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Hettangian and Sinemurian (Lower Jurassic) Biostratigraphy of Argentina

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Hettangian and Sinemurian (Lower Jurassic) Biostratigraphy of Argentina Journal of South American Earth Sciences, Vol. 4, No. 3, pp. 159-170, 1991 0895-9811/91 $3.00 + 0.00 Printed in Great Britain © 1991 Pergamon Press pic & Earth Sciences & Resources Institute Hettangian and Sinemurian (Lower Jurassic) biostratigraphy of Argentina A. C. RlCCARDI, S. E. DAMBORENEA, M. O. MANCEÑIDO, and S. C. BALLENT División Paleozoología Invertebrados, Museo de Ciencias Naturales, Paseo del Bosque s/n, 1900 La Plata, Argentina (Received October 1990; accepted May 1991) Abstract—On the northern bank of the Río Atuel, Mendoza province, Argentina, the marine fossiliferous Mesozoic is now known to begin with Hettangian-lower Sinemurian strata. Traditionally, the marine Jurassic sequence in the area was believed to start with upper Sinemurian levels. Representatives of the genera Psiloceras Hyatt, Caloceras Hyatt, Alsatites Haug, Waehneroceras Hyatt, Schlotheimia Bayle, Sulcife rites Spath, Badouxia Guex and Taylor, Vermiceras Hyatt, Coroniceras Hyatt, Agassiceras Hyatt, Euagassiceras Spath, and Arnioceras Hyatt thus indicate the presence of beds equivalent to the Planorbis, Liasicus, Angulata, Bucklandi, Semicostatum, and Turneri zones of the standard international chrono- stratigraphic scale. Hence, in Argentina, the marine Hettangian, Sinemurian, and lowermost Pliens- bachian have been proved only in the neighborhood of the Río Atuel region, where marine Triassic could also be represented. Elsewhere in Argentina, the oldest Jurassic ammonite-bearing levels usually belong to the upper lower or the upper Pliensbachian. Regionally, these findings imply a substantial modification to previous paleogeographic reconstructions for the Early Jurassic of South America. Resumen—En la margen norte del río Atuel, Mendoza, Argentina, la sucesión fosilífera marina del Mesozoico comienza con niveles del Hettangiano y Sinemuriano inferior. Tradicionalmente se había con• siderado que en la región el Jurásico marino comenzaba con el Sinemuriano superior. Representantes de los géneros Psiloceras Hyatt, Caloceras Hyatt, Alsatites Haug, Waehneroceras Hyatt, Schlotheimia Bayle, Sulciferiies Spath, Badouxia Guez y Taylor, Vermiceras Hyatt, Coroniceras Hyatt, Agassiceras Hyatt, Eu- agassiceras Spath y Arnioceras Hyatt, indican la presencia de estratos equivalentes a las zonas de Planor• bis, Liasicus, Angulata, Bucklandi, Semicostatum y Turneri de la Escala Cronoestratigráfíca Internacional. Así en Argentina el Hettangiano, Sinemuriano, y Pliensbachiano basal marinos solamente han sido comprobados en proximidades de la región del río Atuel, donde también podrían hallarse representados niveles de Triásico marino. En el resto de Argentina los niveles más antiguos portadores de amonites del Jurásico corresponden generalmente al Pliensbachiano inferior alto o Pliensbachiano superior. Desde el punto de vista regional estos hallazgos determinan una modificación substancial en la paleogeografía del Jurásico temprano de América del Sur. INTRODUCTION the first marine fossils are dated as late early Pliens• bachian (Riccardi, 1984). THE LOWER JURASSIC stratigraphy and paleontology In South America, marine Hettangian and lower of the northern bank of the Rio Atuel has been briefly Sinemurian strata have been previously recorded in described by Burckhardt (1900, 1903), Jaworski Chile (Cecioni, 1960; Thiele, 1967; Cecioni and (1914,1915,1925), Gerth (1925), Groeber (1947), and Westermann, 1968; Minato, 1977; Escobar, 1980; Groeber et al. (1953). According to these authors and Hillebrandt, 1970, 1973, 1981, 1987, 1988; Quinzio, to more recent studies (Stipanicic, 1969; Stipanicic 1987), in Peru (Hyatt, 1889; Lisson, 1911; Tilmann, and Bonetti, 1970; Volkheimer, 1978; Rosenfeld and 1917; Schindewolf, 1957; Geyer, 1979; Prinz, 1983, Volkheimer, 1980, 1981; Hillebrandt, 1973, 1981, 1985a,b), in Ecuador (Geyer, 1974), and in Colombia 1987; Damborenea, 1987a), the Jurassic of the area (Geyer, 1973,1976). has been considered to include the following (Riccardi The marine Hettangian and the lower Sinemur• 1983): below, 900 meters of a mainly conglomeratic ian of central Chile are restricted to the Coastal Cor• unit, the El Freno Formation, lacking fossil dillera between Vichuquén and Batuco (35-35°15'S; invertebrates and questionably dated as Hettangian; Thiele, 1967; Corvalán, 1976, 1982; Minato, 1977; above, about 300 meters of marine sandstones, the El Escobar, 1980) and between Los Vilos and Los Molles Cholo or Puesto Araya Formation. Fossil inverte• (32-32°15'S; Fuenzalida, 1938; Cecioni, 1960; Cecioni brates found at different levels of the Puesto Araya and Westermann, 1968). In the Principal Cordillera Formation indicated (?early) late Sinemurian to late of Argentina, the Sinemurian dating of the earliest Pliensbachian ages (Stipanicic, 1969; Riccardi, 1983). marine Jurassic of the Rio Atuel area was supported This succession was believed to document the earliest until quite recently by Hillebrandt's studies (1989). marine Mesozoic of Argentina because in other areas The Pliensbachian stratigraphy of the Rio Atuel area was studied by three of us in 1973 (ACR, SED, Address all correspondence and reprint requests to: MOM; field samples 346-371), and the upper Sine• Dr. A. C. Riccardi (telephone: [541(21)24-4278; telefax: 154] murian and Pliensbachian by two of us in 1983 (SED, (21)25-5004). MOM; field samples 1251-1276). In 1986 (field samples 1384-1477), we undertook field studies over ammonite systematics were used (Donovan et al. the whole region in order to find and date the 1981). Fossil specimens, labeled MLP, are in the col• beginning of the marine Mesozoic. Four selected sec• lections of the Museo de La Plata. tions were studied from west to east along the northern bank of the Rio Atuel between Laguna El Sosneado and Arroyo Blanco (Figs. 1 and 2). These BIOSTRATIGRAPHY studies documented for the first time the existence of marine Hettangian and provided a rich fauna of early Ammonite Zonation Sinemurian invertebrates. Supplementary sampling (1693-1732) and field observations were conducted in Psiloceras Assemblage Zone (I on Fig. 2). This 1988 (Riccardi et al., 1988). zone was defined by Riccardi et al. (1988) in the In classifying the fossiliferous succession on the Arroyo Malo section (Fig. 2A). The beds are about 45 basis of its ammonites, we follow Riccardi et al. meters thick and overlie 300 meters of unfossili- (1990b) and distinguish three levels of stratigraphic ferous turbidites (base not exposed). The zone is units. The lowest level of classification is the "faunal characterized near the base (levels 1384-1385) by horizon," the next is the "assemblage zone," and the Psiloceras cf. tilmanni Lange (Fig. 4, nos. 1-2), and in third level of classification is the "standard chrono- the upper parts (levels 1389, 1701) by Caloceras cf. zone." In the correlation of these units with the peruvianum (Lange) (Fig. 4, nos. 3-5). The middle European standard zonation (Fig. 3), horizontal divi• part of this interval (levels 1386, 1699) yields Psilo• sions are shown as not coinciding in order to avoid ceras cf. rectocostatum Hill. (Fig. 4, no. 6) and a loose implying exact time correlation. Donovan's generic fragment of ?Alsatites cf. liasicus (d'Orb.). Fig. 1. Index map to sections in the Rio Atuel area. w A-ARROYO MALO B- ARROYO EL D-PUESTO PEDRERO ARAYA "I 366-371 lit •^363 H73 - H76 1726 - 1732 — H72 H70 , rm "I , M9 i^rA J 1106 , 1723 ~~-{ — H07 — 1721 - 1722 i J mi -1720 _ Sills 200 m Llmsstonas — 1397-1380 , 1706 Shalas it JM-U-J _1391-5,1707 Mudstonss 100 Sandstones 1702- 1706 3 1*31 I 1390- 1393 l*.v3 Conglomsfates 1 1361- 1369 J 1699-1701 — runjuucm Ammblag* Zon« -Kill — OubfIff• As««mbl«9« Zon« 3QC - MMtocf • AMM*IH« ZOO* 5E — Epophlocf— AtMmbl«9« Zona I — A—itetfH AMbmblftM Zon* 17 — Vwmlctfii AiHmMigi Zoo» HE — BadouKto cwidtuli Zooo I — ttfroomrocor— - Schlothohnm Attombfago Zona I — Estocara• Aaaaotblag* Zoo* Wb. CJtltomoulttM Fig. 2. Columnar sections at Arroyo Malo, Arroyo El Pedrero, Arroyo Las Chilcas, and Puesto Araya, with local zonation. The fragmentary specimen identified as Psilo• previously compared with this species (Hillebrandt, ceras cf. tilmanni is similar to material from Peru 1981, pi. 1, fig. lab; Prinz, 1985a, pi. 1, fig. e) has (Tilmann, 1917, pi. 22, fig. 1) included in P. tilmanni more recently been referred to P. rectocostatum and P. Lange (1925, p. 474). This species has recently been primocostatum Hillebrandt (1988, p. 63, 67). used as index of a "Zone of Psiloceras tilmanni" In Europe, P. plicatulum and C. johnstoni are the (Hillebrandt, 1988). Caloceras peruvianum re• index species of the middle and upper subzones of the sembles C. johnstoni (J. de C. Sowerby), a widely Planorbis zone. The age of this assemblage is there• distributed species known from the Planorbis zone of fore early Hettangian, (?early to) late Planorbis zone Europe, Alaska, and Canada (Blind, 1963, pi. 1, fig. 4; (Fig. 3). The underlying 300 meters of unfossiliferous Prebold and Poulton, 1977, pi. 1, figs. 3-8; Imlay, turbidites are probably Late Triassic to early Planor• 1981, pi. 1, figs. 11-16). Caloceras peruvianum bis in age. Early Hettangian invertebrate faunas are (Lange) is known from Peru (Tilmann, 1917, pi. 22, known from Peru (Lisson, 1911; Tilmann, 1917; figs. 2-3; Prinz, 1985b, pi. 2, fig. 5), and Chile (Cecioni Geyer, 1979; Prinz, 1985a,b) and Chile (Cecioni and and Westermann, 1968, pi. 6, figs. 7-8; Hillebrandt, Westermann, 1968; Escobar, 1980; Hillebrandt, 1981, 1987, pi. 1, fig. 6; Quinzio, 1987, pi. 1, figs. 5-6). Some
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