- Citado por Google
- Similares en SciELO
- Similares en Google
versión impresa ISSN 0716-0208
Rev. geol. Chile v.35 n.1 Santiago ene. 2008
Revista Geológica de Chile 35 (1): 175-184. January, 2008
Theropod Dinosaur Trackways from the Lower Cretaceous of the Chacarilla Formation, Chile
Pistas de dinosaurios terópodos del Cretácico Inferior de la Formación Chacarilla, Norte de Chile
David Rubilar-Rogers1, Karen Moreno2, Nicolás Blanco3, Jorge O. Calvo4
1 Sección Paleontología, Museo Nacional de Historia Natural, Casilla 787, Santiago, Chile.
2 Instituto de Geociencias, Universidad Austral de Chile, Casilla 567, Valdivia, Chile.
Current address: School of Biological, Earth and Environmental Sciences, University of New South Wales, 2052, Sydney, Australia. dinohuella@yahoo. com
3 Servicio Nacional de Geología y Minería, Avenida Santa María 0104, Santiago, Chile.
4 Centro Paleontológico Lago Barreales, Museo de Geología y Paleontología, Universidad Nacional del Comahue, Avenida Mega-raptor 1450, Ruta Provincial 51, km 65, Costa Norte del Lago Barreales, Neuquén, Argentina. jocalvo40@digimedia. com. ar
We describe sixteen theropod dinosaur trackways from site III (Lower Cretaceous?) of the Quebrada Cha-carilla in the ChacariUa Formation (Jurassic-Lower Cretaceous), northern Chile. The trackbed belongs to a meandering river environment, with recurrent track assemblages. We find that the main direction of the ichnites from site III parallels that of water flow. Two theropod footprint morphotypes are recognized: A) digit II and IV occupying about 0.5 times the total footprint length, and B) digit II and IV occupying less than 0.35 times the total footprint length. We estimate similar speed (~7 km/h) for the two parallel theropod trackways of morphotype A, suggesting synchronized walking. We also describe some of the largest theropod footprints from South America (>60 cm), which are all of morphotype B.
Keywords: Large theropod, Behaviour, Synchronized walking, Footprints, Ichnites, Lower Cretaceous, Northern Chile.
Se describen dieciséis pistas de dinosaurios terópodos localizadas en el sitio III (Cretácico Inferior?) de la Formación ChacariUa (Jurásico-Cretácico Inferior) en Quebrada ChacariUa, norte de Chile. La unidad con huellas fue depositada en un ambiente de río meandriforme y presenta recurrentes niveles con asociaciones de trazas. Las icnitas tienen una dirección paralela a la dirección del flujo de agua. Dos morfotipos de huellas de terópodos fueron reconocidos: A) Con los dígitos II y IV, ocupando cerca de 0,5 veces el largo total de la huella y B) con los dígitos II y IV ocupando menos de 0,35 veces la longitud total de la huella. Estimaciones de similar velocidad (~7 km/h) de dos pistas paralelas pertenecientes al morfotipo A, sugieren caminata sincronizada. Además, describimos algunas de las huellas de terópodos más grandes de América del Sur (>60 cm), las que corresponden al morfotipo B.
Palabras claves: Terópodos grandes, Comportamiento, Caminata sincronizada, Huellas, Icnitas, Cretácico Inferior, Norte de Chile.
The record of Mesozoic continental vertebrates in Chile consists mainly of dinosaur tracks (Theropoda-Sauropoda-Ornithopoda), remains of titanosaurid sauropods, and pterosaur bones (Casa-miquelaandFasola, 1968;Casamiquelae?a/., 1969; Casamiquela and Chong, 1980; Chong, 1985; Bell and Suárez, 1989; Salinas et ah, 1991a; Salinas et ah, 1991b;Moreno and Pino, 2002; Rubilar-Rogers, 2003; 2006; Moreno and Benton, 2005).
Galli and Dingman (1962) mentioned the presence of diverse dinosaur footprints in different outcrops of Quebrada Chacarilla, northern Chile (Fig. 1). This was the first description of dinosaur ichnites in this country. On that occasion Joseph T. Gregory (in Galli and Dingman, 1962) identified different morphologies from pictures, including theropods, sauropods, ornithopods, and perhaps stegosaurs. These footprints are distributed in two separated tracksites, although most of the description was focused in the first locality examined.
We re-study the different outcrops of this formation, and present here the first detailed information on the vertebrate ichnofauna of the tracksite mentioned by Galli and Dingman (1962) as 'second locality' with dinosaur footprints, named 'site III' in this paper (Fig. 2). The locality shows numerous eastern-western and northern-southern striking outcrops with a pronounced west-dip (44°) and dozens of dinosaur trackways exposed in a thick sequence of sandstones. Their preservation is generally good, depending on the weathering of the different levels. A detailed track mapping of the Chacarilla Formation is far from complete, thus only preliminary results will be presented here. The present study only describes theropod trackways of an outcrop in Quebrada Chacarilla. The cast of a footprint from this site is housed in the Paleontológica! Collection of the Servicio Nacional de Geología y Minería, Chile (SNGM-311).
2.General Geologic Context
Mesozoic tectonic evolution in northern Chile was dominated by subduction along the western margin of Gondwana (Coira et al., 1982; Jordan et al, 1983; Mpodozis and Ramos, 1989; Ramos and Kay, 1991; Mpodozis and Allmendinger, 1992). During the Jurassic and Lower Cretaceous, a magmatic arc was formed along the present-day Cordillera de la Costa. East of the arc, in the Central Depression and Precordillera in Chile, there was a contemporaneous ensialic back-arc basin, the Tarapacá Basin, which comprises thicknesses of thousands of meters of marine and continental sediments (Coira et al, 1982;Groschkee?a/., 1988; Mpodozis and Ramos, 1989). During Lower and Mddle Jurassic, deposition of marine sequences was controlled by post-rift thermal subsidence and global sea-level fluctuations (Groschke et al, 1988; Ardill et al, 1998), whereas later on, in Middle Jurassic to Cretaceous times, the basin was controlled by tectonic movements related to the break-up of Pangea and fragmentation of Gondwana (Ardill et al., 1998). The latter resulted in a widespread marine regression causing deposition of continental red-beds during Upper Jurassic and Lower Cretaceous in the backarc basin (Rutland, 1971; Chong, 1977; Bogdanic, 1990). Sedimentation stages in Lower Cretaceous times corresponds to the track-bearing deposits of various carnivorous and herbivorous dinosaurs tracks (Blanco et al., 2000; Moreno et al., 2000; Rubilar et al, 2000a and b; Moreno, 2001).
3. Locality and Geologic Setting
The tracksite is located in Quebrada Chacarilla (coordinates 20°38T2.4"S, 69°4'25"W), Region I, northern Chile (Fig. 2).
The ChacarillaFormationis mainly a clastic succession with an exposed thickness of 1100 m. The lower part is of marine origin (Oxfordian), whereas the upper part was deposited in a continental setting (Galli and Dingman, 1962). The marine section at the Quebrada Chacarilla crops out in a box-fold anticline centre (Galli and Dingman, 1962), and the continental deposits form an open syncline. The top of the formation is marked by an angular unconformity, overlaid by volcanic and clastic rocks of the Cerro Empexa Formation (Upper Cretaceous-Lower Paleocene, Tomlinson et al., 2001).
A certain discrepancy in age determination has been noted for lithostratigraphically equivalent continental red-bed successions exposed along the Precordillera in Chile's Regions I and II. This variability is due to the scarcity of biostratigraph-ically significant fossils in the continental facies rocks. As a result, previous workers have reported ages varying from Oxfordian (Galli and Dingman, 1962) or Kimmeridgian (Vergara, 1978) to entirely Lower Cretaceous (Ardill et al., 1998). In addition, 60 km north of the study area, Herbst and Troncoso (1996) placed a part of this formation in the Middle Jurassic, based on a taphoflora association. However, the discovery of large ornithopod ichnites in the Chacarilla Formation indicates a Cretaceous age at least for the upper part of this formation (Blanco et al, 2000; Rubilar et al, 2000a). These tracks are correlated to the Caririchnium ichnofacies described by Lockley et al. (1994) for the Cretaceous of Laurasia, which are dominated by large ornithopod tracks preserved in silicoclastic rocks from coastal plain environments, in medium to high latitudes (Lockley et al, 1994). The studied strata are located in the uppermost part of the Chacarilla Formation, hence it is likely to be of a Lower Cretaceous age.
The measured section (Fig. 3) contains 140 m of rhythmically alternating shales and red sandstones, and is structured in multiple, superposed fining- and thinning-upward sequences of decametric to metric scale. Within this section we observed two facies associations, which represent point bars and flood-plains of a meandering river environment.
The point bar facies association consists of several superposed fining- and thinning-upward cycles, with each cycle being 30-50 cm thick and reaching an overall thickness of 4-10 m. Each cycle is composed of medium-grained quartzose sandstone with trough cross-bedding stratification, which passes gradually into sandstone with parallel plane lamination. The highest part of the cycle shows reddish mudstone with current ripple marks. Sedimentary structures such as trough cross-bedding and parting lineation indicate paleocurrents toward the NW, WNW and W (150 measurements). In sections perpendicular to the paleoflow, the sandstone shows a sigmoidal geometry that forms a large-scale cross-stratification of the epsilon type (Allen, 1963).
The floodplain facies association consists of finely laminated mudstone (generally shale). Plant remains, carbonaceous levels, and root marks are present, as well as some fossil trunks in life position. Furthermore, arboreal root casts and dinosaur footprints can be found. Intercalated in the mudstones are laterally extensive, but thin (0.1-0.3 m), tabular bodies of fine-grained lenticular sandstones, with a planar to slightly concave base, ripple marks, and parallel plane-lamination. These sandstones probably correspond to the distal deposits of crevasse splays covering fioodplain areas (Miall, 1996). Asymmetric ripples in this association indicate a paleoflow toward WSW (50 measurements). The orientations of ornithopod and theropod dinosaur trackways are toward WSW and SW, approximately parallel to the water flow direction.
4. Description of the dinosaur ichnites
Here we describe sixteen trackways (3-6, 8, 10, 12-13, 15-18, 22, 24-26) from Quebrada Cha-carilla site III (Fig. 2), which correspond to the theropod morphology. Measurements were taken in situ (Fig. 4, Table 1). Footprint dimensions clearly show s a tendency toward a longer than wide footprint shape (Fig. 5). This characteristic, together with the anatomical features described below support the assignation of these ichnites to the The-ropoda Suborder. Most of these footprints exhibit a tridactyl morphology, with impressions of digits 11,III and IV. However, trackway 26 also displays the impression of digit I (tetradactyl morphology), which corresponds to a deeper impression of the autopod into the substrate and subsequent collapse of the sedimentary structure (Fig. 6). Despite of this, two main pedal morphotypes are recognized, A and B, based on digital proportions:
In morphotype A, the length of digits II and IV is about half the total footprint length. This morphology is observed in trackways 3,4 and 18 (plastotype SNGM-311, Servicio Nacional de Geología y Minería). Trackways 3 and4 show surprising similarities. Footprints have comparable shape and size. Also, these two trackways are parallel (separated by about 80 cm), and have approximately the same length (6 m) and same number of footprints (8 each). Later on, trackways 1,2 and 5 crossed trackways 3 and 4 (Fig. 7). In morphotype B (trackways 5, 6, 8, 10, 12,13, 15,16,22,24,25 and 26), the length of digits II and IV are proportionally smaller than in morphotype A, and are about a third of the total footprint length. Morphotype B displays a wide variety of footprint dimensions, from 28 cm long and 15 cm wide to 65 cm long and 53 cm wide (Figs. 7-11), including some of the largest in South America (see discussion). Also, the tetradactyl footprints (trackway 26) mentioned above are included in this morphotype. These footprints show deep impressions of digits I to IV plus a metatarsal impression. The impression of digit I is directed anteromedially (Fig. 6). The total anteroposterior length (1 m) of this footprint was taken without accounting for the metatarsal impression, which is approximately one third of the total length (Table 1).
There are two dinosaur groups with tridactyl footprints: theropods and ornithopods. Diagnostic features which permit the discrimination between both groups are the marked differences of footprint length/ width ratio, the lower interdigital angles and lower trackway pace angulations, and the presence of an indentation along the medial edge of digit two just distal to the 'heel' apex seen in theropods as opposite to ornithopods (Fig. 4). However, these characters do not allow the identification of a specific trackmaker, due to the weak correlation between footprint morphology and skeletal features (Farlow and Chapman, 1997).
The ichnofauna identified in site III of Quebrada Chacarilla is composed of about 80% theropods and 20% ornithopod footprints. Therefore, it is distinct from other Late Jurassic-Early Cretaceous tracksites, such as San Salvador and Baños del Flaco, which present a mostly small theropod and a small ornithopod-small theropod-narrow gauge sauropod ichnocoenosis respectively (Moreno and Pino, 2002; Moreno et ah, 2004; Moreno and Benton, 2005). This variation is difficult to interpret since many factors are involved in the preservation of the various tracksites, being dinosaur behaviour, distribution, palaeogeography and chronological differences among the most important. In this respect, much more work is needed in order to identify possible ichnofacies and chronological accuracy.
The general orientation of the trackways in site III is similar to the direction of water flow (NE-SW).
Based on the proportions of the digital impressions, two morphotypes have been recognized: Morphotype A, with a prominent digit III (lateral digits II and IV about a half of digit III length), which is comparable to tracks attributed to 'coelu-rosaurs' in South America (Leonardi, 1989; Calvo, 1991; Leonardi and Spezzamonte, 1994). Within this morphotype we observed two trackways (3 and 4) that are walking parallely at a similar speed (~7 km/h), and have a regular separation between both trackways, suggesting that both individuals were walking in a synchronized manner (Fig. 7).
Morphotype B, with lateral digits (II and IV) about a third of digit III, is similar to the ichnogenus Abelichnus (Calvo, 1991, 1999; see Figs. 10-11), where claw impressions are very prominent and the digit impressions occupy most of the length of the tracks, and may be tentatively referred to that ichnotaxon. However, the pace angulation recorded is 180° in contrast to ~150° for Abelichnus.
Morphotype B includes one of the largest theropod ichnites known in South America. These ichnites are comparable in size (mean hip height ~3 m) with carcharodontosaurids such as Gigano-tosaurus, as was previously referred (Calvo and Mazzetta, 2004) from the early Late Cretaceous of Argentina (Coria and Salgado, 1995; Calvo and Coria, 1998; Novas et ah, 2005). However, theropod remains of this size have not yet been found on the western portion of Gondwana. Consequently, the Chacarilla footprints represent the first evidence of their existence in that area. In addition, a trackway of seven tetradactyl footprints (trackway 26) with metatarsal impression is included in this morphotype. The particular morphology of these footprints suggests a quasi-plantigrade locomotion (Kuban, 1989) and presents independent evidence that these theropods powered the early stance phase by femoral retraction, rather than by knee flexion as in living birds(Gatesye?a/., 1999). Subtracting the posterior footprint elongation from the total footprint length (1 m), we obtain similar dimensions (60 cm long, 53 cm wide) as those as in other trackways of morphotype B (Fig. 6).
The average speed estimated for all the trackways is 5.8 km/h, which is consistent with a walking gait. The only trackway that has a trotting gait is 17, with an estimated speed of 11.2 km/h.
The ichnofossils from the Chacarilla Formation as a whole, but particularly in site III, are a unique record of dinosaurian fauna which inhabited a flood plain environment of a meandering river in the north of Chile during the Early Cretaceous (as indicated by the presence of large ornithopod footprints cha-racteristical of this period). Here, described some of ichnites from site III, which show a main direction NE-SW, and therefore are parallel to the direction of the water flow. Two theropod morphotypes were recognized, including some of the largest of South America, which indicate that large theropods lived on the western portion of Gondwana in earlier times than the suggested by the oldest carcharodonto-saurid record (early Late Cretaceous). In addition, among these large theropods traces we found two parallel trackways with similar speed and footprint morphology, which are evidence of synchronized walking, a behaviour previously not described for these big animals.
The quality, abundance and time span of the footprint record of the Chacarilla Formation makes it potentially useful for the study of paleogeogra-phic, behavioural and evolutionary patterns during the Late Jurassic and Early Cretaceous. This should be addressed in future research.
Field work was supported by Servicio Nacional de Geología y Minería, Chile (SERNAGEOMIN), as part of the project 'Geología de la franja Chuquicamata-Quebra-da Blanca'. We thank A. 'Tuco' Díaz (SERNAGEOMIN) for his help in the field. Z. Gasparini (Universidad de la Plata), A. Tomlinson (SERNAGEOMIN), J. Hutchinson (University of California), R. Charrier (Universidad de Chile), L. Salgado (Universidad Nacional de Comahue) and M. Suárez (SERNAGEOMIN) for their reviews of the manuscript.
Allen, J.RL. 1963. Studies in fluviatile sedimentation: a comparison of fining-upward cyclothems, with special reference to coarse-member composition and interpretation. Journal of Sedimentary Petrology 40: 298-323. [ Links ]
Ardill, J; Hint, S.; Chong, G; Wilke, H. 1998. Sequence stratigraphy of the Mesozoic Domeyko Basin, northern Chile. Journal of the Geological Society 155 (1): 71-88. [ Links ]
Bell, CM.; Suárez, M. 1989. Vertebrate fossils and trace fossils in Upper Jurassic-Lower Cretaceous red beds in the Atacama Region, Chile. Journal of South America Earth Sciences 2: 351-357. [ Links ]
Blanco, N.; Tomlinson, A.J.; Moreno, K.; Rubilar, D. 2000. Importancia estratigráfica de las icnitas de dinosaurios en la Formación Chacarilla (Jurásico-Cretácico Inferior), Región de Tarapacá, Chile. In Congreso Geológico Chileno, No. 9,Actas 1:441-445. Puerto Varas, Chile. [ Links ]
Bogdanic,T 1990. Kontinentale sedimentation derKreide und des Alttertiars in Umfeld des subduktionsbedingten magmatismus in der chilenischen Prakordillere (21o-23°S). Berliner GeowissenschaftlicheAbhandlungen 123: 117. [ Links ]
Calvo, J.O. 1991. Huellas de dinosaurios de la Formación Río Limay (Albiano-Cenomaniano), Picún Leufú, Provincia del Neuquén, República Argentina (Ornithischia-Saurischia: Sauropoda-Theropoda). Ameghiniana 28: 241-258. [ Links ]
Calvo, J.O. 1999. Dinosaurs and other vertebrates of the Ezequiel Ramos Mexía área, Neuquén-Patagonia Argentina. In Proceedings of the Second Gondwa-nan Dinosaur Symposium (Tomida, Y.; Rich, T.H.; Vickers-Rich, P.; editors) National Science Museum Monographs 15: 13-45. Tokio. [ Links ]
Calvo, J.O.; Coria, R. 1998. New specimen of Giganoto-sauruscarolini (Coriaand Salgado, 1995), supports it as the largest theropod ever found. Gaia 15: 117-122. [ Links ]
Calvo, J.O.; Mazzetta, G.V. 2004. Nuevos hallazgos de huellas de dinosaurios en la Formación Candeleras (Albiano-Cenomaniano), Picún Leufú, Neuquén, Argentina. Ameghiniana 41 (4): 545-554. [ Links ]
Casamiquela, R.M.; Fasola, A. 1968. Sobre pisadas de dinosaurios del Cretácico Inferior de Colchagua (Chile). Universidad de Chile, Departamento de Geología 30: 1-24. [ Links ]
Casamiquela, R.M.; Corvalán, J.; Franquesa, F. 1969. Hallazgo de dinosaurios en el Cretácico Superior de Chile. Su importanciacronológica-estratigráfica. Instituto de Investigaciones Geológicas, Boletín 25: 1-31. [ Links ]
Casamiquela, RM.; Chong, G. 1980. LapresenciadePtero-daustro Bonaparte (Pterodactyloidea), del Neojurásico (?) de la Argentina, en los Andes del Norte de Chile. In Congreso ArgentinodePaleontologíayBioestrati grafía, No. 2 y Congreso Latinoamericano de Paleontología, No. 1, Actas 1: 201-213. Buenos Aires. [ Links ]
Chong, G. 1977. Contributions to the knowledge of the Domeyko Range, northern Chile. Geologisches Rundschau 66: 374-404. [ Links ]
Chong, G. 1985. Hallazgo de restos óseos de dinosaurios en la Formación Hornitos, Tercera Región (Atacama, Chile). In Congreso Geológico Chileno, No. 4, Actas 1: 152-159. Antofagasta. [ Links ]
Coria, R.; Salgado, L. 1995. A new giant carnivorous dinosaur from the Cretaceous of Patagonia. Nature 377: 244-226. [ Links ]
Coira, B.; Davidson, J; Mpodozis, C; Ramos, V 1982. Tectonic and magmatic evolution of the Andes of northern Argentina and Chile. Earth Science Reviews 18: 303-332. [ Links ]
Farlow, J.O.; Chapman, R.E. 1997. The scientific study of dinosaur footprints. In The Complete Dinosaur (Farlow, J.O.; Brett-Surman, M.K.; editors). Indiana University Press: 519-553. Bloomington. [ Links ]
Galli, C; Dingman, R. 1962. Cuadrángulos Pica, Alca, Matilla y Chacarilla, con un estudio sobre recursos de agua subterránea, provincia de Tarapacá. Carta Geológica de Chile 7-10: 123 p., escala 1:50.000 [ Links ]
Gatesy, S.M.; Middleton, K.M.; Jenkins, FA.J 1999. Three-dimensional preservation of foot movements in Triassic theropod dinosaurs. Nature 399: 141-144. [ Links ]
Groschke, M.; Hillebrandt, A. V; Prinz, R; Quinzio, L. A.; Wilke, H.G 1988. Marine Mesozoic paleogeography in northern Chilebetween21°-26°S. ZwThe Southern Central Andes, Lecture Notes in Earth Sciences (Bahlburg, H; Breitkreutz, C.; Giese, R; editors). Springer-Verlag: 105-117. Berlin. [ Links ]
Herbst, R.; Troncoso, A. 1996. La tafoflora de Juan de Morales del Jurásico Medio (Formación Chacarilla), Región de Tarapacá, Chile. Revista Geológica de Chile 23(1): 3-16. [ Links ]
Jordan, T.E.; Isacks, B.L.; Allmendinger, R.W.; Brewer, J.A.; Ramos, V. A.; Ando, C.J. 1983. Andean tectonics related to geometry of subducted Nazca plate. Geological Society of America Bulletin: 94: 341-361. [ Links ]
Kuban, GJ. 1989. Elongate dinosaur tracks. In Dinosaur Tracks and Traces (Lockley, M.G.; Gillette, D. D.; editors). Cambridge University Press: 165-178. Cambridge. [ Links ]
Leonardi, G. 1989. Inventory and statistics of South American dinosaurian ichnofauna and its palaeobiological interpretation. In Dinosaur Track and Traces (Gillette, D.D.; Lockley, M.G.; editors). Cambridge University Press: 165-178. Cambridge. [ Links ]
Leonardi, G.; Spezzamonte, M. 1994. New tracksites (Dinosauria: Theropoda and Ornithopoda) from the Lower Cretaceous of the Ceará, Brasil. Studi Trentini di Scienze Naturali-Acta Geológica 69: p. 61-70. [ Links ]
Lockley, M.G.; Meyer, C.A.; Hunt, A.P. 1994. Vertebrate tracks and the ichnofacies concept: Implications for palaeoecology and palichnostratigraphy In Paleo-biology of Trace Fossils (Donovan, S.; editor). John Wiley and Sons: 241-268. London. [ Links ]
Miall, A.D. 1996. The geology of fluvial deposits. Sedimentary facies, basin analysis, and petroleum geology. Springer-Verlag: 582. Berlin. [ Links ]
Moreno, K. 2001. Icnocenosis e icnofacies de la Formación Chacarilla (Jurásico Superior-Cretácico Inferior), Norte de Chile. In Reunión Argentina de IcnologíaNo. 4 y Reunión de Icnología del MERCOSUR, No. 2, Actas: 59. Tucumán. [ Links ]
Moreno, K.; Benton, M. J. 2005. Occurrence of sauropod dinosaur tracks in the Upper Jurassic of Chile (rede-scription of Iguanodonichnus frenki). Journal of South American Earth Sciences 20 (3): 253-257. [ Links ]
Moreno, K.; Pino, M. 2002. Huellas de dinosaurios (Theropoda-Ornitopoda- Sauropoda) de la Formación Baños del Flaco, VI Región, Chile: paleoambiente y paleoetología. Revista Geológica de Chile 29 (2): 191-206. [ Links ]
Moreno, K; Rubilar, D.; Blanco, N. 2000. Icnitas de dinosaurios de la Formación Chacarilla, I y II Región, Norte de Chile. Ameghiniana, Suplemento 37: 30. [ Links ]
Moreno, K.; Blanco, N.; Tomlinson, A. 2004 New dinosaur footprints from the Upper Jurassic of northern Chile. Ameghiniana 41 (4): 535-544. [ Links ]
Mpodozis, C; Ramos, V 1989. The Andes of Chile and Argentina. In Geology of the Andes and its relations to hydrocarbon and mineral resources (Ericksen, G. E; Cañas, M.T; Reinemud, J. A.; editors). Circum-Pacific Council for Energy and Mineral Resources, Earth Science Series: 59-89. Houston, Texas. [ Links ]
Mpodozis, C.; Allmendinger, R.W. 1992. Extensión cretácica a gran escala en el norte de Chile (Puquios-Sierra de Fraga, 27° S): significado para la evolución tectónica de los Andes. Revista Geológica de Chile 19 (2): 167-198. [ Links ]
Novas, FE.; de Valais, S.; Vickers-Rich, P.; Rich, T. 2005. A large Cretaceous theropod from Patagonia, Argentina, and the evolution of carcharodontosaurids. Naturwissenschaften 92 (5): 226-230. [ Links ]
Ramos, V; Kay, S. M. 1991. Triassic rifting and associated basalt in the Cuyo Basin, central Argentina. In Andean Magmatism and its tectonic setting (Harmond, R.S.; Rápela, C.W.; editors). Geological Society of America: 79-91. Boulder, Colorado. [ Links ]
Rubilar, D.; Moreno, K; Blanco, N. 2000a. Huellas de dinosaurios ornitópodos en la Formación Chacarilla (Jurásico Superior-Cretácico Inferior), I Región de Tarapacá, Chile. In Congreso Geológico Chileno, No. 9, Actas: A550-554. Puerto Varas. [ Links ]
Rubilar, D.; Moreno, K.; Blanco, N; Calvo, B. 2000b. Report of theropod trackways from Chacarilla Formation (Upper Jurassic-Lower Cretaceous?), Chile. Journal of Vertebrate Paleontology, 20 (Supplement): 66A. [ Links ]
Rubilar-Rogers, D. 2003. Registro de dinosaurios en Chile. Boletín del Museo Nacional de Historia Natural, 52: 137-150. [ Links ]
Rubilar-Rogers, D. 2006. Icnitas de terópodos de la Formación Baños del Flaco (Jurásico Superior), Chile central. In Congreso Geológico Chileno, No. 11, Actas 2: 117-120. Antofagasta. [ Links ]
Rutland, R.W.R. 1971. Andean orogeny and sea-floor spreading. Nature 233: 252-255. [ Links ]
Salinas, P; Marshall, L.; Sepúlveda, R 1991a. Vertebrados continentales del Paleozoico y Mesozoico de Chile. In Congreso Geológico Chileno, No. 6, Actas 1: 310-313. Viña del Mar. [ Links ]
Salinas, R; Sepúlveda, P; Marshall, L 1991b. Hallazgo de restos óseos de dinosaurios (saurópodos), en la Formación Pajonales (Cretácico Superior) Sierra de Almeyda, II Región deAntofagasta, Chile: implicancia cronológica. In Congreso Geológico Chileno, No. 6, Actas 1: 534-537. Viña del Mar. [ Links ]
Tomlinson, A.; Martin, M.; Blanco, N. 2001. U-Pb and K-Ar geochronology from the Cerro Empexa Formation, Ia and 2a Regions, Precordillera, northern Chile. In South American Symposium on Isotope Geology, Comunicaciones 52, Actas l: 169. Pucón. [ Links ]
Vergara,H. 1978. Cuadrángulo Quehuitay sector occidental del cuadrángulo Volcán Miño: Región de Tarapacá. Instituto de Investigaciones Geológicas, Carta Geológica de Chile 32: 44 p., escala 1:50.000. [ Links ]
Manuscript received: April 24, 2007; accepted: September 14.