRI-184.108.40.206, DU-P1018, Panamá Bay, Pacific; B. pinnimaculatus (Steindachner), STRI-220.127.116.11, Panamá Bay, Pacific; Cathorops agassizii (Eigenmann and Eigenmann), MPEG-1256, off coast of Pará, Brazil; C. aguadulce (Meek), UNEFM PR-020, Términos Lagoon, Mexican rivers; C. arenatus (Valenciennes), MPEG-4665, off the coasts of Pará state, Brazil; C. dasycephalus (Günther), STRI 18.104.22.168, Panamá Bay, Pacific; C. hypophthalmus (Steindachner), STRI-22.214.171.124, Panamá Bay, Pacific; C. spixii (Spix and Agassiz), MPEG-3415, off the coasts of Pará state, Brazil; C.wayuu, (Betancur-R., Acero and Marceniuk), UNEFM PR-010, UNEFM PR-020, Orinoco Delta, Atlantic; Galeichthys afer (Castelnau), OPC0220305-2, Fish River, South Africa; G. feliceps Valenciennes, OPC020305-3, Fish River, South Africa; Genidens barbus (Lacépède), FURG-uncatalog, off the coasts of Rio Grande, Brazil, Atlantic; G. genidens (Cuvier), FURG- uncatalog, off the coasts of Rio Grande, Brazil, Atlantic; G. planifrons (Higuchi, Reis and Araújo), FURG- uncatalog, off the coasts of Rio Grande, Brazil, Atlantic; Notarius cookei (Acero and Betancur-R.), STRI-126.96.36.199, Panamá Bay, Pacific; N. grandicassis (Valenciennes), UNEFM PR-012, Gulf of Venezuela, Caribbean; N. kessleri (Steindachner), STRI-188.8.131.52, UNEFM PR-081, Panamá Bay, Pacific; N. lentiginosus (Eigenmann and Eigenmann), STRI-184.108.40.206, Panamá Bay, Pacific; N. osculus (Jordan and Gilbert), STRI-220.127.116.11, Panamá Bay, Pacific; N. planiceps (Steindachner), STRI-18.104.22.168, UNEFM PR-08, Panamá Bay, Pacific; N. troschelli (Gill), STRI-ST, Panamá Bay, Pacific; Occidentarius platypogon (Günther), STRI-22.214.171.124, Panamá Bay, Pacific; Sciades couma (Valenciennes), UNEFM PR-018, Orinoco Delta, Atlantic; S. dowii (Gill), STRI-5.2.7, UNEFM PR-079, Panamá Bay, Pacific; S. felis (Linnaeus), UNEFM PR-013, Términos Lagoon, México; S. guatemalensis (Günther), STRI-126.96.36.199, Panamá Bay, Pacific; S. herzbergii (Bloch), UNEFM PR-017, Orinoco Delta, Atlantic, UNEFM PR-054, Gulf of Venezuela, Caribbean; S. parkeri (Traill), UNEFM PR-070, Orinoco Delta, Atlantic; S. passany (Valenciennes), UNEFM PR-015, UNEFM PR-071, Orinoco Delta, Atlantic; S. proops (Valenciennes), UNEFM PR-014, Orinoco Delta, Atlantic; S. seemani (Günther), STRI-188.8.131.52, DU-1017, Panamá Bay, Pacific.
Siluriformes sensu Berg 1940
Ariidae Bleeker 1862
Cathorops Jordan and Gilbert 1882
Cathorops goeldii new species
Skull with associated pectoral girdle, MPEV-1526-V.
Locality and geological age
Cathorops goeldii n. sp. is only known from the early Miocene Pirabas Formation, Atalaia beach (0° 35′31.9″S, 47°19′00″W), Salinópolis Prefecture, Pará State, Brazil.
The species is named in honor of Emilio Goeldi, Swiss zoologist and early Amazonas natural science researcher after whom the Museu Paraense in Belém, Brazil, has been named.
Cathorops goeldii n. sp. can be differentiated from its extant subcongeners from Central and South Western Atlantic by the combination of the following characters: The cephalic shield is strongly granulate, parallel to the medial groove; the parieto-supraoccipital posterior process is short to medium in size, almost as narrow at its base as at its posterior portion; the medial groove is deep along the parieto-supraoccipital process reaching the level of the temporal fossa; each side of the medial groove has a pair of divergent, short and shallow lateral sulci; both transcapular processes form an arch, which is anteriorly oriented relative to the body axis; the posterior process of the cleithrum is short and acute, its tip posteriorly oriented; the cleithrum has an expanded bulbous external area around the pocket structure to receive the articular head of the pectoral spine.
Neurocranium (Figs. 4a–c, f–g, 5a–i). The bones of the cephalic shield are strongly granulated and parallel to the medial groove. The posterior cranial fontanelle is reduced to a small opening and posteriorly continued in a deep medial groove along the parieto-supraoccipital, reaching the level of the temporal fossa. Each side of the medial groove has a pair of divergent, short, and shallow lateral sulci. The frontals contact the parieto-supraoccipital posteriorly and the sphenotics postero-laterally. The sphenotic is flat with a straight lateral margin and articulates with the parieto-supraoccipital and pterotic. The extrascapular is oval to subquadrangular in shape and is located on the posterodorsal region of the neurocranium and sutured to the parieto-supraoccipital, the pterotic, and the supracleithrum. The parieto-supraoccipital is the largest bone of the skull; its posterior process is short to medium in size, almost as narrow at its base as at its posterior portion; the posterior margin contacts the nuchal plate through a concave-convex articulation. The upper branch of the supracleithrum is flat, subtriangular in shape, and articulates lateroposteriorly with the cephalic shield. The inferior limb of the relatively short and thick supracleithrum, or transcapular process, is cylindrical to columnar in shape. Both transcapular processes are oriented posteriorly and together form an arch anteriorly oriented relative to the body axis. A thin sheet of the Müllerian ramus can be observed just behind the transcapular process. The very large otic capsules are well differentiated and limited by the prootic, pterotic, and exoccipital. The basioccipital is dagger-shaped. It is posteriorly joined with the first vertebra, forming the distinct, long subvertebral process. The superficial ventral ossification of the Weberian apparatus forms a carina.
Pectoral girdle (Figs. 4a–e, g, 5j–l). The anterior dorsal process is narrow and acute, the posterior dorsal process is not preserved, and the posterior process of the cleithrum is short and acute. The scapulocoracoid forms a very broad surface with well-developed crests ending in an interdigitized projection sutured with the opposite pectoral girdle. The cleithrum has an expanded bulbous external area around the pocket structure to receive the articular head of pectoral spine. Both scapulocoracoids form an arch, which is anteriorly oriented relative to the body axis. The cleithrum surface is coarsely ornamented with reticulate ridges and subcircular pits.
Measurements The holotype, MPEG-1526-V, preserved skull length: 52.0 mm; preserved skull width: 39.0 mm.
Otolith (lapilli), MPEG-1523-V.
Locality and geological age
Early Miocene Pirabas Formation, Atalaia beach (0°35′31.9″S, 47°19′00″W), Salinópolis Prefecture, Pará State, Brazil.
The otolith is macula-shaped to almost rectangular. The anterior margin is incurved. The dorsal surface is smooth and convex, the ventral surface is concave. The anterodistal ditch is deep, continuing to the anterior margin. The pseudocauda of the mesial shallow depression is expanded posteriorly. No mesial inward curvature is developed. Ratio lapillus length/width: 1.4. Ratio lapillus length/thickness: 2.8.
Cantarius new genus
The first part of the generic name relates to the Cantaure Formation and the second part “arius” to the genus name Arius.
Cantarius nolfi n. sp.
Cantarius nolfi new species
Genidens sp. Nolf and Aguilera 1998, p. 251, pl. 4, figs. 1–4, tab. 3
Arius sp. Monsch 1998, p. 43, pl. 4, figs. 19, 20
Ariidae ind. Monsch 1998, p. 43, pl. 4, fig. 19
Aguilera 2010, p. 115
Named in honor of Dirk Nolf, Institut Royal des Sciences Naturelles de Belgique, for contributions to knowledge of fossil teleostean otoliths.
Otolith (lapilli), UNEFM PF-3223
Otolith (lapilli), UNEFM PF-3224-1 to UNEFM PF-3224-6, UNEFM PF-3225-1 to UNEFM PF-3225-6, MPEG-1524-V-1 to MPEG-1524-V-6.
Otolith (lapilli), UNEFM PF-3229-1 to 3229-4, from Castillo Formation, Cerro La Cruz (10°23′N, 70°03′W), Lara State, Venezuela; STRI 16555 (1) and STRI 16677 (3) from the Castilletes Formation, La Guajira Peninsula, Colombia.
Locality and geological age
Cantarius nolfi n. sp. is known from the early Miocene Cantaure Formation, San José de Cocodite (11°56′32″S, 70°01′07″ W), Paraguaná Peninsula, Falcón State, Northwestern Venezuela. Also from the early Miocene Castillo and Castilletes formations (Colombia and Venezuela, respectively), and middle Miocene Pebas Formation in Colombia and Peru (Monsch 1998).
Same as genus (monospecific genus).
The otolith is very regularly ovoid and extremely thick. The anterior margin is slightly concave. The caudal margin is rounded. The antero-mesial projection is small and rounded. The umbo is located on the anterior part of the dorsal surface. The dorsal surface is irregular and very convex. The ventral surface is convex, and both convexities result in a globular aspect of the otolith. The pseudocauda of the mesial shallow depression forms an arch and is expanded posteriorly. The mesial inward curvature forms a well-developed wedge shape oriented posteriorly. Ratio lapillus length/width: 1.1–1.5 (n: 28). Ratio lapillus length/thickness: 1.8–2.6 (n: 28).
Bagre Cloquet 1816
Bagreprotocaribbeanus new species
Arius sp. Nolf and Aguilera 1998, p. 250, pl. 3, figs. 1–5, tab. 3
Arius sp. Aguilera and Rodrigues de Aguilera 2001, p. 733, fig. 1
Otolith (lapilli), UNEFM PF-3226
Otolith (lapilli), UNEFM PF-3227-01 to UNEFM PF-3227-09, MPEG-1525-V-01 to MPEG-1525-V-06.
Locality and geological age
Early Miocene Cantaure Formation, San José de Cocodite (11°56′32″S, 70°01′07″W), Paraguaná Peninsula, Falcón State, Northwestern Venezuela.
Otolith (lapilli), UNEFM PF-3228-1 to 3228-5, from the Castillo Formation, Cerro La Cruz (10°23′N, 70°03′W), Lara State, Venezuela, and STRI 16519 (1), 16555 (1), 16677 (1), 16710 (1), from the Castilletes Formation, La Guajira Peninsula, Colombia.
The species name refers to the Miocene Proto-Caribbean bioprovince.
Bagreprotocaribbeanus n. sp. is distinguished from the extant Bagre species by the long, narrow expansion of the mesial inward curvature and deep mesial notch (vs. reduced in B. bagre, B. marinus and B. panamensis). The otolith is circular (vs. slightly ovoid in B. bagre and B. panamensis).
The broad otolith is clam-shaped with a circular outline, and the anteromesial projection is sharp. The umbo is located on the anterior part of the irregular and strongly convex dorsal surface. The ventral surface is slightly convex. The pseudocauda of the mesial shallow depression forms an arch. The mesial inward curvature forms a long, narrow expansion that is oriented posteriorly. The mesial notch is deep and wide. The ratio lapillus length/width is 1.1–1.3 (number of measured specimens n: 16), and the ratio lapillus length/thickness is 1.3–2.9 (n: 16).
Palaeoenvironment, palaeoceanography and occurrences of fossil ariids
The early Miocene Proto-Caribbean fossil record is a reflection of the drastic macroevolutionary events that occurred in the Neogene as a consequence of the strong palaeoenvironmental changes in the Caribbean, which in turn were a consequence of the closure of the seaway between the Atlantic and Pacific oceans (e.g., Jackson et al. 1993; O′Dea et al. 2007; Johnson et al. 2008; Aguilera et al. 2011; Klaus et al. 2011) during the uplift of the Panamá Isthmus (Coates et al. 2005). The dynamic tectonic of the Caribbean Plate in combination with the North and South American Plates, and the Nazca and Cocos Plates (Bachmann 2001, Pindell et al. 2005) produced island formation and displacement (Greater, Lesser and Leeward Antilleans). As a consequence the littoral and sea palaeoenvironments and the palaeoceanography rapidly changed in the different sedimentary basins in the Proto-Caribbean (Iturralde-Vinet 2004–2005; Iturralde-Vinet and McPhee 1999). The passive margin of Brazil and the coastal platform (Mohriak 2003; Rossetti 2006) were mainly influenced by global eustatic sea-level changes (Carter 1998; Rossetti 2001; Kominz et al. 2008), while the equatorial Atlantic oceanic current (Johns et al. 1998, 2002), and high wave sequence, and tidal influence (Beardsley et al. 1995; Diretoria de Hidrografia e Navegação-DHN 2011) produced dynamic changes in the depositional conditions in the Proto-Caribbean region called Gatunian Province (Landau et al. 2008; Aguilera et al. 2011) during the Miocene to early Pleistocene. In addition, the Andes uplift (Gregory-Wodzicki 2000; Martinod et al. 2010) and particularly the rise of the eastern Andean Cordillera in Colombia isolated the water inflow of the northern drainage system in South America to the Caribbean through the modern Amazonian effluent, resulting in changes of the course of the Proto-Orinoco river (Díaz de Gamero 1996), the establishment of the Amazon drainage to the Atlantic coast (Hoorn et al. 1995, 2010; Figueiredo et al. 2009), and today′s northwestern South American estuarine conditions (e.g., Johnson et al. 2008; Smith et al. 2010). These factors have a strong influence on the development of the coastal marine and estuarine environments which are inhabited by catfishes and influence the biogeographic distribution of these fishes.
In tropical South America, the genus Cathorops is nowadays represented by at least 19 species (Ferraris 2007; Marceniuk and Menezes 2007; Marceniuk 2007; Marceniuk and Betancur-R. 2008; Marceniuk et al. 2012a, b). According to Marceniuk et al. (2012a, b) Cathorops spixii exhibits a wide distribution along the Brazilian coast, from the Amazon delta to Rio de Janeiro State, overlapping only with the distribution of C. agassizii (Amazon delta to near the coast of Sergipe State) and C. arenatus (near the coast of Pará and Maranhão States). The presence of a fossil Cathorops in the Pirabas Formation (Pará State, northern Brazil) and the previous fossil records from Venezuela of the time interval from late Miocene to early Pliocene (Aguilera and Rodrigues de Aguilera 2001; Aguilera 2010; Aguilera et al. 2011), and in middle Miocene strata of Trinidad (Nolf 1976; Aguilera et al. 2011) is associated with a tropical origin. Cathorops goeldii n. sp. from the Pirabas Formation (early Miocene) represents the earliest Cathorops fossil record and possibly predates the New World Cathorops diversification observed today, which is thought to have originated during the early Pliocene (Betancur-R. et al. 2012). Therefore, it is argued here that C. goeldi may be regarded as an offshoot from the main Cathorops stem lineage.
The newly described Cantaurius nolfi shows a wide geographic distribution along the northwestern coast of South America of the Proto-Caribbean region during the early Miocene. The locations and strata, from where C. nolfi was obtained, are characterized by marine shallow water palaeoenvironments. However, some strata were deposited under brackish conditions and environments with estuarine influence (Castillo and Castilletes formations). Cantaurius nolfi also was recorded (as Ariidae indeterminate, Arius sp. and Arius cf. gigas) in Colombia (Los Chorros, Mocagua, Buenos Aires), middle Pebas Formation (Monsch 1998), and in Perú (Santa Julia), Solimões/Pebas formations of northwestern Amazonia in conditions of the so-called “marine incursion” as concluded from the mixture of euryhaline and freshwater taxa (Monsch 1998; Latrubesse et al. 2010). The specimens studied by Monsch (1998) were not accessible for this review, but his illustrations and description support the diagnostic characters of Cantaurius nolfi.
The extant Central and South American ariid species along the Caribbean and the Atlantic coasts are mainly exclusive marine species. However, some species like Cathorops cf. festae (cited by Betancur-R. et al. 2012), Notarius bonillae (Miles), and N. cookie (Acero and Betancur-R.) inhabit freshwater environments and Amphiarius phrygiatus (Valenciennes), Cathorops hypophthalmus (Steindachner), C. tuyra (Meek and Hildebrand), and C. agassizii (Eigenmann and Eigenmann) euryhalyne environments. For all of them (except for A. phrygiatus that lacks sufficient detail information) an origin and diversification age of 4 m.y. was estimated (Betancur-R. et al. 2012). Therefore, the presence of Cantaurius nolfi in the Pebas Formation is interpreted as the result of early independent and unsuccessful invasions of freshwater, and does not necessarily support a marine incursion in the Amazonian region.
Fossil skulls of B. marinus Mitchill, 1815 were previously collected from the late Miocene Urumaco Formation in Venezuela in a wetland deltaic plain palaeoenvironment (Aguilera and Rodrigues de Aguilera 2001; Aguilera 2010). The genus Bagre is represented by one fossil species described here from the early Miocene (Bagreprotocaribbeanus) and four valid extant species (Ferraris 2007; Marceniuk and Menezes 2007), two of them from the Pacific coast [(B.panamensis (Gill, 1863) and B. pinnimaculatus (Steindachner, 1876)] and two from the Atlantic coast (B. marinus Mitchill, 1815 and B. bagre Linnaeus, 1766). The age of diversification of these ariids was estimated between 20 and 15 m.y. by Betancur-R. et al. (2012) and is confirmed well in agreement with the age of fossil records treated here.
This research was supported by the Museum Paraense Emilio Goeldi, the Conselho Nacional de Desenvolvimento Científico e Tecnológico (Process CNPq 311783/2011-2 to OA and CNPq 565046/2010-1 to HM-S) in Brazil, the Universidad Francisco de Miranda in Venezuela, and the Smithsonian Tropical Research Institute in Panamá. We thank Dione Rodrigues de Aguilera for preparation of the fossil and suggestions. Julio Reyes and Ana Cristina Oliveira helped us with the skeletal preparation. Vladimir Zapata, Federico Moreno and Jorge Moreno for the geological survey and for collecting the otolith during a field trip to the La Guajira Peninsula in Colombia. Marcelo Sánchez for collecting the otolith during a field trip to Cerro La Cruz in Venezuela. David Santana for the early review of the manuscript. Zoneibe Luz helped with otolith photographs. Wolmar Wosiacki helped us with skull photograph and supported us with the access to the fish collection in the MPEG. Guillermo Aguilera supported with the 3D and 2D platform, figures and plates design. Jean dos Santos-Lobato helped us with the tomography and image captions. We thank Alexander Marceniuk, Ricardo Betancur-R. and Marcelo Sánchez-Villagra for comments and suggestions. The authors would like to thank especially Werner Schwarzhans, Bettina Reichenbacher, Florian Witzmann, anonymous reviewers and editors for corrections, comments and suggestions that improved the manuscript.