The Upper Jurassic (late Oxfordian to early Tithonian) Morrison Formation is famous for its abundant dinosaur material, particularly sauropods (e.g., Camarasaurus, Diplodocus, Apatosaurus, and Brachiosaurus; McIntosh, 1990a; McIntosh, 1990b; Foster, 2003; Chure et al., 2006; Whitlock, 2011; Woodruff & Foster, 2017; Tschopp & Mateus, 2017). Occurrences of these sauropods are recorded throughout the Morrison Formation, which outcrops in eight states, but it remains unclear if the more than 20 known species co-occurred in the same place or if they were segregated geographically. This is particularly true for species that are rarely found, such as Dyslocosaurus polyonychius (McIntosh, Coombs & Russell, 1992), Dystrophaeus viaemalae (Cope, 1877; McIntosh, 1997), Suuwassea emilieae (Harris & Dodson, 2004), Kaatedocus siberi (Tschopp & Mateus, 2013), and Brachiosaurus altithorax (Riggs, 1903; Riggs, 1904; Bonnan & Wedel, 2004).
The northern exposures of the Morrison Formation are little-known compared to the ones farther south. In order to test for geographical segregation among sauropods, it is therefore crucial to assess the taxonomy of any specimen found in the north in as much detail as possible, no matter how incomplete the specimens are. Herein, we describe a partial, potentially brachiosaurid pes from the Black Hills in Wyoming. Pedal elements can be diagnostic at least at family level, sometimes even below that (McIntosh, Coombs & Russell, 1992; D’Emic, 2012; Mannion et al., 2013; Tschopp et al., 2015). Though found together with Camarasaurus, there are morphological differences that show the new foot to be dissimilar to both Camarasaurus specimens from this quarry. Brachiosaurid material from this site has been reported in the past (Foster, 2003; Bader, Hasiotis & Martin, 2009), but without a detailed systematic assessment or description. Given that these would be the northern-most occurrences of brachiosaurids in the Morrison Formation, the herein described pes adds important data to our understanding of geographical patterning of the Morrison Formation fauna.
Materials and Methods
Material and association
The pes described herein consists of an astragalus (KUVP 142200), metatarsals I to V, four non-ungual pedal phalanges, one ungual (KUVP 129724), an additional non-ungual phalanx (KUVP 133862), and a second ungual (KUVP 144767). It was found at the Bobcat Pit site in Weston County in the Black Hills in north-eastern Wyoming (see Fig. 1A). It has been mentioned in Bader, Hasiotis & Martin (2009), but never described in detail.
In addition to the elements belonging to the pes described herein (KUVP 129724, 133862, 142200, 144767, Figs. 1B and 1C), Bobcat Pit has produced several specimens belonging to camarasaurid, diplodocid, and brachiosaurid sauropods (Bader, Hasiotis & Martin, 2009). During a 1998 expedition led by the University of Kansas, the sauropod pes was found underneath the tail of the Camarasaurus KUVP 129716, with the phalanges scattered around the skeleton (Fig. 1C). Metatarsals I, II, III, and IV of KUVP 129724 were closely associated, whereas metatarsal V and a pedal ungual (likely from digit III) were found nearby. Three proximal phalanges (field numbers BP013, BP194 and BP208; see Table 1) were recovered about a meter away from the metatarsals with a proximal phalanx (field number BP185) slightly further away. Phalanx KUVP 133862 was discovered during preparation of a large field jacket containing caudal elements of Camarasaurus KUVP 129716. The astragalus KUVP 142200 was collected beneath KUVP 129713. A second large claw, likely php I-2, was discovered when the site was later reopened by another excavation crew. This claw was molded and a high fidelity cast was donated to KUVP, bearing the number KUVP 144767. All elements described herein are referred to the same animal as KUVP 129724 due to their great size, relative proximity in the quarry, and lack of any duplication in the elements.
|Element||Length||Proximal width||Distal width||Field number|
|Astragalus (KUVP 142200)||246||370||–|
|php ?V-1 (KUVP 133862)||52||68||–|
Based on comparisons with articulated camarasaurid and brachiosaurid pedes, we interpret the phalanges as php I-1, II-1, III-1, and possible IV-1 and V-1, and the unguals as probably representing unguals I and III. However, given that the specimen was found disarticulated and incomplete, we refrain from reconstructing a pedal formula.
The elements of KUVP 129724, the astragalus KUVP 142200, the phalanx KUVP 133862, and the ungual KUVP 144767 were not consistent in size with the Camarasaurus specimen they were found with (KUVP 129716), nor with a second, larger Camarasaurus specimen from the same quarry. The Camarasaurus KUVP 129716 was nearly complete and included almost all the pedal material in articulation. All pedal bones from this specimen are duplicated in KUVP 129724, so it is certain the large pes does not belong to this specimen. A larger Camarasaurus (KUVP 129713) was excavated in 1997, approximately 7m adjacent in the same quarry. However, this individual is also much smaller than the new pes. Finally, all proximal phalanges display a peculiar bone texture on their proximal articular surfaces. These surfaces are marked by irregularly undulating grooves generally extending from the margins towards the center. Such a texture is likely due to remodeling in response to specific stresses in vivo, supporting the interpretation that all phalanges belong to a single pes, because all the joints between metatarsals and phalanges seem to be equally affected. As specimens at this locality generally occur as discreet skeletons rather than a mass of bonebed elements, these considerations suggest it is very likely the pes is a slightly scattered assemblage of elements from a single individual.
Excavation and preparation
The pes and astragalus were excavated from a mudstone deposit, with some encrustation of caliche on the bones, especially around the articular ends. The softer matrix was removed primarily with X-acto knives and air abrasion utilizing sodium bicarbonate abrasives. Concretionary material was removed much more slowly employing Aro and Chicago Pneumatic air scribes and air abrasion with Dolomite (and very seldom glass beads and Aluminum Oxide) abrasives. All elements were scanned using an Artec Spider handheld structured light unit and processed using Artec Studio 12 software. Individual scan files were organized and arranged in Blender software to produce figure images. The three-dimensional models are available through KUVP for research purposes.
Description and Comparison
The astragalus KUVP 142200 (Fig. 2) is slightly wider transversely than proximodistally tall and anteroposteriorly long (Table 1). It has neosauropod affinities based on the ascending process that reaches the posterior margin (Wilson & Sereno, 1998). As in most sauropods, it is wedge-shaped, with a reduced medial corner. However, it differs from diplodocids and camarasaurids by a more pentagonal instead of subtriangular outline in posterior view (Fig. 3). The extension of the medial corner is similar to the brachiosaurids Giraffatitan and Lusotitan, which have a relatively shorter and more rounded medial end than Janenschia and Camarasaurus (Fig. 3; Janensch, 1961; Mannion et al., 2013; Tschopp et al., 2015). The lateral surface of the astragalus KUVP 142200 received the fibula. It faces laterally, and has no distinct bony shelf that would have supported the fibula, unlike the condition in diplodocids (Whitlock, 2011; Tschopp, Mateus & Benson, 2015).
The pes KUVP 129724 (Fig. 2) has the typical shape of a eusauropod pes, having a spreading, asymmetrical metatarsus with an entaxonic structure, where mt I is the most robust element (Table 1; Coombs Jr, 1975; Cooper, 1984; McIntosh, 1990a; Farlow, 1992; Upchurch, 1998; Wilson & Sereno, 1998; Bonnan, 2005).
The metatarsals (Fig. 2) are generally hour-glass shaped with transversely and dorsoplantarly expanded proximal and distal articular surfaces. As is typical for eusauropods, the mt V differs from the rest in having a much more widely expanded proximal end compared to the distal one, resulting in a paddle-like shape (Bonnan, 2005). The distal articular surfaces bear distinct condyles in mt I, which gradually decrease in size and distinctiveness towards mt V with its gently rounded surface without any differentiation into separate condyles.
The metatarsals of KUVP 129724 can be distinguished from diplodocid ones by the absence of a well-developed posterolateral process on the distal articular surfaces of mt I and II, and from flagellicaudatan metatarsals more generally by the lack of distinct rugose ridges close to the dorsolateral edges (McIntosh, Coombs & Russell, 1992; Harris, 2007; Whitlock, 2011; Tschopp, Mateus & Benson, 2015).
Metatarsal I (Fig. 2) has a subrectangular to D-shaped proximal articular surface, with a concave lateral and a convex medial edge. The surface is dorsoplantarly higher than transversely wide. The dorsolateral corner of the proximal articular surface bears a distinct, tapered projection, as occurs in the mt I of the early brachiosaurid Vouivria (Fig. 4; Mannion, Allain & Moine, 2017). The proximal articular surface is strongly beveled compared to the long axis of the shaft, whereas the distal articular surface is approximately perpendicular to it. The distal articular surface is usually similarly beveled as the proximal one in flagellicaudatans (Fig. 4; Janensch, 1961: Beilagen P, R; McIntosh, Coombs & Russell, 1992: Fig. 3; Harris, 2007: Fig. 8; Tschopp & Mateus, 2017: Fig. 75).
Metatarsal II (Fig. 2) is slightly longer than mt I (Table 1). It has a subtrapezoid proximal articular surface with an expanded dorsolateral corner. Both the medial and the lateral edges are dorsoplantarly straight in proximal view (Fig. 5A). As such, it differs from many diplodocids, in which medial and lateral edges are concave (Tschopp, Mateus & Benson, 2015; Tschopp & Mateus, 2017), as well as from the rather subquadrangular shape of the proximal articular surface of mt II in Camarasaurus (Fig. 5A; Tschopp et al., 2015). It most resembles the proximal outline of mt II of Giraffatitan brancai (Fig. 5A), although these also have slightly concave medial and lateral edges (Janensch, 1961; MB.R.2268, E Tschopp, pers. obs., 2014). The shaft of mt II of KUVP 129724 is stout, but less so than in mt I.
Metatarsal III (Fig. 2) is the most slender and longest of the five elements (Table 1). The proximal articular surface was damaged during excavation. What remains of the proximal articular surface indicates that the surface had a rhomboid to slightly sheared subrectangular outline, probably similar to Ligabuesaurus (D’Emic, Wilson & Williamson, 2011). It is dorsoplantarly higher than transversely wide. The shaft expands considerably transversely towards the proximal and distal ends. The dorsal surface of the shaft is relatively flat and straight, whereas the plantar surface is concave in lateral view. The distal articular surface has distinct medial and lateral condyles.
Metatarsal IV (Fig. 2) is slightly more robust than mt III. It has a subtriangular proximal articular surface (Fig. 6A), which is different from the L-shaped one of Camarasaurus (Fig. 6A; Tschopp et al., 2015), and the kidney-shaped surface of the putative brachiosaurid Europasaurus (Fig. 6A; DFMMh FV886.3; E Tschopp, pers. obs., 2014). The distal articular surface is beveled medially, so that the medial side of the bone is shorter than the lateral one. Such a beveling has been identified as a synapomorphy for Brachiosauridae by D’Emic (2012) and Mannion et al. (2013).
Metatarsal V (Fig. 2) has a widely expanded proximal end, which strongly tapers into a long slender shaft, similar to the brachiosaurids Giraffatitan brancai (Janensch, 1961) and Sonorasaurus (D’Emic, Foreman & Jud, 2016). In Janenschia and Camarasaurus, the expansion is wide too, but it extends further distally along the shaft (Fig. 7; Bonaparte, Heinrich & Wild, 2000; Tschopp et al., 2015), whereas in many diplodocids, the proximal expansion is similarly developed as in KUVP 129724 (Fig. 7; Janensch, 1961; Tschopp & Mateus, 2017). The distal articular surface of mt V of KUVP 129724 is only weakly transversely expanded compared to minimum shaft width, which is similar to Camarasaurus, but different from flagellicaudatans (Janensch, 1961; Remes, 2009; Tschopp et al., 2015; Tschopp & Mateus, 2017), see Table S1 and Fig. 7 for mt V proportions). The distal articular surface of mt V of KUVP 129724 is less expanded in relation to proximodistal length than the metatarsals V of both Camarasaurus and diplodocids, and are instead comparable to the somphospondylians Tastavinsaurus and MUCPv-1533 (Canudo, Royo-Torres & Cuenca-Bescós, 2008; González Riga, Calvo & Porfiri, 2008) and the brachiosaurids Cedarosaurus and Sonorasaurus (Fig. 7; D’Emic, 2013; D’Emic, Foreman & Jud, 2016).
The phalanges (Fig. 2) are generally wider than long (Table 1) and have distinctly expanded proximal articular surfaces and no collateral ligament pits, which is typical for eusauropods (Upchurch, 1998; Wilson & Sereno, 1998; Wilson, 2002; Upchurch, Barrett & Dodson, 2004). In php II-1, III-1, and IV-1, also the distal articular surfaces are expanded transversely.
Phalanx php I-1 (Fig. 2) is just slightly wider than dorsoplantarly high, both proximally and distally, resembling the proportions of Giraffatitan (Janensch, 1961) and diplodocids (Tschopp & Mateus, 2017), but not Camarasaurus (Tschopp et al., 2015). The proximal articular surface lacks the plantar “lip” typical for diplodocids (Upchurch, Tomida & Barrett, 2004; Whitlock, 2011; Tschopp, Mateus & Benson, 2015). The distal articular surface projects slightly dorsomedially, resulting in a distinctly concave medial edge. This corner is equally developed in Giraffatitan (Janensch, 1961) and Sonorasaurus (D’Emic, Foreman & Jud, 2016), but no projection occurs in any other sauropod taxon known to us (Fig. 8).
The putative php II-1 and III-1 of KUVP 129724 (Fig. 2) are relatively short, compared to Giraffatitan (Janensch, 1961), and more similar in proportion to Camarasaurus (Tschopp et al., 2015). However, the distal condyles of php III-1 of KUVP 129724 are less distinct in dorsal view than in Camarasaurus (Tschopp et al., 2015), and resemble more the state in Giraffatitan (Janensch, 1961).
The other two non-ungual phalanges do not provide any particular morphological information for comparative purposes. Phalanx IV-1 has a very irregular dorsal surface (Fig. 2). The smallest element (KUVP 133862) is a nubbin-like bone typical for the reduced terminal, non-ungual phalanges of digits IV and V of most neosauropods (Bonnan, 2005).
Two unguals were recovered with the pedal elements (Fig. 2). The larger of the two (KUVP 144767; interpreted to be php I-2 herein) has the typical sickle-shape of eusauropod unguals (Wilson & Sereno, 1998), whereas the smaller ungual (part of KUVP 129724; interpreted to be php III-4) is rather straight (Fig. 9). The high dorsal projection of the proximal articular surface is however also present in Giraffatitan (Janensch, 1961) and Sonorasaurus (D’Emic, Foreman & Jud, 2016). The proximal and distal outlines resemble Giraffatitan (Janensch, 1961). The scalene cross-section of the unguals differs from the isosceles shape of Camarasaurus (Fig. 9; Tschopp et al., 2015).
The morphological comparisons lead to an identification of the pes as belonging to Titanosauriformes, and more specifically Brachiosauridae, in particular due to the orientation of the distal articular surface of mt IV that was recovered as a synapomorphy for the clade in two independent phylogenetic analyses (D’Emic, 2012; Mannion et al., 2013). In addition, the elongation of mt V is most similar to titanosauriform taxa sampled herein (see Fig. 7 and Table S1); Camarasaurus has more widely expanded proximal and distal articular surfaces relative to proximodistal length, whereas diplodocids all have more widely expanded distal articular surfaces. The morphology of the phalanx php I-1, with its rounded proximal articular surface and the dorsomedial projection on the distal articular surface strongly suggest a close affinity with the brachiosaurids Giraffatitan and Sonorasaurus. Finally, the relatively straight ungual php III-3 of KUVP 129724 resembles the latter two taxa most and its scalene triangle cross section differs substantially from the isosceles triangle cross section of Camarasaurus KUVP 129716 (A Maltese, pers. obs., 2018). This shape rarely occurs outside of Brachiosauridae. The features distinguishing KUVP 129724 from Giraffatitan are most likely representing differences at a lower taxonomic level within Brachiosauridae, given that many of them are more variable among eusauropods than the traits mentioned above.
The only currently known titanosauriform taxon from the Morrison Formation is Brachiosaurus altithorax. The type locality for this species is close to the town of Grand Junction, Colorado (Riggs, 1903; Riggs, 1904; Fig. 3), and several other localities have been reported to have produced brachiosaurid material in the meantime (Jensen, 1987; Curtice, Stadtman & Curtice, 1996; Carpenter & Tidwell, 1998; Bonnan & Wedel, 2004; Taylor, 2009; Bader, Hasiotis & Martin, 2009). However, the absolute number of brachiosaurid specimens from the Morrison Formation is still low relative to other sauropods, and none of these specimens preserve any bones from the lower hindleg (Taylor, 2009), so that no overlapping material of Brachiosaurus exists with which the pes described herein could be compared. Therefore, even though attribution to Brachiosaurus seems reasonable, we cautiously refer KUVP 129724, 133862, 142200, and KUVP 144767 to Brachiosauridae indet.
|CPT; L||MNN TIG4||ZDM T5704; R||NHMUK R3078; L||ZDM T5701; L||ZDM T5402; L|
|Metatarsal I||230 (CPT-1318)||165||152||192||110|
|Metatarsal II||300 (CPT-1309)||215||204||202||150|
|Metatarsal III||300 (CPT-3967)||300||212||180|
|Metatarsal IV||280 (CPT-1268)||207|
|Metatarsal V||245 (CPT-3965)||187|
|Source||R Royo-Torres, pers. comm., 2018||Sereno et al. (1999)||He, Li & Cai (1988)||E Tschopp, pers. obs., 2011||He, Li & Cai (1988)||Zhang (1988)|
|?CM 11984; L||CM 3018; L||CM 94; L||ANS 21122; R||SMA 0011; L||AC 663; L|
|Source||McIntosh (2005)||Gilmore (1936)||Hatcher (1901); Mazzetta, Christiansen & Fariña (2004)||Harris (2007)||Tschopp & Mateus (2017)||McIntosh, Coombs & Russell (1992)|
|AMNH FARB 5761; R||GMNH-PV 101; R||YPM VP.001905; L||SMNS 12144; R||SMA 0002; R||CM 11338; L|
|Source||Osborn & Mook (1921)||McIntosh et al. (1996)||E Tschopp & O Mateus, pers. obs., 2014||Fraas (1908); J Nair, pers. comm., 2015||Tschopp et al. (2015)||Gilmore (1925)|
|KUVP 129724; L||MB.R.2181||ASDM 500; R||MNHN.F.1934.6; L||DMNS 39045;||DMNS 40932; R|
|Source||This study||Paul (1988)||D’Emic, Foreman & Jud (2016)||Mannion, Allain & Moine (2017)||A Maltese, pers. obs., 2012||A Maltese, pers. obs., 2012|
|MPM-PV 1156; R||NMMNH P-49967; R||MPZ 99/9; R||MCF-PHV-233; R||UNCUYO-LD 302; R||ZPAL MgD-I/48; R|
|Source||Lacovara et al. (2014)||D’Emic, Wilson & Williamson (2011)||Canudo, Royo-Torres & Cuenca-Bescós (2008)||Bonaparte, Riga & Apesteguía (2006)||González Riga et al. (2016)||Borsuk-Bialynicka (1977)|
The largest neosauropod pes
Although the taxonomic position of the new specimen cannot be determined for certain, it does represent a dinosaur of enormous proportions. Indeed, the metatarsals of KUVP 129724 are slightly larger than the largest ones of Giraffatitan, and they are considerably larger than those of Dreadnoughtus, which was reported to be one of the largest sauropods ever found (Table 2; Lacovara et al., 2014). The only other sauropod pes known so far that is close to these proportions is from the non-neosauropod eusauropod Turiasaurus riodevensis from the Late Jurassic of Spain (Royo-Torres, Cobos & Alcalá, 2006; R Royo-Torres, pers. commm., 2018).
Based on the hindlimb proportions of the brachiosaurid Vouivria (Mannion, Allain & Moine, 2017), we estimated a femur length of 2071 mm and a tibia length of 1,220 mm for KUVP 129724. This is slightly larger (2%) than the type specimen of Brachiosaurus altithorax (2,030 mm femur length; Riggs, 1903). Assuming that the cartilage caps on the proximal and distal articular surfaces of the longbones would increase their length by approximately 10% (Schwarz, Wings & Meyer, 2007; Bonnan et al., 2010; Holliday et al., 2010), this would result in a hip height of approximately 3.99 m. Although this appears to be the largest pes reported to date, traces and other incomplete body fossils show that the pes described herein does not represent the maximum body size of sauropod dinosaurs. Some of the largest sauropods such as Argentinosaurus or Patagotitan do not preserve pedal material but have femur lengths that considerably exceed our estimate for KUVP 129724 (Argentinosaurus: 2,557 mm, estimated based on incomplete femur; Patagotitan: 2,360 mm; Mazzetta, Christiansen & Fariña, 2004; Carballido et al., 2017). The largest sauropod tracks from the Broome Sandstone of Australia are >1,100 mm in diameter, indicating a similar hip height as calculated for KUVP 129724 herein (>3.41 m; Salisbury et al., 2016). However, all these finds are from the Cretaceous, so that the type specimen of Brachiosaurus altithorax and the pedal elements described herein still represent the largest individual specimens found in the Morrison Formation, only matched in size during the same period by Turiasaurus from Spain and Giraffatitan from Tanzania. Given that the type specimen of Brachiosaurus altithorax was found in western Colorado (Riggs, 1904) and the pes described herein in northeastern Wyoming, this shows that sauropods with very large body size were distributed across wide ranges in the Morrison Formation.
Brachiosaurid distribution in the Late Jurassic of North America
Our detailed description and systematic assessment of the pedal elements KUVP 129724, 133862, 142200, and 144767 confirms the presence of large-sized brachiosaurids in the Upper Jurassic Morrison Formation of the Black Hills. Together with the small-sized brachiosaur mentioned in Bader, Hasiotis & Martin (2009), this pes is the northern-most occurrence of this taxon reported so far in the Late Jurassic of North America (Fig. 10). If the material described herein belonged to the currently only known Late Jurassic North American species Brachiosaurus altithorax, this taxon would cover a range of latitudes across the Morrison Formation. Brachiosaurids, like camarasaurids, were sauropods with broad-crowned teeth, which could process relatively tougher vegetation than the peg-like diplodocoid teeth (Janensch, 1935; Calvo, 1994; Wiersma & Sander, 2017). It would, therefore, seem reasonable to assume they could cover a wide range of vegetational zones. Camarasaurids are also known to (seasonally) migrate (Fricke, Hencecroth & Hoerner, 2011), and Camarasaurus specimens have been found from New Mexico to Montana (Ikejiri, 2005; Woodruff & Foster, 2017). Given the similarities in tooth crown morphology in the two genera, brachiosaurs could have displayed similar geographical spreading and/or migrational habits as camarasaurids. However, additional information will be needed to assess species diversity within brachiosaurids of the Morrison Formation, and to understand in more detail how their distribution, the climate, and vegetation changed throughout the time of deposition of the formation. This is outside of the scope of the current study.
We present the first brachiosaurid pedal elements from the Late Jurassic of North America. The pes represents the largest sauropod pes described to date. Size estimations scaled due to lack of anatomical overlap indicate that these pedal elements belonged to a brachiosaur slightly larger than the holotype of Brachiosaurus altithorax. Moreover, this pes and a small specimen of a brachiosaur from the same quarry represent the northernmost occurrences of the taxon in the Morrison Formation.
List of Institutional Abbreviations
Beneski Museum of Natural History of the Amherst College, Amherst, Massachusetts, USA
American Museum of Natural History, New York City, New York, USA
Academy of Natural Sciences, Philadelphia, Pennsylvania, USA
Arizona-Sonora Desert Museum, Tucson, Arizona, USA
Carnegie Museum of Natural History, Pittsburgh, Pennsylvania, USA
Cincinnati Museum of Natural History and Science, Cincinnati, OH
Museo de la Fundación Conjunto Paleontológico de Teruel-Dinópolis, Aragón, Spain
Dinosaurier-Freilichtmuseum, Münchehagen, Germany
Denver Museum of Nature and Science, Denver, Colorado, USA (previously DMNH)
Field Museum of Natural History, Chicago, Illinois, USA
Gunma Museum of Natural History, Gunma, Japan
Instituto Argentino de Nivologia Glaciologia y Ciencias Ambientales, Mendoza, Argentina
Kansas University Museum of Natural History, Vertebrate Paleontology, Lawrence, Kansas, USA
Malawi Department of Antiquities Collection, Lilongwe and Nguludi, Malawi
Museum für Naturkunde Berlin, Berlin, Germany
Museo ‘Carmen Funes’, Plaza Huincul, Neuquén, Argentina
Muséum National d’Histoire Naturelle, Paris, France
Musee National du Niger, Niamey, Republic of Niger
Colección de Paleovertebrados de la Museum Provincial de Cipolletti ‘Carlos Ameghino’, Cipolletti, Rio Negro Province, Argentina
Museo Padre Molina, Rio Gallegos, Santa Cruz, Argentina
Museo Paleontológico de Zaragoza, Zaragoza, Spain
Museo de Geología y Paleontología Universidad Nacional de Comahue, Argentina
Natural History Museum, London, United Kingdom
New Mexico Museum of Natural History and Science, Albuquerque, New Mexico, USA
National Science Museum, Tokyo, Japan
Sauriermuseum Aathal, Switzerland
Staatliches Museum für Naturkunde, Stuttgart, Germany
Universidad Nacional de Cuyo, Laboratorio de Dinosaurios, Mendoza, Argentina
Universidad Nacional de la Patagonia San Juan Bosco, Comodoro Rivadavia, Argentina
Yale Peabody Museum of Natural History, New Haven, Connecticut, USA
Zigong Dinosaur Museum, Zigong, China
Institute of Paleobiology, Polish Academy of Sciences, Warsaw, Poland