N. Jb. Geol. Paläont. Abh. 257/2, 181– 236 published online June 2010
Article
Ammonites from the Maastrichtian (Upper Cretaceous) Quiriquina Formation in central Chile Christian Salazar, Heidelberg, Wolfgang Stinnesbeck, Heidelberg, Luis Arturo Quinzio-Sinn, Concepción With 48 figures
SALAZAR, C., STINNESBECK, W. & QUINZIO-SINN, L. A. (2010): Ammonites from the Maastrichtian (Upper Cretaceous) Quiriquina Formation in central Chile. – N. Jb. Geol. Paläont. Abh., 257: 181–236; Stuttgart. Abstract: The Quiriquina Formation in central Chile is famous for its abundant and diverse ammonite assemblages of Maastrichtian age. In the type locality around the Concepción Bay in the Bío-Bío Region of central Chile we have identified a total of 30 species referred to 17 genera. Hypophylloceras (Neophylloceras) ramosum, H. (N.) hetonaiense, H. (N.) inflatum, H. (N.) surya, Anagaudryceras politissimum, Gaudryceras kayei, Zelandites varuna, Pseudophyllites indra, Kitchinites darwini, Kossmaticeras (Natalites) erbeni, Grossouvrites gemmatus, Gunnarites spinosissimus, Maorites densicostatus, Pachydiscus (P.) jacquoti chilensis, Menuites fresvillensis, Diplomoceras cylindraceum, Phylloptychoceras sp., Baculites huenickeni, Baculites vicentei and Eubaculites carinatus have been recorded previously from the Quiriquina Formation. Hoploscaphites constrictus quiriquiniensis sensu WILCKENS (1904). Phyllopachyceras forbesianum, Anagaudryceras subtilineatum, Gunnarites cf. bhavaniformis and Baculites anceps are new records for the Quiriquina Formation added here. Kitchinites vicentensis n. sp., Kitchinites ifrimae n. sp., Grossouvrites joharae n. sp., Pachydiscus (P.) gutierrezi n. sp. and Menuites gerardoi n. sp. are new. Gaudryceras kayei specimens are recorded with diameters in excess of 200 mm and present marked changes during growth. Anagaudryceras politissimum and Zelandites varuna also show strong ontogenetic changes. Kitchinites darwini of the Quiriquina Formation differs from material from Antarctica; we propose that the latter should by separated. The presence of Hypophylloceras (Neophylloceras) surya, Zelandites varuna, Pachydiscus (P.) jacquoti, Diplomoceras cylindraceum, Baculites anceps, Eubaculites carinatus and Hoploscaphites constrictus quiriquiniensis indicates a Maastrichtian age for the Quiriquina Formation. Menuites fresvillensis confirms the late Maastrichtian age for most of the Quiriquina Formation. The assemblage presented shows cosmopolitan and Indo-Pacific affinities with a few European and Tethyan links. Key words: Maastrichtian, ammonites, Quiriquina Formation, Chile.
Concepción Bay are best known for their diverse invertebrate assemblages. Outcrops in Quiriquina Island have been considered to be the most expanded and Las Tablas Bay on the Northwestern shore described as the type locality (BIRÓ 1982 a). Additional important outcrops on Quiriquina Island are located
1. Introduction In central Chile, the uppermost Cretaceous Quiriquina Formation occurs locally along the Pacific Ocean coast, from Algarrobo near Santiago in the north, to the Arauco Peninsula in the south. Sections in the
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DOI: 10.1127/0077-7749/2010/0072
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Fig. 1. Map of the Chilean territory showing the location of outcrops of the Quiriquina Formation in the area of Concepción. CA: Cerro Amarillo; CC: Cerro Chacabuco; CO: Cocholgüe; EC: Cerro El Conejo; HU: Hualpencillo; LC: Los Chilcos; LI: Lirquén; LT: Las Tablas; LV: Los Viejos; PA: Punta de Parra; PP: Puente Perales; SV: San Vicente; SM: Cerro San Martín; SS: Santa Sabina; TO: Tomé.
along the West coast, such as the beach cliffs Los Viejos (the “Saurierbucht” of STEINMANN 1895) and Los Chilcos, northeast of Las Tablas (Fig. 1). Sections in Concepción Bay are found along the beaches of Cocholgüe, Tomé, Punta de Parra and Lirquén. In the urbanised area of Concepción-Talcahuano, outcrops exist at San Vicente, Cerro El Conejo, Cerro San Martín, Hualpencillo, Puente Perales, Cerro Chacabuco, Cerro Amarillo and Santa Sabina.
MANN (1895) described a section (the “Saurierbucht”) on the western coast of Quiriquina Island as the “locus typicus” of the “Quiriquinian Stage” and determined its age as Late Senonian. STEINMANN et al. (1895) described the molluscan assemblage from this locality and compared the ammonites with coeval assemblages from India and New Zealand, thus establishing the Indo-Pacific relationship. WILCKENS (1904) and WETZEL (1930) revised the bivalves and gastropods, while the latter (WETZEL 1930) contributed sedimentological and palaeoecological data on the Quiriquina Formation. Additional faunal data and taxonomic revisions were published on bird remains (LAMBRECHT 1929), plesiosaurs (BROILI 1930), microfossils (WETZEL 1960), baculitids (HÜNICKEN & COVACEVICH 1975), trigoniids (PÉREZ & REYES 1978; MAEDA et al. 1981), the
2. Previous work Palaeontological studies of the Quiriquina Formation and its faunal assemblages date back to the first half of the nineteenth century and were carried out by D’ORBIGNY (1842), FORBES (in DARWIN 1846), HUPÉ (1854), GABB (1860), and PHILIPPI (1887). STEIN-
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Fig. 2. Cross section of the Quiriquina Formation at Las Tablas (Type Section) with lithological units, ammonite zones and ranges of ammonite species.
Maastrichtian, based on ranges of ammonite species.
ammonite Hoploscaphites and the coleoid Naefia (BIRÓ 1982b, c), turtle remains (GASPARINI & BIRÓ 1986), callianassid srimps and crabs (FÖRSTER & STINNESBECK 1987), and gastropods (BANDEL & STINNESBECK 2000). Plants and palynomorphs have been studied by DOUBINGER (1972), STINNESBECK (1986), TORRES & BIRÓ (1986), NISHIDA (1985), and NISHIDA et al. (1990). In 1986, STINNESBECK evaluated the depositional facies and revised bivalve and ammonite assemblages. He concluded that the Quiriquina Formation was Maastrichtian in age. In a later paper, STINNESBECK (1996) further restricted the age of the Quiriquina Formation to the upper
3. Geology and sections The geology of the Concepción area is simple. The metamorphic basement of Palaeozoic age consists of schists of the Oriental Series (AGUIRRE et al. 1972) and granitoids of the Nahuelbuta Complex (PARADA et al. 2007), the latter being part of the Chilean Coastal batholite. An angular disconformity separates these rocks from overlying sediments, either the latest Cretaceous Quiriquina Formation, or the Paleocene
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Ammonites were coated with magnesium oxide prior to photography, except where indicated otherwise.
to Eocene Curanilahue, Cosmitos and Cerro Alto formations. At the type locality at Las Tablas, the Quiriquina Formation is 65 m thick. Layers dip about 105º to the SW. STINNESBECK (1986) differentiated the following lithological units (from base to top, fig. 2): The Quiriquina Formation overlies Paleozoics shists with an angular disconformity. The lowermost 15 metres correspond to a polymictic basal conglomerate, which is composed of rounded and angular clasts of schists, meta-sandstone and quartz. Resting on this unit are 6.5 metres of yellow, cross-bedded sandstone and interbedded conglomeratic lenses. Upsection, a 10 m thick unit of glauconitic green sandstone is present; 5-30 cm thick resistant coquina layers are intercalated; these have been interpreted as tempestites (STINNESBECK 1986). Faunal assemblages in these coquinas are dominated by bivalves, principally Cardium and Pacitrigonia, which indicate shallow-water environments less than 20 m in depth. The coquina unit grades into a 35 metre-thick unit of intensively bioturbated, green sandstone-siltstone with levels of calcareous sandstone concretions. The latter are between 20 and 100 cm in diameter and are alligned parallel to the stratification. The uppermost 2 to 3 m of this unit is without records of ammonites but do yield detritus-feeding bivalves (e. g., N. (Neilo) pencana, N. (Neilo) quiriquinae, Yoldia levitestata, Nucula cocholguei and Tellina largillierti). Teichichnus and Zoophycos are abundant at these levels (STINNESBECK 1986). Ammonite species are known from the unit of yellow cross-bedded sandstone upwards to the last 2 or 3 metres of the Quiriquina Formation (Fig. 2).
5. Systematic palaeontology D imens ions : All dimensions are given in mm. Uncertain values due to deformation of specimens and ratios resulting from uncertain measurements are in brackets. Abbreviations: D: Diameter, Wb: Whorl breadth, Wh: Whorl height, U: Width of umbilicus. Suture ter minology: Abbreviation of sutural elements corresponds to: E: External lobe, L: Lateral lobe, U: Auxiliary lobes (some with index: UB1B, UB2B, ...), I: Internal lobe. The saddles are denoted as: E/L: Saddle between external and lateral lobe, L/U: Saddle between lateral and outer auxiliary lobe. Collections : The registration prefix is CPUC (Colección Paleontológica de la Universidad de Concepción) and Q (Quiriquina Formation). For abbreviations of sections see Fig. 1. All specimens described and figured herein are registered and housed at the Paleontological Collection of the Departamento de Ciencias de la Tierra of the University of Concepción, Chile. Other collections mentioned are BMNH, The Natural History Museum, London; GK, Kyushu University, Fukuoka; IPB, Institut für Paläontologie Bonn; IRSNB, Institut Royal des Sciences Naturelles de Belgique; TM, Transvaal Museum, Pretoria; USNM, United States National Museum, Washington, D.C.; WAM, Western Australian Museum. S ys tematics : Systematic nomenclature follows the “Treatise on Invertebrate Paleontology” (WRIGHT et al. 1996) to subspecies level, except for Gaudryceras. S ynonymies : Only references of the original description, some synonyms and all references used for the definition of species are included. Where possible, more complete lists of synonymy are indicated.
4. Material
Order Ammonoidea Z ITTEL, 1884 Suborder Phylloceratina ARKELL, 1950 Superfamily Phylloceratoidea ZITTEL, 1884 Family Phylloceratidae ZITTEL, 1884 Subfamily Phylloceratinae ZITTEL, 1884 Genus Hypophylloceras SALFELD, 1924 Subgenus Neophylloceras SHIMIZU, 1934
Fossil preservation is good to very good, most being preserved three-dimensionally, only a few specimens are deformed. Most ammonites preserve the shell with ornament. Suture lines are observable only in some of them. Our material includes new collections from localities in Quiriquina Island (Las Tablas, Los Viejos), in Concepción Bay (Cocholgüe, Tomé, Lirquén), at San Vicente, and in the urbanised area of Concepción-Talcahuano. We also include specimens housed at the University of Concepción, collected in the 1970s and 1980s by the late LAJOS BIRÓ. As to the palaeobiogeographic distribution we shall use mainly the standards used by IFRIM et al. (2004), who differentiated between Cosmopolitan, Indo-Pacific, EuropeTethys and Endemic taxa. Differentiated warm or cold water species will only be used in relation to the latitudinal distribution.
Type s pecies : Ammonites (Scaphites?) ramosum (MEEK, 1857). For discussion of genus and subgenus, see HENDERSON & MCNAMARA (1985).
Hypophylloceras (Neophylloceras) ramosum (MEEK, 1857) Figs. 3, 4 a-d, m
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Fig. 3. Relationship between Wb/Wh and D of Hypophylloceras (Neophylloceras) ramosum (MEEK, 1857), Hypophylloceras (Neophylloceras) hetonaiense (MATSUMOTO, 1942) and Hypophylloceras (Neophylloceras) inflatum STINNESBECK, 1986.
dense lirae, prorsiradiate and flexuous. Lirae are slightly concave on umbilical shoulder, convex on median flank, concave on ventrolateral portion of flank and convex across venter.
1857 Ammonites (Scaphites?) ramosum MEEK, p. 45. ?1895 Phylloceras ramosum MEEK. – STEINMANN, p. 80, pl. 5, fig. 5. 1904 Phylloceras ramosum (MEEK). – WILCKENS, p. 187. 1930 Phylloceras (Schlueteria) ramosum (MEEK). – WETZEL, p. 87. 1970 Neophylloceras ramosum (MEEK). – HENDERSON, p. 5, pl. 1, fig. 3; text-fig. 2. 1985 Phylloceras (Neophylloceras) ramosum (MEEK). – HENDERSON & MCNAMARA, p. 40, pl. 1, figs. 1-3; text-fig. 2c. 1986 Phylloceras (Neophylloceras) ramosum (MEEK, 1957); STINNESBECK, p. 189, pl. 7, figs. 1-2. 1993 Phylloceras (Neophylloceras) ramosum (MEEK); WARD & KENNEDY, p. 15, fig. 17.2, 17.5, 17.6. 1994 Neophylloceras ramosum (MEEK); YAZIKOVA, p. 287, pl. 1, figs. 9-10.
Dimensions CPUC/Q/ TO/3323 CPUC/Q/ LV/102 CPUC/Q/ TO/3236 CPUC/Q/ CO/3603 CPUC/Q/ CO/3164 CPUC/Q/ TO/3597 CPUC/Q/ LT/3601 CPUC/Q/ TO/3602 CPUC/Q/ CO/2517 CPUC/Q/ CO/3596 CPUC/Q/ CO/2536 CPUC/Q/ CO/2705 CPUC/Q/ CO/3604
Ty p e : Holotype USNM 12451, the specimen illustrated by MEEK (1857: 45), is from the Maastrichtian of Vancouver Island, Canada. M a te r ia l: 17 specimens, 13 of which are complete and four are fragmentary phragmocones. Only the best-preserved specimens were measured and listed. D e s c r ip tio n : Coiling is very involute and whorl section compressed. Umbilicus is narrow, with an U/D between 0.07 and 0.09, and steep umbilical walls. Whorl section is discoidal, flanks near straight and weakly converging towards the narrowly rounded venter. Ornament consists in
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D
Wb
Wh
Wb/Wh U
U/D
12.0
4.0
6.5
0.61
1.0
0.08
15.5
8.0
14.0
0.57
1.5
0.09
19.0
6.0
10.5
0.57
1.5
0.07
23.0
7.0
13.5
0.53
2.0
0.08
27.0
8.0
18.0
0.44
2.0
0.07
27.0
8.0
15.5
0.52
2.0
0.07
33.0
8.5
21.0
0.40
3.0
0.09
-
10.5
21.0
0.50
-
-
40.0
12.0
25.0
0.52
3.0
0.07
41.0
15.0
25.0
0.60
3.0
0.07
46.0
13.5
27.0
0.50
3.5
0.07
50.0
15.0
28.0
0.53
3.5
0.07
56.0
15.5
34.0
0.45
3.5
0.06
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CPUC/Q/ CO/2793 CPUC/Q/ LT/3598
(57.0) (16.0) (35.0) (0.45)
4·0
(0.07)
-
7.0
-
29.0
56.0
0.52
D es cription: Coiling very involute and whorl section compressed. Umbilicus narrow (U/D 0.6-0.9) and umbilical wall steep. Whorl section discoidal. Flanks almost subparallel, with maximum width at mid-flank. Venter narrowly rounded. Ornament of dense lirae, slightly prorsiradiate and gently flexuous. Lirae are distinctly concave in umbilical area, straight to slightly concave at mid-flank, and straight in ventrolateral area and across venter. Between 5 and 6 weak concentric depressions are present on flanks.
R e ma r k s : H. (N.) ramosum is characterised by a discoidal whorl section, flanks which slightly converge towards the venter and flexuous lirae. H. (N.) hetonaiense is closely related, but flanks are almost subparallel, lirae are less flexuous and slightly prorsiradiate, and 5 to 6 weak concentric depressions are present on the flank which are not seen in H. (N.) ramosum. H. (N.) inflatum is clearly different mainly on account of whorl section which is more inflated (Fig. 3). HENDERSON & MCNAMARA (1985) and WARD & KENNEDY (1993) presented a full discussion of H. (N.) ramosum. The specimen of STEINMANN (1895) probably is lost (STINNESBECK 1986).
Dimensions CPUC/Q/ TO/3324 CPUC/Q/ LT/3606 CPUC/Q/ LT/3610 CPUC/Q/ CO/2497 CPUC/Q/ CO/3599 CPUC/Q/ CO/1915 CPUC/Q/ CO/3607 CPUC/Q/ CO/2333 CPUC/Q/ CO/3497 CPUC/Q/ CO/3449 CPUC/Q/ CO/2479 CPUC/Q/ TO/3329 CPUC/Q/ LT/3609 CPUC/Q/ LT/3608 CPUC/Q/ LI/3145 CPUC/Q/ CO/3139 CPUC/Q/ CO/3109 CPUC/Q/ CO/3138
O c c u r r e n c e : In the Quiriquina Formation (sections Las Tablas, Los Viejos, Cocholgüe and Tomé), this taxon is abundant in the unit with calcareous sandstone concretions, in the upper Eubaculites carinatus Zone (Kitchinites (K.) darwini Subzone). Elsewhere, H. (N.) ramosum is widely distributed in upper Campanian to Maastrichtian strata, with records from British Columbia and California, southern Argentina, eastern Russia, as well as SantonianMaastrichtian of New Zealand. In Western Australia, the species occurs in the upper Maastrichtian Miria Formation (HENDERSON & MCNAMARA 1985). In the Biscay region, it has been recorded from the upper A. mayaroensis planktic foraminiferal zone of the upper Maastrichtian (WARD & KENNEDY 1993). H. (N.) ramosum appears to be restricted to high latitudes over 30º north and south.
Hypophylloceras (Neophylloceras) hetonaiense (MATSUMOTO, 1942) Figs. 3, 4 g-h, k-l 1942
Neophylloceras hetonaiense MATSUMOTO, p. 675, fig. 1a3, 1b3. ? 1953 Neophylloceras hetonaiense MATSUMOTO. – SPATH, p. 5, pl. 1, fig. 2. 1959 Neophylloceras hetonaiense MATSUMOTO. – MATSUMOTO, p. 5, pl. 3, fig. 1. 1963 Neophylloceras hetonaiense MATSUMOTO. – JONES, p. 23, pl. 6, fig. 9, 10; pl. 7, fig.1; text-fig 8. 1986 Phylloceras (Neophylloceras) hetonaiense (MATSUMOTO). – STINNESBECK, p. 190, pl. 7, figs. 3-4; textfigs. 16 b, 17a (with full synonymy). 1994 Neophylloceras hetonaiense MATSUMOTO. – YAZIKOVA, p. 288, pl. 1, figs. 5-7. 2004 Hypophylloceras (Neophylloceras) hetonaiense MATSUMOTO. – IFRIM et al. p. 1578, text-figs. 2F-H, 3D.
D
Wb
Wh
Wb/Wh U
U/D
15.0
4.5
8.0
0.56
1.3
0.08
22.5
6.5
12.5
0.54
2.0
0.08
23.5
8.0
14.5
0.55
2.0
0.08
27.0
9.0
17.0
0.52
2.0
0.07
35.0
11.0
21.0
0.52
2.0
0.06
38.0
10.0
22.0
0.45
3.5
0.09
38.0
10.5
22.5
0.46
2.5
0.06
-
12.0
-
-
-
-
(44.0) 12.5
25.0
0.50
3.5
(0.07)
46.0
13.0
26.0
0.50
3.5
0.07
-
15.0
31.0
0.48
4.0
-
52.0
15.0
28.0
0.54
4.0
0.08
54.0
16.0
33.0
0.48
3.5
0.06
(57.0) 17.5
35.0
0.50
4.0
(0.07)
-
20.0
37.0
0.54
4.0
-
-
21.0
42.0
0.50
-
-
(82.0) 24.0
42.0
0.57
3.5
(0.04)
-
56.0
0.48
-
-
27.0
Fig. 4. a-d, e: Hypophylloceras (Neophylloceras) ramosum (MEEK, 1857), a-b: CPUC/Q/CO/2536, x1; c-d: CPUC/Q/CO/2705, x1; e: CPUC/Q/CO/2705, x1. f, i-j, m Hypophylloceras (Neophylloceras) inflatum STINNESBECK, 1986, f: CPUC/Q/TO/522, x2; i-j: CPUC/Q/LT/3642, x2; m: CPUC/Q/CO/3445, x2;. g-h, k-l: Hypophylloceras (Neophylloceras) hetonaiense (MATSUMOTO, 1942), g-h: CPUC/Q/CO/2497, x1; k-l: CPUC/Q/CO/3109, x1.
Ty p e : Lectotype is GK. H3801, designated by MATSU(1959: 5, pl.3, fig. 1).
MOTO
M a te r ia l: Twenty specimens, thirteen of which are complete and seven fragmentary phragmocones.
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Fig. 4 (Legend see p. 186)
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Fig. 5. a-f, Gaudryceras kayei (FORBES, 1846), a-b: CPUC/Q/LI/400, x1; c-d: CPUC/Q/TO/3322, x1. e-f: CPUC/Q/ CO 1337, x1. g-h: Anagaudryceras subtilineatum (KOSSMAT, 1895), CPUC/Q/CO/3062, x1. i-j: Anagaudryceras politissimum (KOSSMAT, 1895) CPUC/Q/LT/3592, x1. k-l: Phyllopachyceras forbesianum (D’ORBIGNY, 1850), CPUC/Q/ LT/248, x1. m: Hypophylloceras (Neophylloceras) surya (FORBES, 1846), CPUC/Q/LT/3648, x 0.5.
Remarks: H. (N.) hetonaiense differs from H.(N.) ramosum in having less flexuous lirae, by flanks which are almost subparallel, and by 5 to 6 weak concentric depressions on the flank. H. (N.) hetonaiense differs from H. (N.) inflatum by simple unforged lirae, and a less inflated whorl section (Fig. 3).
Maastrichtian (YAZIKOVA 1994). In the Mendez Formation of the northeast Mexico, H. (N.) hetonaiense was recorded by IFRIM et al. (2004) from the lower Maastrichtian planktic foraminiferal biozone CF 7 (LI et al. 1999). H. (N.) hetonaiense appears to be a cold-water species (IFRIM et al. 2004) restricted to northern and southern high latitudes.
O c c u r r e n c e : In the Quiriquina Formation (sections Las Tablas, Cocholgüe, Tomé and Lirquén), this taxon is present in the unit of calcareous sandstone concretions, in the Eubaculites carinatus Zone (Kitchinites (K.) darwini subzone and top of Menuites fresvillensis subzone). In the Antarctic Peninsula, H. (N.) hetonaiense is assigned to the Campanian-Maastrichtian (SPATH 1953). The species is also known from the Maastrichtian of Japan (MATSUMOTO 1942), Alaska (JONES 1963) and California (MATSUMOTO 1959). In eastern Russia, it is assigned to the upper
Hypophylloceras (Neophylloceras) inflatum STINNESBECK, 1986 Figs. 3, 4 f, i-j, m 1930 1986
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Phylloceras nera PAULCKE (non FORBES), WETZEL, p. 87. Phylloceras (Hypophylloceras) inflatum STINNESBECK, p. 192, pl. 7, fig. 8.
Ammonites from the Maastrichtian Quiriquina Formation in central Chile
1985
Phylloceras (Neophylloceras) surya (FORBES). – HENDERSON & MCNAMARA, p. 42, pl. 1, figs. 7-8, 11-12; pl. 2, figs. 1-2; text-fig. 2g (with synonymy). 1986 Phylloceras (Neophylloceras) surya (FORBES). – STINNESBECK, p. 193, pl. 7, figs. 5-7. 1992a Phylloceras (Neophylloceras) surya (FORBES). – KENNEDY & HENDERSON, p. 391, pl. 1, figs. 1-7, 9, 13-14; pl. 15, figs. 4-5 (with additional synonymy). 1993 Phylloceras (Neophylloceras) surya (FORBES). – WARD & KENNEDY, p. 16, figs. 17.13, 18.3, 18.4, 18.16, 18.17. 1993 Phylloceras (Neophylloceras) surya (FORBES). – BIRKELUND, p. 43, pl. 2, fig. 2. 1999 Phylloceras (Neophylloceras) surya (FORBES). – FATMI & KENNEDY, p. 643, figs. 4.1-4.6, 15.3. ? 2004 Hypophylloceras (Neophylloceras) sp. cf. H. (N.) surya (FORBES). – IFRIM et al., p. 1580, text-figs. 2C-E, 3A.
Type: Holotype is Phylloceras nera in WETZEL 1930 (p. 87), designated by STINNESBECK (1986). Paratypes are QVO/ 181-186, QVO/188, C22/30 and TO/210 of STINNESBECK (op. cit.). The type material is from Quiriquina Island, Chile. M a te r ia l: Seven specimens, five of which correspond to complete and two to fragmentary phragmocones. D e s c r ip tio n : Coiling very involute and whorl section compressed. Umbilicus narrow (U/D 0.11-0.13) and umbilical area steep and narrowly rounded. Whorl section discoidal and slightly inflated, with evenly convex flanks. Venter narrowly rounded. In dorsolateral area, between 10-12 bullae present per whorl. First and second order lirae extend from these bullae and are prorsiradiate and flexuous. Second order lirae progressively projected from first order lirae. All lirae cross flank and venter, parallel and equidistant. Dimensions CPUC/Q/ TO/3448 CPUC/Q/ TO/3450 CPUC/Q /TO/522 CPUC/Q/ TO/3445 CPUC/Q/ LT/3642 CPUC/Q/ LT/3643 CPUC/Q/ LT/1778
D
Wb
Wh
Wb/Wh U
U/D
17.0
6.5
9.0
0.72
2.0
0.12
16.0
6.5
10.0
0.65
2.0
0.13
18.0
7.0
10.5
0.67
2.0
0.11
23.5
8.5
12.5
0.68
2.5
0.11
-
9.0
13.5
0.66
2.0
-
-
11.0
16.0
0.68
-
-
-
11.5
(15.0) (0.77)
-
-
Type: Lectotype is BMNH C51074, the original of KOSSMAT, 1895, pl. 16 (2), fig. 1a-c, by subsequent designation of KENNEDY & HENDERSON (1992a, pl. 1, figs. 13-14). M aterial: Three specimens, one of which corresponds to a complete and two to fragmentary phragmocones. D es cription: Coiling very involute. Umbilicus narrow (U/D 0.11) and with steep umbilical walls. Whorl section discoidal. Flanks weakly convex and slightly converging towards venter, with maximum width at mid-flank. Venter acutely rounded. Ornament of 10-11 undulating ribs per half whorl, present from umbilical shoulders to ventral part of flank, but weakening towards venter, flexuous and prorsiradiate. Additional secondary fine ribs successively initiate from principal ribs and cross flanks and venter parallel and in equidistance.
R e ma r k s : H. (N.) ramosum and H. (N.) hetonaiense differ from H. (N.) inflatum in having a less inflated whorl section (Fig. 3) and in the absence of bullae and second order lirae. STINNESBECK (1986) presented a full discussion of this species.
Dimensions CPUC/Q/ LT/3647 CPUC/Q/ CO/2490 CPUC/Q/ LT/3648
O c c u r r e n c e : In the Quiriquina Formation (sections Las Tablas and Tomé), H. (N.) inflatum is recorded from the Eubaculites carinatus Zone, extending from the upper part of the unit with coquina layers to the unit with calcareous sandstone concretions. Currently, H. (N.) inflatum is known only from the Quiriquina Formation.
1976
D
Wb
Wh
Wb/Wh U
U/D
-
-
-
-
-
-
-
27.0
53.0
0.51
-
-
101.0 29.0
56.0
0.51
12.0
0.11
Remarks : HENDERSON & MCNAMARA (1985) presented a full description and discussion of this species. IFRIM et al. (2004) described specimens from Mexico in open nomenclature.
Hypophylloceras (Neophylloceras) surya (FORBES, 1846) Figs. 5m, 6a 1846 1956
189
O ccur rence: In the Quiriquina Formation (sections Las Tablas and Cocholgüe), H. (N.) surya is recorded from the uppermost metres of the unit with calcareous sandstone concretions, in the Zone “without-Baculitids”. Elsewhere, H. (N.) surya is known from the Maastrichtian of Madagascar (COLLIGNON 1956) and South Africa (KENNEDY & KLINGER 1976). In northeastern Mexico, it is possibly known from the lower Maastrichtian (IFRIM et al. 2004). In Western Australia, the species is assigned to the upper
Ammonites surya FORBES, p. 106, pl. 7, fig. 10. Epiphylloceras mikobokense COLLIGNON, p. 24, pl. 2, fig. 3, 3a; pl. 4, fig. 5, 5a, 5b. Phylloceras (Hypophylloceras) mikobokense (FORBES); KENNEDY & KLINGER, p. 368, pl. 12, fig. 1.
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C. Salazar et al.
Fig. 6. a: Hypophylloceras (Neophylloceras) surya (FORBES, 1846), CPUC/Q/CO/2490, x1. b-c, e-f, i: Zelandites varuna (FORBES, 1846), b-c: CPUC/Q/LT/3590, x1; e-f: CPUC/Q/CO/3163, x1; i: CPUC/Q/LV/3591, x1. d, g-h, Anagaudryceras politissimum (KOSSMAT, 1895), d: CPUC/Q/LT/3593, x1; g-h: CPUC/Q/LT/571, x1.
Genus Phyllopachyceras SPATH, 1927
Maastrichtian (HENDERSON & MCNAMARA 1985). In South India, it may belong to the lower part of the A. mayaroensis biozone of the upper Maastrichtian (KENNEDY & HENDERSON 1992a). In the Biscay region, WARD & KENNEDY (1993) recorded this taxon from the upper Maastrichtian, from the A. fresvillensis to the base of the A. terminus zones. In Pakistan, FATMI & KENNEDY (1999) assigned the species to the upper Maastrichtian but possibly not uppermost. In Denmark, H. (N.) surya is the only species which can be firmly dated to the Late upper Maastrichtian (BIRKELUND 1993). H. (N.) surya is a cosmopolitan species.
Type s pecies : Ammonites infundibulum D’ORBBIGNY, 1841, p. 131, pl. 39, figs. 4-5, by original designation.
Phyllopachyceras forbesianum (D’ORBIGNY, 1850) Fig. 5 k-l 1846
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Ammonites Royanus D’ORBIGNY. – FORBES, p. 108, pl. 8, fig. 6.
Ammonites from the Maastrichtian Quiriquina Formation in central Chile
191
Fig. 7. Whorl sections of Anagaudryceras and Gaudryceras kayei. a: Anagaudryceras subtilineatum CPUC/Q/CO/3062. b: Anagaudryceras politissimum. CPUC/Q/LT/571. c, d-f: Gaudryceras kayei, c: CPUC/Q/CO/1337, d: GSP 1069 of FATMI & KENNEDY (1999). e: WAM 80.977 of HENDERSON & MCNAMARA (1985). f: Gaudryceras kayei CPUC/Q/SV/1463.
1963
Phyllopachyceras forbesianum (D’ORBIGNY). – JONES, p. 24, pl. 41, figs. 2, 4-6; text-fig. 9. 1970 Phyllopachyceras forbesianum (D’ORBIGNY). – HENDERSON, p. 7, pl. 1, figs. 2, 4, 5 (with additional synonymy). 1985 Partschiceras (Phyllopachyceras) forbesianum (D’ORBIGNY). – HENDERSON & MCNAMARA, p. 43, pl. 1, figs. 4-6; text-fig. 3f. 1986 Partschiceras forbesianum (D’ORBBIGNY). – KENNEDY & SUMMESBERGER, p. 184, pl. 1, figs. 2-3, 6; pl. 5, figs. 3, 6. 1992a Phyllopachyceras forbesianum (D’ORBIGNY). – KENNEDY & HENDERSON, p. 394, pl. 2, figs. 1-12; text-fig. 3c (with additional synonymy). 1993 Phyllopachyceras forbesianum (D’ORBIGNY). – WARD & KENNEDY, p. 17, text-figs. 17.14-17.17, 18.5-18.7. 2004 Phyllopachyceras forbesianum (D’ORBIGNY). – IFRIM et al., p. 1583, pl. 1, figs. 1-4; text-fig. 3B-C.
HENDERSON (1992a: 396, pl. 2, figs. 1-3) from the original type series. M aterial: One well-preserved phragmocone from the Las Tablas section. D es cription: Coiling extremely involute (U/D 0.08) and whorl section inflated, with high expansion rate. Umbilical wall steep. Whorl section wide and subelliptical, with arched flanks and venter. Ornament consists of fine lirae, straight in ventrolateral area and venter and slightly prorsiradiate. Dimensions D CPUC/Q/ LT/248 39.0
Wb
Wh
Wb/Wh U
U/D
18.5
25.0
0.74
0.08
3.0
Remarks : HENDERSON (1970) and KENNEDY & SUMMESBERGER (1986) presented a full discussion and synonymy of this species.
Ty p e : Ammonites forbesianum FORBES, 1846 (pl. 8, fig. 6) was introduced as a new name for Ammonites Royanus D’ORBIGNY, without designation of a holotype. Lectotype is BMNH C51081, subsequently designated by KENNEDY &
O ccur rence: Phyllopachyceras forbesianum is here recorded for the first time from the Quiriquina Formation. The single specimen was found as float in the unit with
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Fig. 8. Suture lines. a: Anagaudryceras subtilineatum (CPUC/Q/CO/3062). b: Anagaudryceras politissimum (CPUC/Q/LT/571).
calcareous sandstone concretions at Las Tablas. Elsewhere, the taxon has been described from the Santonian of Madagascar (COLLIGNON 1956, 1969), the lower Campanian of Spain (WIEDMANN 1962) and from the CampanianMaastrichtian of Japan (MATSUMOTO 1942), Alaska (JONES 1963), New Zealand (MARSHALL 1926; HENDERSON 1970), Austria (KENNEDY & SUMMESBERGER 1986), Antarctica, South Africa and Germany (see KENNEDY & HENDERSON 1992 a). In northeast Mexico, it is recorded from the lower Maastrichtian (IFRIM et al. 2004). It is also known from the upper Maastrichtian of southern India (KENNEDY & HENDERSON 1992a), Western Australia (HENDERSON & MCNAMARA 1985) and the Biscay region (WARD & KENNEDY 1993). Phyllopachyceras forbesianum is considered a cosmopolitan species.
1922 1956 1965 1979 1985
Type: The holotype is the original of KOSSMAT (1895, pl. 19, figs. 1a-c), from the Arialoor Group of Karapady, South India. The lectotype (TM 559) was designated by KENNEDY & KLINGER (1979: 155, text-fig. 3; pl. 14, figs. 3-12).
Suborder Lytoceratina HYATT, 1899 Superfamily Tetragonoidea H YATT, 1900 Family Gaudryceratidae SPATH, 1927 Genus Anagaudryceras SHIMIZU, 1934
M aterial: Three juvenile specimens, all well-preserved phragmocones. D es cription: Coiling extremely evolute and expansion rate low. U/D between 0.48-0.61, decreasing slowly as diameter increases. Umbilicus wide and shallow, with rounded umbilical walls. Whorl section rounded, wider than high, with arched venter and convex flanks (Fig. 7). Juvenile stages characterized mainly by low and strongly inflated whorl section (Fig. 7). Wb/Wh and U/D relationships increase with diameter. Ornament consists of very fine prorsiradiate lirae. Three weak constrictions are present on last whorl, each preceded by a prominent collar. Constrictions strongly prorsiradiate on flanks and venter. Suture line intensely incised. E lanceolate. LB1B slightly asymmetric; divided into auxillary lobes, with biphylloid and triphylloid terminations. LB1/LB2B divided into two
Ty p e s p e c ie s : Ammonites sacya FORBES (1846: 113, pl. 14, fig 9), as designated by SHIMIZU (1934: 67). The genus was discussed by KENNEDY& KLINGER (1979).
Anagaudryceras subtilineatum (KOSSMAT, 1895) Figs. 5g-h, 7a, 8a, 9 1895 1921
Gaudryceras tenuilineatum VAN HOEPEN. – SPATH, p. 117. Anagaudryceras subtilineatum (KOSSMAT). – COLLIGNON, p. 68. Anagaudryceras subtilineatum (KOSSMAT). – HOWARTH, p. 358. Anagaudryceras subtilineatum (KOSSMAT). – KENNEDY & KLINGER, p. 155, pl. 14, figs. 3-12; textfig. 3. Anagaudryceras subtilineatum (KOSSMAT). – HENDERSON & MCNAMARA, p. 45, pl. 2, figs. 3-4; textfig. 4a.
Lytoceras (Gaudryceras) subtilineatum KOSSMAT, p. 123, pl. 19, figs. 1a-c, 2a, b. Gaudryceras tenuilineatum VAN HOEPEN, p. 5, pl. 2, figs. 7-9; text-fig. 2.
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193
Fig. 9. Relationship between Wb/Wh and D of Anagaudryceras of the Quiriquina Formation and other formations. In Anagaudryceras politissimum there is a clear break in ontogeny separating juveniles (D < 40 mm) and adults (D > 40 mm).
Anagaudryceras politissimum (KOSSMAT, 1895) Figs. 5 i-j, 6d, g-h, 7b, 8 b, 9
principal saddles, with simple and biphylloid terminations (Fig. 8). LB2B with biphylloid terminations. LB2/LB3B divided into two main saddles, with simple and biphylloid terminations (Fig. 8). LB3B with simple terminations. Dimensions CPUC/Q/ TO/3235 CPUC/Q/ CO/2332 CPUC/Q/ CO/3062
1895
D
Wb
Wh
Wb/Wh U
U/D
1956
12.0
4.5
2.5
1.80
6.5
0.54
1979
14.0
5.0
3.0
1.66
8.0
0.57
25.0
10.0
7.0
1.43
12.0
0.48
1985 1986
R e ma r k s : Anagaudryceras is more evolutely coiled than Gaudryceras. Lirae are finer and less flexuous (WRIGHT et al. 1996). Coiling is more evolute and the suture line slightly more complex than in A. politissimum (Fig. 8). The ontogenetic development of Wb/Wh and D differ between A. subtilineatum and A. politissimum (Fig. 9), with a slightly wider and lower section in A. subtilineatum. KENNEDY & KLINGER (1979) presented a full discussion of this species.
1993 1999 2004
O c c u r r e n c e : Anagaudryceras subtilineatum is here recorded for the first time for the Quiriquina Formation. Specimens were found at Cocholgüe, Tomé and Lirquén, where they occur in the unit with calcareous sandstone concretions, in the Eubaculites carinatus Zone (Kitchinites (K.) darwini Subzone). A. subtilineatum is known from the ?Campanian of South India, the Santonian or Campanian of Pondoland (KENNEDY & KLINGER 1979) and the upper Maastrichtian of Western Australia (HENDERSON & MCNAMARA 1985). The taxon has an Indo-Pacific distribution.
Lytoceras (Gaudryceras) politissimum KOSSMAT, p. 128, pl. 15, fig. 7a-c. Anagaudryceras politissimum (KOSSMAT). – COLLIGNON, p. 58, pl. 8, fig. 2, 2a, 2b. Anagaudryceras politissimum (KOSSMAT). – KENNEDY & KLINGER, p. 154, pl. 5, fig. 3 (with full synonymy). Anagaudryceras politissimum (KOSSMAT). – HENDERSON & MCNAMARA, p. 46, pl. 1, figs. 9-10; textfig. 4d (with full synonymy). Anagaudryceras cf. politissimum (KOSSMAT). – STINNESBECK, p. 194, pl. 7, fig. 9; pl. 8, fig. 1; textfigs. 18-19. Anagaudryceras politissimum (KOSSMAT). – WARD & KENNEDY, p. 21, pl. 17, figs. 9, 12; pl. 19, figs. 2, 6, 14-15. Anagaudryceras politissimum (KOSSMAT). – FATMI & KENNEDY, p. 646, figs. 4.7-4.8. Anagaudryceras politissimum (KOSSMAT). – IFRIM et al., p. 1590, text-figs. 3I-J, 6D-E, I.
Type: The holotype is the original of KOSSMAT (1895: 128, pl. 15, fig. 7) from South India. M aterial: Five well-preserved phragmocones. D es cription: In juvenile specimens (D < 40 mm) coiling is serpenticone, whorl section subtrapezoidal to rounded with rounded venter, umbilicus wide and with rounded walls. For adult specimens (D > 40 mm), coiling is gradually more evolute in outer whorls and whorl section more
eschweizerbart_xxxx
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C. Salazar et al.
Fig. 10. Relationship between Wb/Wh and D in Gaudryceras kayei. There are marked changes during ontogeny, clearly separating juveniles (D < 100 mm) from adult specimens (D > 100 mm).
cluded here. Suture terminations are more complex than in A. subtilineatum. KENNEDY & KLINGER (1979) presented a full discussion of A. politissimum.
rounded and elliptical, higher than wide, with rounded venter (Fig. 7), shallow umbilicus and with rounded walls. During growth Wb/Wh gradually decreases (1.27 in juveniles to 0.85 in adults) and U/D relationship increases (Fig. 9). Ornament of fine and prorsiradiate lirae, convex on umbilical shoulder and projected on flanks and venter. Between 3 and 5 prorsiradiate constrictions on last whorl. Suture line of rounded elements. E lanceolate. E/L divided into eight auxiliary saddles with simple and biphylloid terminations. L as deep as E and with biphylloid and triphylloid terminations (Fig. 8). Dimensions CPUC/Q/ TO/3512 CPUC/Q/ LT/3593 CPUC/Q/ CO/3594 CPUC/Q/ LT/3592 CPUC/Q/ LT/571
D
Wb
Wh
Wb/Wh U
U/D
19.5
7.0
5.5
1.27
10.5
0.53
24.0
8.0
6.5
1.23
12.0
0.50
(27.0) 9.0
8.5
1.05
13.0
(0.48)
28.0
9.0
9.5
0.95
13.0
0.46
81.0
28.0
33.0
0.85
29.0
0.36
O ccur rence: In the Quiriquina Formation (sections Las Tablas, Cocholgüe and Tomé). A. politissimum occurs in the Eubaculites carinatus Zone, in the units with coquina layers and with calcareous sandstone concretions. The taxon is known from the Turonian-Santonian of South India (KOSSMAT 1895), Santonian of Zululand (KENNEDY & KLINGER 1979), Maastrichtian of Madagascar (COLLIGNON 1956) and lower Maastrichtian (planktic foraminiferal Zone CF 7) of northeastern Mexico (IFRIM et al. 2004). Upper Maastrichtian occurrences are reported from Pakistan (FATMI & KENNEDY 1999), Western Australia (HENDERSON & MCNAMARA 1985) and the Biscay region (in the A. mayaroensis Zone; WARD & KENNEDY 1993). Anagaudryceras politissimum is a cosmopolitan species, but with a strong Indo-Pacific dominance.
Genus Gaudryceras DE GROSSOUVRE, 1894 Type s pecies : Ammonites mitis (VON HAUER 1866: 305, pl. 2, figs. 3-4) by subsequent designation of BOULE et al. (1906: 183). This genus was revised by HENDERSON & MCNAMARA (1985), who considered Vertebrites as junior synonym of Gaudryceras.
R e ma r k s : Coiling in A. politissimum is more involute and the whorl section higher than in A. subtilineatum (Fig. 7). The ontogenetic curves of the two species also differ clearly (Fig. 9). The new material and data allow material described in open nomenclature by STINNESBECK (1986) to be in-
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195
Fig. 11. a-b: Gaudryceras kayei (FORBES, 1846), CPUC/Q/SV/1462, x0.5. a: coated. b: uncoated.
Gaudryceras kayei (FORBES, 1846) Figs. 5a-f, 7c-f, 10, 11 a-b, 13 d-e 1846 1895 1904 1906 1971 1979 1985
Gaudryceras (Vertebrites) kayei (FORBES). – STINp, 198, pl. 8, figs. 2-3, text-fig. 21. 1992a Gaudryceras kayei (FORBES). – KENNEDY & HENDERSON, p. 402, pl. 5, figs. 19-22, 24, 28-41; textfig. 3d. 1993 Gaudryceras kayei (FORBES). – WARD & KENNEDY, p. 17, text-figs. 17.11, 18.11-18.12, 18.15. 1999 Gaudryceras kayei (FORBES). – FATMI & KENNEDY, p. 644, figs. 5.1-5.2, 16.2. 2004 Gaudryceras kayei (FORBES). – IFRIM et al., textfigs. 3L-N, 5D, 6A-C, H.
1986
NESBECK,
Ammonites kayei FORBES, p. 101, pl. 8, fig. 3. Lytoceras kayei (FORBES). – STEINMANN, p. 86, pl. 15, fig. 5. Lytoceras kayei (FORBES). – WILCKENS, p. 188. Gaudryceras kayei (FORBES). – WOODS, p. 335, pl. 41, fig. 8; pl. 42, fig. 1. Vertebrites kayei (FORBES). – COLLIGNON, p. 2, pl. 640, fig. 2362. Vertebrites kayei (FORBES). – KENNEDY & KLINGER, p. 160, fig. 5; pl. 14, fig. 2 (with full synonymy). Gaudryceras kayei (FORBES). – HENDERSON & MCNAMARA, p. 46, pl. 1, figs. 9-10; text-fig. 4d.
Type: Lectotype is BMNH C51050, the original of FORBES (1846, pl. 8, fig 3), by subsequent designation of MATSUMOTO & YOSHIDA (1979: 70).
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C. Salazar et al.
upper part of the section. The small specimens here recorded from the Lirquen and Tomé sections are in the Eubaculites carinatus Zone, in the unit with calcareous sandstone concretions. STINNESBECK (1986) recorded Gaudryceras kayei from the Las Tablas and Cocholgüe sections, from the unit with calcareous sandstone. Elsewhere, Gaudryceras kayei is known from the SantonianCampanian of South Africa (KENNEDY & KLINGER 1979), the lower Maastrichtian of northeast Mexico (IFRIM et al. 2004), upper Maastrichtian of South India (KENNEDY & HENDERSON 1992a), Pakistan (FATMI & KENNEDY 1999), Western Australia (HENDERSON & MCNAMARA 1985) and the Biscay region (WARD & KENNEDY 1993). G. kayei is considered to be a cosmopolitan species.
M a te r ia l: Six well-preserved specimens. D e s c r ip tio n : In juvenile stages (D < 100 mm) whorl section low and more rectangular than rounded, with straight to slightly convex flanks and rounded venter (Fig. 7). Coiling depressed and characterized as more involute than in later growth stages (Fig. 10). Umbilicus narrow with rounded umbilical walls. Ornament of dense and fine prorsiradiate and slightly flexuous lirae. 3 to 4 weak constrictions parallel to lirae. In adult stages (D > 100 mm) whorl section rounded-rectangular, with rounded flanks and wide venter (Fig. 6). Last whorl high and roundedrectangular, with slightly convex flanks and rounded venter. Maximum whorl width reached at mid-flank. Coiling extremely evolute, with low expansion rate (Fig. 10). Umbilicus shallow and wide (U/D: 0.26-0.28), with rounded umbilical walls. Ornament consists of dense and fine, prorsiradiate and slightly flexuous lirae. 6 to 7 weak constrictions on last whorl and parallel to lirae. Dimensions CPUC/Q/ LI/400 CPUC/Q/ TO/3322 CPUC/Q/ CO/1337 CPUC/Q/ SV/1463
CPUC/Q/ SV/1462 CPUC/Q/ SV/2315
D
Wb
Wh
Wb/Wh U
U/D
14.0
5.0
3.0
1.66
8.5
0.61
16.5
6.0
3.5
1.71
9.0
0.54
34.0
10.5
11.0
0.95
16.0
0.47
235.0 100.0 113.0 0.88 230.0 96.0 118.0 0.81 134.0 50.0 52.0 0.96
65.0 62.0 42.0
0.28 0.27 0.31
246.0 103.0 135.0 0.76 170.0 56.0 40.0 0.74
65.0 46.0
0.26 0.32
270.0 102.0 125.0 0.82
75.0
0.28
Genus Zelandites MARSHALL, 1926 Type s pecies : Zelandites kaiparaensis MARSHALL, 1926, p. 147, pl. 19, fig. 9; pl. 31, figs. 1-2, by original designation. This genus was discussed by KENNEDY & KLINGER (1979).
Zelandites varuna (FORBES, 1846) Figs. 6 b-c, e-f, i, 12 1846 1895
Ammonites varuna FORBES, p. 107, pl. 8, fig. 5. Lytoceras (Gaudryceras) varuna (FORBES). – KOSSMAT, p. 161, pl. 16, fig. 4; pl. 17, fig. 8. 1938 Zelandites varuna (FORBES) var. japonica MATSUMOTO, p. 140, pl. 14, figs. 1-7; text-fig. 1. 1956 Zelandites varuna (FORBES). – COLLIGNON, p. 67. 1979 Zelandites varuna (FORBES). – KENNEDY & KLINGER, p. 296, figs. 30-31. non 1986 Zelandites varuna (FORBES). – MACELLARI, p. 14, figs. 11.11-11.12, 12. 1986 Zelandites varuna (FORBES). – STINNESBECK, p. 195, pl. 8, figs. 5-6; text-fig. 20. 1992a Zelandites varuna (FORBES). – KENNEDY & HENDERSON, p. 404, pl. 5, figs. 13-15; pl.17, figs. 2-3. 1994 Zelandites varuna (FORBES). – YAZIKOVA, p. 289, pl. 1, fig. 8. 2004 Zelandites varuna (FORBES). – IFRIM et al., p. 1592, text-figs. 3O-P, 6F-G, J.
R e ma r k s : Gaudyceras is more evolute and coiling more serpenticone than in Anagaudryceras, with low whorls and more flexuous lirae. G. kayei differs from A. politissimum and A. subtilineatum by stronger lirae. See HENDERSON & MCNAMARA (1985) and KENNEDY & HENDERSON (1992a) for reviews of this species. Gaudryceras kayei has been described only from specimens with diameters of < 60 mm (KENNEDY & KLINGER 1979; HENDERSON & MCNAMARA 1985; STINNESBECK 1986; WARD & KENNEDY 1993; FATMI & KENNEDY 1999; IFRIM et al. 2004). Several of our specimens have much larger diameters (D 235-270 mm) than the typical G. kayei described from the Quiriquina and other formations (Fig. 10). These adult specimens are proportionally wider and slightly more involute. G. kayei is characterized by marked changes throughout ontogeny and a gradual decrease of the Wb/Wh (1.71 in juveniles to 0.74 in adults) and U/D relationships (Fig. 10). Our material confirms that HENDERSON & MCNAMARA (1985) were right to consider Vertebrites as a junior synonym of Gaudryceras.
Type: Lectotype is BMNH C51059, designated by KENNEDY & HENDERSON (1992a, p. 404) from the originals of FORBES (1846). M aterial: 11 well-preserved specimens, two retaining the body chamber. D es cription: Coiling involute with moderate expansion rate. Umbilicus narrow and shallow. Marked changes observed during ontogeny. U/D (13-20 %) decreases slightly with increasing diameters (from 10 to 46 mm), whereas Wb/Wh increases from 0.6 to 0.8 (Fig. 12). Whorl section trapezoidal in earliest stages (D < 11 mm) and gradually changes to trapezoidal-discoidal in later stages (D >11 mm).
O c c u r r e n c e : The large specimens of Gaudryceras kayei here described have been found at San Vicente, from the
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197
Fig. 12. Zelandites varuna (FORBES, 1846). Relationship between Wb/Wh and D. Note that a clear break exists between juvenile (D < 11 mm) and adult (D > 11 mm) specimens.
Umbilical shoulders rounded. Flanks convex and slightly convergent, and venter narrowly rounded. Ornament consists of dense and fine flexuous lirae, prorsiradiate on dorsolateral area, convex at mid-flank and rectiradiate on ventrolateral area. Specimens CPUC/Q/LV/3591 and CPUC /Q/LI/3481 preserve body chamber with two deep and strong constrictions, parallel to lirae (Fig. 6i). Dimensions CPUC/Q/ LI/3486 CPUC/Q/ TO/3237 CPUC/Q/ CO/2916 CPUC/Q/ LI/3485 CPUC/Q/ CO/2480 CPUC/Q/ CO/3163 CPUC/Q/ CO/3446 CPUC/Q/ TO/3317 CPUC/Q/ LT/3590 CPUC/Q/ LI/3481 CPUC/Q/ LV/3591
D
Wb
Wh
Wb/Wh U
U/D
10.0
4.0
5.0
0.80
2.0
0.20
15.5
5.0
7.0
0.71
3.0
0.19
17.0
6.0
9.0
0.66
3.0
0.18
22.0
7.0
11.0
0.64
3.0
0.14
22.0
7.0
11.0
0.64
3.5
0.16
22.0
7.5
12.0
0.63
3.0
0.14
24.0
8.5
12.5
0.68
3.0
0.13
26.0
9.0
12.0
0.75
5.0
0.19
27.0
8.0
13.0
0.62
4.0
0.15
30.0 42.0
9.0
15.0
0.60
5.0 5.1
0.17 0.12
32.0 46.0
9.0
15.0
0.60
4.5 4.14
0.14 0.09
Remarks : Quiriquina specimens correspond to Z. varuna as described by KENNEDY & HENDERSON (1992a). It is important to note that marked changes are observed in the ontogeny of this species, Wb/Wh and U/D decrease strongly between juvenile and adult specimens (Fig. 12). Z. varuna described from Antarctica by MACELLARI (1986) differs by a much lower Wb/Wh than observed in the Quiriquina specimens or the Indian type material (Fig. 12). It should therefore be referred to another taxon. O ccur rence: In the Quiriquina Formation (sections Las Tablas, Los Viejos, Cocholgüe, Tomé and Lirquén), Zelandites varuna is present in the unit with calcareous sandstone concretions, in the Eubaculites carinatus Zone (mainly in the Kitchinites (K.) darwini subzone). Z. varuna is known from the Maastrichtian of Japan (MATSUMOTO 1938) and Madagascar (COLLIGNON 1956), the lower Maastrichtian of Northeast Mexico (IFRIM et al. 2004), Upper Maastrichtian of Eastern Russia (YAZIKOVA 1994). In South India, the species probably belongs to the lower part of the A. mayaroensis zone (KENNEDY & HENDERSON 1992a). Z. varuna is considered to be an Indo-Pacific species. The occurrence in Antarctica of Z. varuna in the uppermost ammonite-bearing sediment horizon of the Pachydiscus ultimus zone remains doubtful (MACELLARI 1986; ZINSMEISTER et al. 1989).
Family Tetragonitidae H YATT, 1900 Genus Pseudophyllites KOSSMAT, 1895 Type s pecies : Ammonites indra FORBES, 1846, p. 105, pl. 11, fig. 7, by original designation
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C. Salazar et al.
Fig. 13. a-c: Pseudophyllites indra (FORBES, 1846), a-b: CPUC/Q/LT/130, x0.75; c: CPUC/Q/CO/3296, x0.75. d-e: Gaudryceras kayei (FORBES, 1846), CPUC/SV/Q/1463, x0.5 uncoated.
Pseudophyllites indra (FORBES, 1846) Figs. 13 a-c 1846 1895
1963 1971
Ammonites indra FORBES, p. 105, pl. 11, fig. 7. Pseudophyllites indra (FORBES). – KOSSMAT, p. 137, pl. 16, figs. 6-9; pl. 17, figs. 6-7; pl. 18, fig. 3.
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Pseudophyllites indra (FORBES). – JONES, p. 25, pl. 7, figs. 6-7; pl. 8; pl. 29, figs. 7-12; text-fig. 10. Pseudophyllites indra (FORBES). – COLLIGNON, p. 2, pl. 639, fig. 2355; pl. 640, fig. 2363; p. 81, pl. 649, fig. 2355.
Ammonites from the Maastrichtian Quiriquina Formation in central Chile
199
Fig. 14. Whorl sections of. a: K. darwini CPUC/Q/LT/2020. b: K. darwini, OSU 38370 of Macellari (1986). c: Kitchinites vicentensis n. sp., CPUC/Q/SV/1448. d: Kitchinites ifrimae n.sp., CPUC/Q/CO/3161.
rounded. Ornament consists of dense and fine lirae curved forwards and prorsiradiate on umbilical shoulders and inner flank, convex on ventrolateral area and gently concave on the venter.
1977
Pseudophyllites indra (FORBES). – KENNEDY & KLINGER, p. 182, text-figs. 19-22 (with additional synonymy). 1985 Pseudophyllites indra (FORBES). – HENDERSON & MCNAMARA, p. 50, pl. 2, figs. 7- 8; pl. 3, figs. 4-5; text-fig. 5a-d. 1986 Pseudophyllites indra (FORBES). – STINNESBECK, p. 199, pl. 8, fig. 4. 1986 a Pseudophyllites indra (FORBES). – KENNEDY, p, 19, pl. 1, fig. 1-5; text-fig. 4e, 5a, 6a-e (with additional synonymy). 1991 Pseudophyllites indra (FORBES). – COBBAN & KENNEDY, p. E2, pl. 1, figs. 1-5. 1992a Pseudophyllites indra (FORBES). – KENNEDY & HENDERSON, p. 398, pl. 3, figs. 7-9, 13-27; pl. 4, figs. 1-3. 1993 Pseudophyllites indra (FORBES). – WARD & KENNEDY, p. 22, text-figs. 17.8, 18.9-18.10, 19.7, 19.9, 19.13, 21.1-21.2, 22.1-22.2, 27.6. 1995 Pseudophyllites indra (FORBES). – COBBAN & KENNEDY, p. 4, figs. 2.1-2.4, 2.10 (with additional synonymy). 2004 Pseudophyllites indra (FORBES); IFRIM et al., p. 1587, text-figs. 3H, 5A-B.
Dimensions CPUC/Q/ CO/3595 CPUC/Q/ CO/3296 CPUC/Q/ LT/130 CPUC/Q/ CO/530
D
Wb
Wh
Wb/Wh U
U/D
-
28.0
-
-
10.0
-
(82.0) (45.0) (43.0) (1.05)
17.0
(0.21)
96.0
45.0
54.0
0.83
17.0
0.18
-
61.0
64.0
0.95
23.0
-
Remarks: According to HENDERSON & MCNAMARA (1985), P. indra is distinguished from other species of the genus by a flat umbilical wall and a lanceolate external saddle. WARD & KENNEDY (1993) presented a full discussion of this species. Occur rence. In the Quiriquina Formation (sections Las Tablas and Cocholgüe), this taxon is present in the unit of calcareous sandstone concretions, in the Eubaculites carinatus Zone (mainly in the Kitchinites (K.) darwini subzone). P. indra is known from the upper Santonian to Maastrichtian (see WARD and KENNEDY 1993). In northeast Mexico, P. indra was recorded by IFRIM et al. (2004) from the lower Maastrichtian planktic foraminiferal biozone CF7 of LI et al. (1999). In the Biscay region, this taxon has been recorded from the upper Maastrichtian, in the A. fresvillensis and A. terminus zones (WARD & KENNEDY 1993). P. indra is a cosmopolitan taxon.
Ty p e : Lectotype is BMNH C51068, the original of FORBES (1846, pl. 11, fig. 7a, b), designated by Kennedy & KLINGER (1977). M a te r ia l: Four specimens, two of which correspond to complete and two to fragmentary phragmocones. D e s c r ip tio n : Coiling involute with fast rate of expansion. Umbilicus narrow (U/D 0.18-0.21) and deep. Whorl section
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C. Salazar et al.
Fig. 15. Relationship between Wb/Wh and D in Kitchinites darwini from the Quiriquina Formation and Antarctica, as well as Kitchinites laurae from Antarctica. Note that specimens of K. darwini from Antarctica are clearly separated by their thicker shell.
M aterial: 30 specimens, 12 of which are fragments. Only the best-preserved specimens were measured and listed. D es cription: Coiling evolute, umbilicus wide (U/D 0.290.40), increasing during growth. Whorl section discoidal, with vertical and slightly rounded umbilical shoulder. Flanks convergent and venter narrowly rounded (Fig. 14 a). In juvenile specimens (D < 56 mm), ornament of 3 to 4 constrictions; prorsiradiate and slightly concave. In larger specimens (D > 60 mm), approximately 80 thick ventral ribs present as well as 6-7 deep constrictions accompanied on both sides by elevated rims. Constrictions prorsiradiate and projected ventrolaterally; 1-2 ribs adjacent to constrictions cut off by constrictions.
Suborder Ammonitina H YATT, 1889 Superfamily Desmoceratoidea ZITTEL, 1895 Family Desmoceratidae ZITTEL, 1895 Subfamily Puzosiinae SPATH, 1922 Genus Kitchinites SPATH, 1922 Ty p e s p e c ie s : Holcodiscus pondicherryanus KOSSMAT, 1897, by original designation
Kitchinites darwini (STEINMANN, 1895) Figs. 14 a, 15, 16 a-f 1895
Puzosia darwini PHILIPPI. – STEINMANN, p. 73, pl. 5, fig. 3 a, b. non 1966 Kitchinites darwini (STEINMANN). – HOWARTH, p. 59, pl. 2, fig. 3. non 1976 Kitchinites darwini (STEINMANN). – DEL VALLE et al., p. 5, pls. 1-8. non 1986 Kitchinites (Kitchinites) darwini (STEINMANN). – MACELLARI, p. 19, figs. 14.2-14.3, 17.1-17.3, 18, 19.1, 22.2. 1986 Kitchinites (Kitchinites) darwini darwini (STEINMANN). – STINNESBECK, p. 209, pl. 10, fig. 7; pl. 11, fig. 1.
Dimensions CPUC/Q/ CO/3588 CPUC/Q/ CO/2218 CPUC/Q/ CO/3242 CPUC/Q/ CO/3561 CPUC/Q/ CO/2216 CPUC/Q/ CO/2327 CPUC/Q/ CO/214 CPUC/Q/ LM/3240
Ty p e : Lectotype, IPB No. 262 designated by STINNESBECK (1986, p. 209, pl. 10, fig. 7) is from Quiriquina Formation, Chile.
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D
Wb
Wh
Wb/Wh U
U/D
40.0
10.0
16.0
0.63
13.0
0.33
45.0
(10.0) 18.0
(0.55)
14.0
0.31
46.0
12.0
19.0
0.63
18.0
0.39
50.0
-
22.0
-
16.0
0.32
51.0
12.0
21.0
0.56
18.0
0.35
53.0
12.0
21.0
0.57
18.0
0.34
54.0
14.0
20.0
0.70
21.0
0.37
56.0
(14.0) 22.0
0.64
21.0
0.38
Ammonites from the Maastrichtian Quiriquina Formation in central Chile
201
Fig. 16. a-f: Kitchinites darwini (STEINMANN, 1895). a-b: CPUC/Q/CO/214, x1; c-d: CPUC/Q/PP/3240, x1; e: CPUC/Q/LT/534, x1; f: CPUC/Q/LT/3586, x1.
CPUC/Q/ CO/2923 CPUC/Q/ CO/3136 CPUC/Q/ CO/3057 CPUC/Q/ LT/1882 CPUC/Q/ CO/20 CPUC/Q/ LT/3137 CPUC/Q/ LT/2342
73.5
-
27.5
-
26.5
0.36
-
18.0
31.0
0.58
-
-
(76.0) 18.0
33.0
0.54
22.0
(0.29)
-
31.0
53.0
0.58
-
-
86.0
33.0
-
-
31.0
0.36
89.0
21.0
37.0
0.57
35.0
0.39
91.0
-
-
-
36.0
0.40
CPUC/Q/ LT/3586 CPUC/Q/ LT/3496 CPUC/Q/ LT/534 CPUC/Q/ LT/2020 CPUC/Q/ CO/363 CPUC/Q/ CO/3135 CPUC/Q/ CO/3363
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94.0
21.0
36.0
0.58
38.0
0.40
95.0
-
39.0
-
38.0
0.40
106.0 21.0
41.0
0.51
41.0
0.39
107.0 25.0
43.0
0.58
36.0
0.34
115.0 -
43.0
-
42.0
0.37
-
30.5
51.0
0.59
-
-
-
(37.0) 64.0
(0.57)
-
-
202
C. Salazar et al.
Fig. 17. a-c: Kitchinites vicentensis n. sp. a-b: CPUC/Q/SV/1449, x0.5; c: CPUC/Q/SV/1450, x0.4.
recorded from the unit of calcareous sandstone concretions in the Eubaculites carinatus Zone.
R e ma r k s : Kitchinites darwini described by STEINMANN (1895) from the Quiriquina Formation is characterised by an inflated whorl section whereas specimens described by
Kitchinites vicentensis n. sp. Figs. 14 c, 17a-c
STINNESBECK (1986) as well as the material presented here are much thinner. Specimens from Antarctica described as K. (K.) darwini by HOWARTH (1966) and DEL VALLE et al. (1976) also present a more inflated whorl section and a widely rounded venter (cf. Fig. 15). They appear to be related to K. (K.) laurae MACELLARI 1986. Specimens of K. darwini from the Quiriquina Formation described here also differ from Antarctic material of K. (K.) darwini described by MACELLARI (1986) which are more inflated as well (Fig. 14). Consequently, these Antarctic specimens of Kitchinites (K.) darwini differ from specimens described herein by their more inflated whorl section (Fig. 15). They should by separated from K. darwini based on their thicker whorl section. Kitchinites ifrimae n. sp. differs in having fine flexuous flank ribs and a lower number of constrictions on the last whorl, usually 1 or 2.
Types: Holotype: CPUC/Q/SV/1449, an internal mould of a complete phragmocone. Paratypes: CPUC/Q/SV/1450 and CPUC/Q/SV/1480 internal moulds of complete phragmocones; CPUC/Q/SV/1448 is a fragmentary internal mould of phragmocone. Etymology: After the city of San Vicente (west of Talcahuano) where the type material was found. D iagnos is : Whorl section discoidal and venter archedshaped to narrowly rounded. Shell smooth, except for 3-4 strong constrictions on last half of whorl, and 2-3 constrictions on internal whorls, prorsiradiate and sigmoidal, convex on dorsolateral area and concave on ventrolateral area and venter.
O c c u r r e n c e : In the Quiriquina Formation (sections Las Tablas, Cocholgüe and Santa Sabina), Kitchinites darwini is
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203
Fig. 18. a-d: Kitchinites ifrimae n. sp., a-b: CPUC/Q/CO/534, x1; c-d: CPUC/Q/CO/3161, x1.
3-5 rectiradiate constrictions on the last whorl. Kitchinites ifrimae n. sp. differs from Kitchinites vicentensis n. sp. by its arched venter (Fig. 14), fine ribs and only 1-2 weak constrictions on the last whorl.
D e s c r ip tio n : Coiling evolute to moderately involute, umbilicus narrow (U/D 0.22-0.24) and with high expansion rate. Whorl section compressed, whorl discoidal and umbilical wall steep and rounded. Flanks convex, venter arched-shaped to narrowly rounded. Maximum width on dorsolateral area (Fig. 14c). 3-4 strong constrictions on last half of whorl, prorsiradiate and sigmoidal on dorsolateral area and concave on ventrolateral area and venter. Dimensions CPUC/Q/ SV/1448 CPUC/Q/ SV/1480 CPUC/Q/ SV/1450 CPUC/Q/ SV/1449
D
Wb
Wh
Wb/Wh U
U/D
-
39.0
72.0
0.54
-
-
(227.0) (60.0) 108.0 (0.55)
50.0
(0.22)
228.0 (71.0) 110.0 (0.64)
52.0
0.22
229.0 73.0
54.0
0.24
114.0 0.64
O ccur rence: Kitchinites vicentensis n. sp. occurs at San Vicente in the unit of yellow sandstone (Baculites anceps Zone).
Kitchinites ifrimae n. sp. Figs. 14 d, 18 a-d 1986
Kitchinites (Neopuzosia) sp. – STINNESBECK, p. 212, pl. 11, figs. 2-3.
Ty p e s : Holotype: CPUC/Q/CO/3161, a well-preserved phragmocone. Paratypes: CPUC/Q/CO/534 a well-preserved phragmocone, CPUC/Q/CO/35 and CPUC/Q/CO/ 2917 all fragment any specimens.
R e ma r k s : K. darwini differs from Kitchinites vicentensis n. sp. by a lanceolate whorl section, a narrowly-arched venter (Fig. 14), strong ventrolateral ribs and a higher number of strong constrictions (5-7 on the last whorl). Kitchinites spathi (compare HENDERSON & MCNAMARA 1985) differs from Kitchinites vicentensis n.sp. by more convex flanks, a rounded venter and strong ventral ribs. K. laurae (compare MACELLARI 1986) is distinguished by a more inflated whorl section and wider venter (Fig. 13). It has weak ribs and
Etymology: Species dedicated to CHRISTINA IFRIM in recognition of her assistance and helpful comments on Maastrichtian ammonite taxonomy. Diagnosis: Whorl discoidal with venter arched-shaped. Faint fine ribs on umbilical area and flanks; progressively thickening towards ventral area. 1-4 weak constrictions on last whorl, prorsiradiate and flexuous.
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Fig. 19. Kossmaticeras (Natalites) erbeni from the Quiriquina Formation. Relationship between Wb/Wh and D.
Family Kosmaticeratidae SPATH, 1922 Subfamily Kossmaticeratinae SPATH, 1922 Genus Kossmaticeras DE GROSSOUVRE, 1901 Subgenus Natalites COLLIGNON, 1954
D e s c r ip tio n : Coiling evolute and whorl section compressed. Umbilicus narrow. Umbilical wall straight to slightly rounded. Flanks subparallel to slightly convex (Fig. 14 d). Venter narrowly-arched. Approximately 40 ribs present on last half whorl, prorsiradiate and flexuous, weak on flanks and progressively thicker towards venter. 1-4 weak, prorsiradiate and flexuous constrictions present on last whorl. Dimensions CPUC/Q/ CO/3161 CPUC/Q/ CO/534 CPUC/Q /CO/2917 CPUC/Q/ CO/35
D
Wb
Wh
Wb/Wh U
U/D
75.0
15.0
27.0
0.57
28.0
0.37
90.0
20.0
37.5
0.53
27.0
0.30
94.0
22.0
42.0
0.52
39.0
0.42
96.5
19.0
39.5
0.48
28.5
0.30
Type species: Madrasites natalensis SPATH, 1922, p. 134, by original designation.
Kossmaticeras (Natalites) erbeni STINNESBECK, 1986 Figs. 19, 20 a-g, 21a 1986 Kossmaticeras (Natalites) erbeni STINNESBECK, p. 213, pl. 12, fig. 1; pl. 13, figs. 4-5. Type: Holotype is IPB CO/1, from the Quiriquina Formation at Cocholgüe, Chile. M aterial: Nine well-preserved specimens and a fragment of the phragmocone.
R e ma r k s : K. darwini differs from Kitchinites ifrimae n. sp. by a discoidal whorl, narrowly rounded venter (Fig. 14), strong ribs on the ventral area, and by more (6-7) constrictions on the last whorl. K. laurae MACELLARI, 1986 differs by a more inflated whorl section, a wider venter, and by 3-5 rectiradiate constrictions. Kitchinites spathi (see HENDERSON & MCNAMARA 1985) presents convex flanks, a discoidal whorl, rounded venter, ribs and weak constrictions.
D es cription: Coiling evolute with low expansion rate, U/D 0.29-0.51. Whorl section rounded in younger stages and oval-subrectangular in adults. In consequence, ratio Wb/Wh presents strong changes during ontogeny (Fig. 19). In young specimens, umbilical shoulder rounded and flanks convex. In adult stages (D > 40 mm), umbilical shoulder straight and slightly rounded and flanks straight. The venter is rounded. 9-13 rounded umbilical tubercles present per half whorl. Each tubercle gives rise to 2-4 ribs, inflated, prorsiradiate and tenuously concave on umbilical shoulder.
O c c u r r e n c e : Kitchinites ifrimae n. sp. is present at Cocholgüe in the unit of calcareous sandstone concretions, in the Eubaculites carinatus Zone.
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205
Fig. 20. a-g: Kossmaticeras (Natalites) erbeni STINNESBECK, 1986. a-b: CPUC/Q/LT/3599, x2; c-d: CPUC/Q/TO/3644, x 2; e-g: CPUC/Q/SV/3589, x0.5.
On dorsolateral area, ribs rectiradiate, changing to prorsiradiate and concave on mid-flank. Young specimens present 4 prorsiradiate constrictions not seen in adults. Dimensions CPUC/Q/ TO/3233 CPUC/Q/ LT/3600 CPUC/Q/ CO/3447 CPUC/Q/ LT/3599
D
Wb
Wh
Wb/Wh U
U/D
12.0
5.0
5.0
1.00
5.0
0.42
18.0
8.0
6.0
1.36
8.0
0.44
19.0
7.0
8.0
0.87
8.0
0.42
21.0
9.0
7.0
1.28
7.5
0.35
CPUC/Q/ TO/3644 CPUC/Q/ TO/3110 CPUC/Q/ SV/3589 CPUC/Q/ LT/3575
21.0
10.0
8.5
1.17
7.0
0.33
29.0
7.0
9.0
0.77
15.0
0.51
160.0 51.0
65.0
0.78
46.0
0.29
-
140.0 -
-
-
-
Remarks : Kossmaticeras (Natalites) erbeni is characterised by a rounded to oval-subrectangular whorl section, convex flanks, umbilical tubercles with groups of 2-4 ribs, and in younger stages prorsiradiate constrictions. STINNESBECK
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C. Salazar et al.
Fig. 21. a: Kossmaticeras (Natalites) erbeni STINNESBECK, 1986, CPUC/Q/LT/3575, x0.2. b: Grossouvrites gemmatus (HUPE, 1854), CPUC/Q/SV/2316, x0.5.
non 1909 Kossmaticeras (Grossouvrites) gemmatus (HUPÉ). – KILIAN & REBOUL, p. 38, pl. 17, figs. 1-3. 1930 Kossmaticeras (Grossouvrites) gemmatus (HUPÉ). – WETZEL, p, 83, pl. 13, fig. 1. non 1953 Grossouvrites gemmatus (HUPÉ). – SPATH, p. 29, pl. 5, fig. 1. non 1958 Grossouvrites gemmatus (HUPÉ). – HOWARTH, p. 12, pl. 2, fig. 4. ?1965 Grossouvrites gemmatus (HUPÉ). – HÜNICKEN, p. 77, pl. 6, figs. 1-2; pl. 7, figs. 8-9. non 1984 Grossouvrites gemmatus (HUPÉ). – OLIVERO, p. 73, pl. 2, figs. 1-2. non 1986 Grossouvrites gemmatus (HUPÉ). – MACELLARI, p. 43, figs. 33.1-33.3, 35. 1985 Grossouvrites gemmatus (HUPÉ). – HENDERSON & MCNAMARA, p. 66, pl. 5, figs. 1-7. 1986 Grossouvrites gemmatus (HUPÉ). – STINNESBECK, p. 217, pl. 12, fig. 3; pl. 13, fig. 1.
(1986) presented a full description and discussion of this species. O c c u r r e n c e : In the Quiriquina Formation (sections Las Tablas, Cocholgüe, Tomé and San Vicente), this taxon has been recorded from the unit of calcareous sandstone concretions and coquina layers, in the Eubaculites carinatus Zone. K. (N.) erbeni is only known from central Chile.
Genus Grossouvrites KILIAN & REBOUL, 1909 Ty p e s p e c ie s : Grossouvrites gemmatus (HUPÉ, 1854), by monotypy.
Grossouvrites gemmatus (HUPÉ, 1854) Figs. 21b, 22 b; 23, 24 b-e 1854 1895
M aterial: Five specimens, four well-preserved and a fragment of the phragmocone.
Ammonites gemmatus HUPÉ in GAY, p. 35, pl. 1, fig. 3. Holcodiscus gemmatus (HUPÉ). – STEINMANN, p. 68, pl. 6, fig. 1.
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207
Fig. 22. Whorl sections in Grossouvrites. a: Grossouvrites joharae n. sp., CPUC/Q/LT/100. b: Grossouvrites gemmatus, CPUC/Q/LT/3580. c: Grossouvrites gemmatus, specimen of STEINMANN (1895). d: Grossouvrites gemmatus, OSU 38412 of MACELLARI (1986).
scribed by MACELLARI (1986) have a wider umbilicus (U/D 0.15-0.17), rectiradiate ribs, a more inflated whorl section (Wb/Wh 0.625-0.83) and more convex flanks (Fig. 22). Their ratio between Wb/Wh and D is larger than in the type G. gemmatus from the Quiriquina Formation (Fig. 23). In consequence, the Antarctic material described as G. gemmatus corresponds to Grossouvrites joharae n. sp. as discussed below. We also refer specimens published by KILIAN & REBOUL (1909), SPATH (1953), HOWARTH (1958) and MACELLARI (1986) to this new species (see below). The Wb/Wh to D ratio in G. gemmatus from the Miria Formation (HENDERSON & MCNAMARA 1985) agrees with specimens from the Quiriquina Formation (Fig. 23), but the Australian material has a wider umbilicus, a more rounded venter and constrictions in juvenile stages. Considering these differences, the Miria specimens of G. gemmatus may correspond to another subspecies.
D e s c r ip tio n : Coiling evolute and compressed (U/D 0.190.21). Whorl section discoidal, higher than wide and venter rounded to sharpened (Fig. 22). Umbilical border straight and vertical, flanks straight and subparallel. Wb/Wh ratio decreases as diameter increases (Fig. 23). 10-11 rounded umbilical tubercles present per half whorl, each giving rise to 2-3 equidistant ribs. Additional rib of similar size inserted between each primary rib, initiating near mid-flank and crossing venter. In consequence, 35-40 fine dense and slightly flexuous ribs present on half whorl, prorsiradiate on dorsolateral area and slightly concave; on mid-flank more concave and inclined towards aperture. Dimensions CPUC/Q/ LT/276 CPUC/Q/ LT/3580 CPUC/Q/ SV/2318 CPUC/Q/ LT/131 CPUC/Q/ SV/2316
D
Wb
Wh
Wb/Wh U
U/D
78.0
27.0
38.0
0.71
16.0
0.21
112.0 36.0
56.0
0.64
22.0
0.19
158.0 (38.0) (59.0) (0.64)
19.0
0.12
-
-
-
51.0
0.23
40.0
55.0
0.72
218.0 (51.0) 102.0 (0.50)
O ccur rence: In the Quiriquina Formation, Grossouvrites gemmatus is recorded from the Eubaculites carinatus and Baculites anceps zones. At Las Tablas, the taxon was registered in the unit with coquina layers and the lower part of the unit with calcareous sandstone concretions; specimens from San Vicente were found in the unit of calcareous sandstone. Grossouvrites gemmatus in Australia was recorded from the upper Maastrichtian (HENDERSON & MCNAMARA 1985).
R e ma r k s : Ammonites gemmatus was first figured by HUPÉ (1854), but the original from Chile is lost. STEINMANN’s concept (1895) of G. gemmatus differs from HUPÉ’s original description by sharper flanks on the ventral area and by a wider umbilicus. However, subsequent authors have considered them conspecific. G. gemmatus from Antarctica decribed by KILIAN & REBOUL (1909), SPATH (1953), HOWARTH (1958) and MACELLARI (1986) differs from material of the Quiriquina Formation presented here. For instance, specimens de-
Grossouvrites joharae n. sp. Figs. 22a, 23, 25, 26 a-c 1909
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Kossmaticeras (Grossouvrites) gemmatus (HUPÉ). – KILIAN & REBOUL, p. 38, pl. 17, figs. 1-3.
208
C. Salazar et al.
Fig. 23. Relationship between Wb/Wh and D in Grossouvrites.
1953 1958 1984 1986
Grossouvrites gemmatus (HUPÉ). – SPATH, p. 29, pl. 5, fig. 1. Grossouvrites gemmatus (HUPÉ). – HOWARTH, p. 12, pl. 2, fig. 4. Grossouvrites gemmatus (HUPÉ). – OLIVERO, p. 73, pl. 2, figs. 1-2. Grossouvrites gemmatus (HUPÉ). – MACELLARI, p. 43, figs. 33.1-33.3, 35.
Dimensions CPUC/Q/ LT/100 CPUC/Q/ CO/358 CPUC/Q/ CO/3479
D
Wb
Wh
Wb/Wh U
U/D
140.0 53.0
68.0
0.77
31.0
0.22
(220.0) 63.0
85.0
0.74
43.0
(0.19)
67.0
(0.24)
(270.0) (86.0) (104.0) (0.82)
Remarks : Grossouvrites joharae n. sp. differs from G. gemmatus by an inflated whorl section, rounded venter (Fig. 22), elongated tubercles and thicker ribs. G. gemmatus from Australia (HENDERSON & MCNAMARA 1985) differs by rounded umbilical tubercles, a wider umbilicus (U/D 0.25-0.35), a discoidal whorl section, straight and subparallel flanks and a rounded venter (Fig. 23). Grossouvrites joharae n. sp. and specimens of G. gemmatus from Antarctica are similar in ornament, whorl section and ontogenetic growth curve (Figs. 22-23); we therefore include the Antarctic material in this new species.
Ty p e s : Holotype: CPUC/Q/LT/100, a well-preserved phragmocone. Paratypes: CPUC/Q/CO/3479 is a phragmocone, with the ventral area slightly deformed. CPUC/Q/CO/ 358 is a complete shell. E t y m o l og y : Species dedicated to JOHARA BOURKE in recognition of her assistance and importance to the senior author. D ia g n o s is : Whorl section subrounded and inflated, flanks subparallel to slightly convex, venter widely rounded. 11-13 strong umbilical tubercles present per half whorl and each tubercle giving rise to 2-3 thick, equidistant ribs of similar size and course.
O ccur rence: In the Quiriquina Formation, Grossouvrites joharae n. sp. was recorded from the Eubaculites carinatus Zone. At Las Tablas, it was registered in the coquina layer unit and the lower part of the unit with calcareous sandstone concretions. At Cocholgüe, the species was recorded from the unit with calcareous sandstone concretions. In Antarctica, the taxon is known from the Maastrichtian (MACELLARI 1986).
D e s c r ip tio n : Coiling evolute and compressed. Whorl section subrounded, inflated, and compressed, higher than wide. Umbilical border straight and vertical. Flanks subparallel to slightly convex and venter widely rounded (Fig. 22). Between 11-13 strong umbilical tubercles present per half whorl, rounded to elongate, giving rise to 2-3 thick, slightly prorsiradiate and flexuous ribs; convex on dorsolateral and slightly concave on ventral area. Additional rib usually intercalated between each tubercle.
Genus Gunnarites KILIAN & REBOUL, 1909 Type s pecies : Gunnarites antarcticus WELLER, 1903, by original designation.
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Ammonites from the Maastrichtian Quiriquina Formation in central Chile
209
Fig. 24. a: Maorites densicostatus (KILIAN & REBOUL, 1909), CPUC/Q/LT/1610, x0.7. b-e: Grossouvrites gemmatus gemmatus. (HUPE, 1854). b: CPUC/Q/LT/276, x1; c-e: CPUC/Q/LT/3580, x1.
M aterial: Two fragments of phragmocones, CPUC/Q/ SV/3306 and CPUC/Q/LT/2163.
Gunnarites cf. bhavaniformis (KILIAN & REBOUL, 1909) Fig. 26 e 1909 1953 1953 1972 1986
D es cription: Coiling evolute and compressed, with discoidal whorl section. Flanks straight, slightly convex, venter narrowly rounded. Shell ornamented by fine prorsiradiate and flexuous ribs and umbilical tubercles, latter fine and rounded; each tubercle giving rise to 3 to 4 fine ribs, slightly convex on dorsolateral area, prorsiradiate and convex on mid-flank and concave on venter.
Kossmaticeras (Gunnarites) antarcticum ST. WELLER sp., var. bhavaniformis, KILIAN & REBOUL, p. 33, pl. 15, fig. 2. Gunnarites bhavaniformis (KILIAN & REBOUL). – SPATH, p. 32, pl. 8, figs. 1-7. Gunnarites kalika (STOLICZKA). – SPATH, p.33. pl. 10, figs. 1-6. Gunnarites kalika (STOLICZKA). – LAHSEN & CHARRIER, p. 529, pl. 2, figs. 3-6. Gunnarites bhavaniformis (KILIAN & REBOUL). – MACELLARI, p. 42, fig. 33.7.
Dimensions D CPUC/Q/ SV/3306 65.0
eschweizerbart_xxxx
Wb
WH
WB/Wh U
(14.0) (28.0) (0.50)
U/D
(14.0) (0.21).
210
C. Salazar et al.
Fig. 25. Grossouvrites joharae n. sp. CPUC/Q/CO/3479, x0.5.
Remarks : Gunnarites spinosissimus was established by WETZEL (1930). It is characterised by rectiradiate ribs, a straight and vertical umbilical shoulder and ribs with fine spines (STINNESBECK 1986). In our material there are no new specimens present.
R e ma r k s : Ornament and coiling of the present fragments correspond to G. bhavaniformis, with the only difference that crenulation of ribs is not recognised here, possibly due to surface weathering. Gunnarites spinosissimus is similar, but differs in having rectiradiate ribs, a straight umbilical shoulder and fine spines on the ribs (STINNESBECK 1986).
O ccur rence: Gunnarites spinosissimus was recorded by STINNESBECK (1986) from the San Vicente section, from the unit with calcareous sandstone, in the Eubaculites carinatus Zone.
O c c u r r e n c e : In the Quiriquina Formation, this taxon appears in the Baculites anceps and Eubaculites carinatus zones. At Las Tablas, it was registered in the coquina layer unit and in the lower part of the unit with calcareous sandstone concretions. At Cocholgüe, it is recorded in the unit with calcareous sandstone concretions. Gunnarites bhavaniformis was recorded from the upper Campanian of Seymour Island (Antarctica) by MACELLARI (1986) and from the Maastrichtian of Magallanes in southern Chile (LAHSEN & CHARRIER 1972). It is thus only known from Antarctica and Chile.
Genus Maorites MARSHALL, 1926 Type species: Maorites tenuicostatus (MARSHALL, 1926), by original designation.
Maorites densicostatus (KILIAN & REBOUL, 1909) Figs. 24 a, 26 d
Gunnarites spinosissimus WETZEL, 1930 1930 1986
1909
Gunnarites spinosissimus WETZEL, p. 85, pl. 14, fig. 2. Gunnarites spinosissimus WETZEL. – STINNESBECK, p. 215, pl. 12, fig. 2; pl. 13, figs. 2-3.
1917 1926
Ty p e s : Holotype is IPB V-259, from the Maastrichtian Quiriquina Formation, Chile.
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Kossmaticeras (Madraites) bhavani (STROLICZKA) var. densicostata KILIAN & REBOUL, p. 30, pl. 15, fig. 4; pl. 18, fig. 1. Kossmaticeras tenuicostatum MARSHALL, p. 445, pl. 33, fig. 1. Maorites tenuicostatus (MARSHALL). – MARSHALL, p. 177, pl. 23, fig.1; pl. 42, figs. 1-2.
Ammonites from the Maastrichtian Quiriquina Formation in central Chile
211
Fig. 26. a-c: Grossouvrites joharae n. sp., CPUC/Q/LT/100, x0.6. d: Maorites densicostatus (KILIAN & REBOUL, 1909), CPUC/Q/LT/3295, x0.5. e: Gunnarites cf. bhavaniformis (KILIAN & REBOUL, 1909), CPUC/Q/SV/3306, x1.
1926 1953 1970
Maorites suturalis MARSHALL, p. 179, pl. 23, fig. 3; pl. 43, fig. 1; pl. 45, fig. 5. Maorites densicostatus (KILIAN & REBOUL). – SPATH, p. 23, pl. 2, figs. 7-9, (non pl. 7, fig. 6). Maorites tenuicostatus (MARSHALL). – HENDERSON, p. 50, pl. 9, figs. 3-4; pl. 10, fig. 2.
1972 1977 1985
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Maorites cf. M. tenuicostatus (MARSHALL). – LAHSEN & CHARRIER, p. 530, pl. 3, figs. 1-2. Maorites tenuicostatus (MARSHALL). – COLLIGNON, p. 12, pl. 5, figs. 2-3. Maorites densicostatus (KILIAN & REBOUL). – HENDERSON & MCNAMARA, p. 64, pl. 4, figs. 7-8, 11-13.
212
C. Salazar et al.
Fig. 27. a: Whorl section of Pachydiscus (P.) jacquoti chilensis STINNESBECK, 1986, CPUC/Q/CO/1476. b-c: Whorl section of Pachydiscus (Pachydiscus) gutierrezi n. sp., b: CPUC/Q/LT/89. c: CPUC/Q/CO/2786.
1986 1986
is known from the Santonian-Maastrichtian of New Zealand (HENDERSON 1970), the Maastrichtian of the Magallanes region in southern Chile (LAHSEN & CHARRIER 1972), Seymour Island in Antarctica (MACELLARI 1986), and from the upper Maastrichtian Miria Formation in Australia (HENDERSON & MCNAMARA 1985). It has a southern IndoPacific distribution.
Maorites tenuicostatus (MARSHALL). – STINNESBECK, p. 215, pl. 11, figs. 4-6. Maorites densicostatus (KILIAN & REBOUL). – MACELLARI, p. 25 figs. 23.4-23.9, 24, 25.1, 26 (with additional synonymy).
M a t e r i a l : Six phragmocones with shell preserved. D e s c r i p t i o n : Coiling evolute. Whorl discoidal, with straight umbilical wall, straight-subparallel flanks and arched venter. Ornament of last whorl of 9 rounded to elongated umbilical nodes, 80 to 84 thick prorsiradiate flexuous ribs and 7 to 8 prorsiradiate, flexuous constrictions. Most ribs emerge on umbilical shoulder while others are virgatotome and successively initiate upwards from constrictions; some ribs have ramifications. Dimensions CPUC/Q/ LT/3501 CPUC/Q/ CO/3645 CPUC/Q/ LT/1610 CPUC/Q/ LT/2446 CPUC/Q/ LT/2445 CPUC/Q/ LT/3295
D
Wb
Wh
Wb/Wh U
U/D
-
9.0
11.0
0.82
-
-
58.0
17.0
25.0
0.68
17.0
0.29
82.0
21.0
38.0
0.55
20.0
0.24
-
23.0
36.0
0.64
-
-
-
29.0
(43.0) (0.67)
-
-
62.0
46.0
0.29
Family Pachydiscidae SPATH, 1922 Genus Pachydiscus ZITTEL, 1884 Subgenus Pachydiscus MATSUMOTO, 1947 Type species: Ammonites neubergicus VON HAUER, 1858, p. 12, pl. 2, figs. 1-4), by subsequent designation of DE GROSSOUVRE (1894: 177).
Pachydiscus (Pachydiscus) jacquoti (SEUNES, 1890) Pachydiscus (Pachydiscus) jacquoti chilensis STINNESBECK, (1986) Figs. 27a, 28 a-b, 30 1930 1986
154.0 38.0
0.61
Parapachydiscus ootacodensis WETZEL, p. 85, pl. 13, fig. 2. Pachydiscus (Pachydiscus) jacquoti chilensis STINNESBECK, p. 218, pl. 13, fig. 8; pl. 15, figs. 1, 3.
M aterial: Three well-preserved phragmocones.
Remarks: M. tenuicostatus and M. suturalis present gradual transitions regarding ribs and were first considered synonymous by HENDERSON (1970). MACELLARI (1986) interpreted M. tenuicostatus as a synonym of M. densicostatus, and presented a full discussion of this species.
D es cription: Coiling evolute-compressed and umbilicus narrow (U/D 0.25-0.32). Compressed whorl rounded (WB/WH 0.72-0.93). Umbilical wall rounded and flanks convex. Ornament on last whorl of 15 to 16 primary ribs, distant, prorsiradiate and slightly concave. In addition, 13 primary ribs with strong elongated umbilical tubercles. 14-15 secondary ribs are thinner and initiate on mid-flank, parallel to main ribs.
O c c u r r e n c e : In the Quiriquina Formation (sections Las Tablas and Cocholgüe) Maorites densicostatus is present in the Eubaculites carinatus Zone. At Las Tablas, it is recorded from the unit of coquina layers and in the unit of calcareous sandstone concretions. At Cocholgüe, it is present in the unit of calcareous sandstone concretions. M. densicostatus
Dimensions D Wb CPUC/Q/ CO/1476 150.0 54.0
eschweizerbart_xxxx
Wh
Wb/Wh U
U/D
58.0
0.93
0.30
45.0
Ammonites from the Maastrichtian Quiriquina Formation in central Chile
213
Fig. 28. a-b: Pachydiscus (Pachydiscus) jacquoti chilensis STINNESBECK (1986); CPUC/Q/CO/539, x0.6.
CPUC/Q/ LT/2436 CPUC/Q/ CO/539
160.0 (42.0) 75.0
(0.56)
51.0
0.32
210.0 68.0
0.72
53.0
0.25
94.0
Maastrichtian Abathomphalus mayaroensis planktonic foraminiferal biozone (WARD & KENNEDY 1993).
Pachydiscus (Pachydiscus) gutierrezi n. sp. Figs. 27 b-c, 29-31, 32 a-b
R e ma r k s : The type material of P. (P.) jacquoti chilensis differs from P. (P.) jacquoti jacquoti (SEUNES, 1890) by a higher number of ribs (22-26) per whorl and coarse ornament (WARD & KENNEDY 1993). P. (P.) neubergicus differs by the presence of concave ribs on the dorsolateral area, a more compressed whorl section and a narrow umbilicus (WARD & KENNEDY 1993). Pachydiscus (Pachydiscus) gutierrezi n. sp. differs from P. (P.) jacquoti chilensis by a narrower umbilicus, slightly flexuous ribs and rounded whorl section (Figs. 27, 30).
1986
Pachydiscus (Pachydiscus) sp. – STINNESBECK, p. 220, pl. 13, figs. 6-7.
Types: Holotype CPUC/Q/LT/89 is a well-preserved phragmocone. Paratypes: CPUC/Q/CO/2786, CPUC/Q/CR/264 and CPUC/Q/CO/3297 are well-preserved phragmocones. Additional material are eight phragmocones, plus IPB CO/159 and IPB CO/160 (see STINNESBECK 1986: figs. 6-7).
O c c u r r e n c e : In the Quiriquina Formation, P. (P.) jacquoti chilensis is recorded from the Eubaculites carinatus Zone. At Las Tablas, it is registered in the unit with coquina layers and the lower part of the unit with calcareous sandstone concretions. At Cocholgüe, it is recorded in the unit with calcareous sandstone concretions. P. (P.) jacquoti is restricted to the upper Maastrichtian with records from France, the Netherlands, Armenia and Madagascar (WARD & KENNEDY 1993) and Prairie Bluff Chalk (COBBAN & KENNEDY 1995). In the Miria Formation of Western Australia P. (P.) jacquoti australis is assigned to the upper Maastrichtian (HENDERSON & MCNAMARA 1985). In the Biscay region, P. (P.) jacquoti is restricted to the upper
Etymology: We dedicate this species to HÉCTOR GUTIERREZ in acknowledgement of his help in collecting fossils from the Quiriquina Formation. D iagnos is : Characterised by evolute coiling, inflated compressed whorl section, rounded umbilical wall and wide rounded venter. 11-13 elongated umbilical tubercles present on last whorl, giving rise to broad prorsiradiate ribs. Primary ribs paralleled by 2-3 finer secondary ribs without tubercles. In total, 30 ribs present on last whorl. D es cription: Coiling evolute (U/D 0.19-0.29). Whorl section compressed rounded (Wb/Wh 0.92-1.10), with
eschweizerbart_xxxx
214
C. Salazar et al.
Fig. 29. Suture line of Pachydiscus (Pachydiscus) gutierrezi n. sp. (CPUC/Q/CO/2786).
rounded umbilical wall, convex flanks and rounded, widely arched venter (Fig. 27b-c). Ornament of last whorl consisting of 11 to 13 elongated tubercles, passing into thick primary ribs, rectiradiate to prorsiradiate and slightly flexuous; slightly concave on dorsolateral area and slightly convex at mid-flank. Secondary ribs inserted between main ribs and parallel to these; initiate as fine ribs on umbilical shoulder and increase in width towards venter. Suture line with rounded elements, L1 deeper than E. L1 and L2 divided into seven auxiliary lobes with biphylloid and triphylloid terminations and with simple terminations at base of lobe and saddle. E/L1 and L1/L2 divided into six auxiliary saddles with simple, biphylloid and triphylloid endings and U retracted (Fig. 29). Dimensions CPUC/Q/ LT/3646C CPUC/Q/ LI/3483 CPUC/Q/ LI/3282 CPUC/Q/ LT/3646B CPUC/Q/ LT/3646D CPUC/Q/ PP/3104 CPUC/Q/ LT/3646A CPUC/Q/ CO/3299 CPUC/Q/ CO/2786 CPUC/Q/ CO/3297 CPUC/Q/ CO/1540 CPUC/Q/ LT/89
Remarks : Pachydiscus (Pachydiscus) gutierrezi n. sp. resembles P. (P.) jacquoti chilensis, but the latter has a whorl section which is higher than wide (Fig. 27), ribs are prorsiradiate and concave, and the umbilicus is wider (U/D 0.25-0.32). In the ontogeny P. (P.) gutierrezi n. sp. has differential distribution (Fig. 31). In Pachydiscus (P.) jacquoti, the umbilicus is wider, the whorl section more subrounded, the umbilical wall is vertical, the ventrolateral area is narrower and the venter is arched (HENDERSON & MCNAMARA 1985). Whorl section in Pachydiscus (P.) noetlingi is oval and 60 ribs are present per whorl, approximately 30 more than in Pachydiscus (Pachydiscus) gutierrezi n. sp. Adults of Pachydiscus. (P.) neubergicus are characterised by 20-27 ventral ribs per half whorl and a narrower whorl section (WARD & KENNEDY 1993). Pachydiscus (P.) egertoni has umbilical bullae, ribs efface on the flanks and whorl section compressed (KENNEDY & HENDERSON 1992a and COBBAN & KENNEDY 1995). In Menuites fresvillensis the whorl section is elliptical to rounded, umbilical bullae are weak and 39 to 41 wide ribs are present.
D
Wb
Wh
Wb/Wh U
U/D
13.5
-
-
-
4.0
0.29
16.0
7.0
6.0
1.10
3.0
0.19
18.0
8.0
8.5
0.94
4.0
0.22
20.0
(6.5) 10.0
(0.65)
4.5
0.22
21.0
10.0
10.5
0.95
5.0
0.23
27.0
12.0
13.0
0.92
6.0
0.22
28.0
12.5
13.0
0.96
7.0
0.25
Genus Menuites SPATH, 1922
31.0
(11.0) 14.0
(0.78)
7.0
0.22
Type s pecies : Ammonites menu FORBES, 1846, p. 111, pl. 10 fig. 1, by original designation.
50.0
23.5
0.98
13.0
0.26
75.0
(32.0) (33.0) (0.97)
22.0
0.29
76.0
32.0
33.5
0.95
18.5
0.24
138.0 68.0
71.0
0.95
26.0
0.19
24.0
O ccur rence: In the Quiriquina Formation, Pachydiscus (Pachydiscus) gutierrezi n. sp. is present in the Eubaculites carinatus Zone. In the sections Las Tablas, Cocholgüe, Lirquén and Puente Perales the taxon is recorded from the unit with calcareous sandstone concretions.
Menuites fresvillensis (SEUNES, 1890) Figs. 30, 32 c-d, 33a-b, 34 a-b, 35 a-b, 36 a-b 1890
eschweizerbart_xxxx
Pachydiscus fresvillensis SEUNES, p. 3, pl. 2(1), fig. 1.
Ammonites from the Maastrichtian Quiriquina Formation in central Chile
215
Fig. 30. Relationship between Wb/Wh and D in species of Pachydiscus and Menuites from the Quiriquina Formation.
1895
Pachydiscus quiriquinae STEINMANN, p. 74, pl. 6, fig. 3a, b. 1930 Pachydiscus sp. – WETZEL, p. 86, pl. 14, fig.1. 1986 Anapachydiscus fresvillensis quiriquinae (STEINMANN). – STINNESBECK, p. 221, pl. 14, fig. 1; pl. 16, fig. 1. 1986 b Anapachydiscus fresvillensis SEUNES. – KENNEDY, p. 173, pl. 6; pl. 7, figs. 1-2; pl. 8; pl. 9, figs. 1-2; pl. 10, figs. 1-5; pl. 11, figs. 5-6; pl. 12, figs. 12-14; pl. 13, figs. 6-7; pl. 14, figs. 1-3, 7, 11-12; pl. 15, figs. 4-6; pl. 23, fig. 5 (with full synonymy). 1993 Anapachydiscus fresvillensis (SEUNES). – WARD & KENNEDY, p. 39, figs. 35.3, 35.5-35.6, 36.1-36.2, 37.1-37.6, 38.1-38.3, 40.8, 45.1 (with additional synonymy). 1993 Menuites fresvillensis (SEUNES). – KENNEDY & HANCOCK, p. 588, pl. 3, figs. 4-5, 7; pl. 4, figs. 3-4, 6; pl. 5, figs. 1-5; pl. 6, figs. 4-5; pl. 7, figs. 1-6. 1999 Menuites fresvillensis (SEUNES). – FATMI & KENNEDY, p. 651, figs. 5.6-5.7. 2001 Menuites fresvillensis (SEUNES). – KLINGER et al., p. 283, pl. 8, text-fig. 3. 2006 Menuites fresvillensis (SEUNES). – KENNEDY & KLINGER, p. 76; figs. 69-70, 71e, f, 72b, c, 73.
D es cription: Coiling involute (U/D 0.16-0.25). Internal whorls slightly depressed, with elliptical to rounded whorl section, higher than wide. Venter rounded-arched. Flanks convex with maximum whorl width on dorsolateral area. Whorl section successively higher than wide. On last whorl, ornament of 9 to 10 weak umbilical bullae and 39 to 41 wide ribs, prorsiradiate, straight in dorsolateral area and concave between mid-flank and ventrolateral area. Dimensions D CPUC/Q/ LT/2439 CPUC/Q/ LT/1871 CPUC/Q/ LT/99 CPUC/Q/ LT/1452 CPUC/Q/ SV/98 CPUC/Q/ SV/1493
Wb
Wh
Wb/Wh U
U/D
117.0
57.0
63.0
0.90
22.0
0.19
143.0
(92.0) (69.0) (1.33)
35.0
0.25
220.0
98.0
114.0
0.86
36.0
0.16
230.0
105.0 138.0
0.76
39.0
0.17
255.0
109.0 132.0
0.83
41.0
0.16
360.0
(120.0) 169.0
(0.71)
88.0
0.24
Remarks : Anapachydiscus fresvillensis quiriquinae STINNESBECK, 1986 was considered synonymous with Menuites fresvillensis KENNEDY (1986b). HENDERSON & MCNAMARA (1985), KENNEDY (1986b, 1986c) and WARD & KENNEDY (1993) presented full discussions of this species. The ornament of Menuites fresvillensis is closely related with Menuites gerardoi n. sp., but a preferential distribution of the two species is observed in their ontogeny (Fig. 30). Menuites gerardoi n.sp. is wider than high and the last whorl has 20-25 wide and lengthened umbilical bullae.
Ty p e : Lectotype, as designated by KENNEDY (1986c, p. 44) is no. A1186 in the collections of the École des Mines, Paris, now in the collections of the Université ClaudeBernard, Lyon. It is the original of SEUNES (1890, p. 3, pl. 2(1), fig. 1), from the Calcaire à Baculites of Fresville, Manche, France. M a te r ia l: Six well-preserved phragmocones.
eschweizerbart_xxxx
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C. Salazar et al.
Fig. 31. a-b: Pachydiscus (Pachydiscus) gutierrensi n. sp.; CPUC/Q/LT/89, x1.
O c c u r r e n c e : In the Quiriquina Formation (section Las Tablas), this taxon is recorded from the coquina layer unit. It is also registered from San Vicente where it occurs in a unit of calcareous sandstone. Elsewhere, Menuites fresvillensis is known from the upper Maastrichtian of the Cotentin Peninsula and the Pyrénées-Atlantique region of France, the Netherlands, Denmark, South India and Madagascar (KENNEDY 1986 b, 1986c), Pakistan (FATMI & KENNEDY 1999), Australia (HENDERSON & MCNAMARA 1985), the Biscay region (WARD & KENNEDY 1993) and South Africa (KENNEDY & KLINGER 2006). The species appears to be restricted to the upper Maastrichtian and, where known (e. g., the Biscay region), to the A. mayaroensis Zone.
CPUC/Q/SV/1464, CPUC/Q/CR/264 and CPUC/Q/SV/ 1451.
Menuites gerardoi n. sp. Figs. 32, 36 c-d, 37a-b, 38 a-b, 39a-b, 40 a-b
D es cription: Coiling involute (U/D 0.14-0.25). Whorl section elliptical to rounded, wider than high (Wb/Wh 1.7-1.28). Umbilical shoulder rounded and flanks convex. Venter wide and evenly rounded. In juvenile specimens (D < 150 mm), ornament of approximately 20 wide and lengthened umbilical bullae weakening towards mid-flank.
Etymology: Species dedicated to Gerardo Flores in acknowledgement for preparation of ammonites and for his help in collecting fossils from the Quiriquina Formation. D iagnos is : Whorl section rounded, wider than high. In juvenile specimens, last whorl shows 20 wide and lengthened umbilical bullae giving rise to primary, prorsiradiate ribs. 1-2 secondary ribs intercalated between each primary rib. In adult specimens, 20-25 lengthened umbilical bullae are present, gradually passing into wide prorsiradiate ribs.
Ty p e : Holotype is CPUC/Q/SV/1455. Paratypes are CPUC/Q/SV/2846, CPUC/Q/SV/2845, CPUC/Q/SV/1453,
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217
Fig. 32. a-b: Pachydiscus (Pachydiscus) gutierrezi n. sp., a: CPUC/Q/CO/3297, x1; b: CPUC/Q/CO/2786, x1; c-d: Menuites fresvillensis (SEUNES, 1890); CPUC/Q/LT/2439; x1.
Primary ribs wide and prorsiradiate, nearly straight on dorsolateral area and gently concave on ventrolateral area. 1 to 2 secondary ribs intercalated at mid-flank and projected towards venter. In adult specimens (D > 150 mm), ornament on the last whorl consists of 20-25 lengthened umbilical bullae, giving rise to projected wide ribs, prorsiradiate, straight in dorsolateral area and concave between mid-flank and ventrolateral area. Dimensions D Wb Wh Wb/Wh U CPUC/Q/ CR/264 103.0 (66.0) 53.0 (1.25) 25.0 CPUC/Q/ SV/1451 238.0 (83.0) 132.0 (0.63) 34.0
CPUC/Q/ SV/2845 CPUC/Q/ SV/2846 CPUC/Q/ SV/1464 CPUC/Q/ SV/1455 CPUC/Q/ SV/1453
U/D
270.0 151.0 135.0 1.11
69.0
0.25
280.0 156.0 121.0 1.28
65.0
0.23
285.0 160.0 139.0 1.15
65.0
0.23
300.0 190.0 158.0 1.20
66.0
0.22
350.0 183.0 170.0 1.07
80.0
0.23
Remarks : Menuites gerardoi n. sp. is closely related to Menuites fresvillensis. However, marked differences exist during their ontogenetic development, with M. gerardoi n. sp. characterised by a wide whorl section (Fig. 30). In
0.24 0.14
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218
C. Salazar et al.
Fig. 33. a-b: Menuites fresvillensis (SEUNES, 1890); CPUC/Q/SV/98, x0.4.
Menuites fresvillensis, the whorl section is discoidalelongated, higher than wide (Fig. 30). In addition, between 18-21 umbilical bullae are present on the last whorl, each grading into a primary rib. Menuites gerardoi n. sp. resembles Menuites spathi but the latter has a depressed reniform whorl section, 26-35 ribs narrow and sharp, concave across the flank, the ribs arise in pairs at the umbilical shoulder, with some shorter intercalated ribs (KENNEDY & KLINGER 2006).
Subfamiliy Diplomoceratinae SPATH, 1926 Genus Diplomoceras HYATT, 1900 Type s pecies : Baculites cylindraceus DEFRANCE, 1816, p. 160, by original designation. For a discussion of the genus, see OLIVERO & ZINSMEISTER (1989); and see KENNEDY (1986c).
Diplomoceras cylindraceum (DEFRANCE 1816) Figs. 41-42
O c c u r r e n c e : In the Quiriquina Formation, this taxon is recorded only from the San Vicente section where it occurs in the unit with calcareous sandstone concretions in the Eubaculites carinatus Zone.
1816 1895 1930 1986
Suborder Ancyloceratina W IEDMANN, 1966 Superfamily Turrilitoidea G ILL, 1871 Familiy Diplomoceratidae SPATH, 1926
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Baculites cylindracea DEFRANCE, p. 160. Hamites cf. cylindraceus, STEINMANN, p. 89 (non cylindraceus DEFRANCE 1822). Diplomoceras cf. notabile, WETZEL, p. 89. Diplomoceras (Diplomoceras) cf. notabile (WHITEAVES). – STINNESBECK, p. 200.
Ammonites from the Maastrichtian Quiriquina Formation in central Chile
219
Fig. 34. a-b: Menuites fresvillensis (SEUNES, 1890); CPUC/Q/LT/99, x0.5.
Type: The neotype, designated by KENNEDY (1986b: 181, pl. 24, figs. 1-3), is IRSNB 10511.
1986 b Diplomoceras cylindraceum (DEFRANCE. – KENNEDY, p.181, pl. 17, fig. 3, pl. 18, fig. 5, pl. 21, figs. 2-4, 6, pl. 22, fig 6, pl. 23, figs. 1-2, pl. 24, figs. 1-3, pl. 25, figs. 1-8, pl. 26, fig. 18, pl. 33, fig. 16, pl. 36, fig. 6, text-figs. 9-10. 1986 c Diplomoceras cylindraceum (DEFRANCE). – KENNEDY p. 51, pl. 4, figs. 1-2; pl. 9, figs. 8-10; pl. 10; text-figs 3i-l, 6, 7g-m (with full synonymy). ? 1989 Diplomoceras lambi (SPATH). – OLIVERO & ZINSMEISTER, p. 627, fig. 2.1-2.4. ? 1989 Diplomoceras maximum (SPATH). – OLIVERO & ZINSMEISTER, p. 629, figs. 2.5, 4.1-4.4, 5.1-5.4. 1992 b Diplomoceras cylindraceum (DEFRANCE). – KENNEDY & HENDERSON, p. 704, pl. 6, figs. 1-3; textfigs. 1b, 3 (with full synonymy). 1992 Diplomoceras cylindraceum (DEFRANCE). – HENDERSON et al., p. 140, figs. 5, 6a-e, h-k, 7. 1993 Diplomoceras cylindraceum (DEFRANCE). – WARD & KENNEDY, p. 49, figs. 42, 43.16-43.17. 2003 Diplomoceras cylindraceum (DEFRANCE). – KLINGER & KENNEDY, p. 171 ff., figs. 1-17. 2004 Diplomoceras cylindraceum (DEFRANCE). – IFRIM et al., text-figs. 13G-H, 14E.
M aterial: Five fragments of the straight shaft and one specimen corresponding to a well-preserved hook. Description: Whorl section elliptical to rounded, ornament of dense-near, ventrally projected ribs. Specimen CPUC/ Q/LT/2077 has a rib index of 16 with Wh 69 mm. On hook, ribs are radially projected. Dimensions CPUC/Q/ CO/3581 CPUC/Q/ LT/2320 CPUC/Q LT/2077 CPUC/Q/ SV/2317 CPUC/Q/ SV/573
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Wh
Wb
Wb/Wh L
(130.0) (62.0) (0.47)
140.0
65.0
62.0
0.95
104.0
69.0
59.0
0.85
245.0
64.0
58.0
0.91
94.0
65.0
56.0
0.86
134.0
220
C. Salazar et al.
Fig. 35. a-b: Menuites fresvillensis (SEUNES, 1890), CPUC/Q/LT/1452, x0.5.
R e ma r k s : Diplomoceras cylindraceum is a highly variable species concerning whorl section and ribbing; D. lambi, D. notabile and D. maximum are considered synonymous (KENNEDY 1986 c). WARD & KENNEDY (1993), KENNEDY (1986b and 1986c) and KLINGER & KENNEDY (2003) gave detailed accounts of the species.
Phylloptychoceras sp. Remarks : STINNESBECK (1986) described this genus from the Quiriquina Formation, based on five fragments of phragmocones. They are closely related to Phylloptychoceras sipho.
O c c u r r e n c e : In the Quiriquina Formation (sections Las Tablas, Cocholgüe and San Vicente), D. cylindraceum is recorded from the upper portion of the unit with calcareous sandstone concretions, in the Zone “without baculitids” (Hoploscaphites constrictus subzone, Fig. 2). Diplomoceras cylindraceum is a cosmopolitan species of the upper Campanian to Maastrichtian (IFRIM et al. 2004).
O ccur rence: In the Quiriquina Formation, Phylloptychoceras sp. has been recorded by STINNESBECK (1986) from the Tomé section, in the unit with calcareous sandstone concretions, in the Eubaculites carinatus Zone (Fig. 2).
Family Baculitidae GILL, 1871 Genus Baculites LAMARCK, 1799
Subfamily Polyptychoceratinae MATSUMOTO, 1938 Genus Phylloptychoceras SPATH, 1953
Type s pecies : Baculites vertebralis LAMARCK, 1801, p. 103, by subsequent designation of MEEK (1876: 391).
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Ammonites from the Maastrichtian Quiriquina Formation in central Chile
221
Fig. 36. a-b: Menuites fresvillensis (Seunes, 1890); CPUC/Q/SV/1493, x0.25; c-d: Menuites gerardoi n. sp.; CPUC/Q/SV/1455, x0.5.
D es cription: Whorl section ovoid to sub-pentagonal, higher than wide. Venter acute with flattened keel. In early growth stages (Wh < 20 mm) dorsum flat to slightly rounded and flanks moderately convex. Maximum whorl width at mid-flank. In following growth stage (Wh > 20 mm), dorsum flat, flanks slightly rounded. Maximum whorl width approximately at mid-flank (Fig. 44). Ornament of thick ribs, prorsiradiate on flanks and concave on dorsum. On venter, ribs are finer and projected towards aperture. In young specimens, rib index 9-5 with Wh 18, adult rib index 1-2 with Wh 43.
Baculites huenickeni STINNESBECK 1986 Fig. 43 a-i, 44 c-d 1975 1986
Baculites sp. B. – HÜNICKEN & COVACEVICH, p. 146, pl. 2, figs. 1-3; text-fig. 5 a-b. Baculites huenickeni STINNESBECK, p. 201, pl. 8, figs. 7-8; pl. 9, figs. 1-2; text-fig. 24B, C.
Ty p e : Holotype is IPB VO/96 of the La Gloria section at San Vicente, designated by STINNESBECK (1986: 201, pl. 8, fig. 7), from the Maastrichtian of the Quiriquina Formation, Chile.
Dimensions Wh CPUC/Q/ CO/2563 43.0
M a te r ia l: 32 specimens, all well-preserved internal moulds of phragmocones. Only the best-preserved specimens were measured and listed.
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Wb
Wb/Wh L
28.0
0.65
45.0
222
C. Salazar et al.
Fig. 37. a-b: Menuites gerardoi n. sp., CPUC/Q/CR/264, x1.
CPUC/Q/ LT/269 CPUC/Q/ CO/3490 CPUC/Q/ LM/3182 CPUC/Q/ LT/3141 CPUC/Q/ SV/1023 CPUC/Q/ CO/3503 CPUC/Q/ LM/3192 CPUC/Q/ LM/3576 CPUC/Q/ LM/3195 CPUC/Q/ TO/3504 CPUC/Q/ LM/3185 CPUC/Q/ LM/3196 CPUC/Q/ LM/3197 CPUC/Q/ LM/3194
38.5
26.5
0.69
116.0
25.0
17.0
0.68
53.0
26.0
16.0
0.62
52.0
23.0
16.0
0.70
75.0
24.0
15.0
0.62
48.0
22.0
13.0
0.59
138.0
18.0
13.0
0.72
50.0
20.0
11.0
0.55
80.0
18.5
11.5
0.62
101.0
18.0
11.0
0.61
72.0
15.0
10.0
0.66
94.0
15.0
10.0
0.66
62.0
13.0
10.0
0.76
41.0
11.5
-
-
63.0
O ccur rence: In the Quiriquina Formation (sections Las Tablas, Cocholgüe, San Vicente and Santa Sabina), the taxon is recorded from the unit with calcareous sandstone concretions, in the Eubaculites carinatus Zone (Fig. 2). Baculites huenickeni is restricted to the Quiriquina Formation.
Baculites anceps LAMARCK, 1822 Figs. 43 j-n, 44 a-b, 45 f-g 1822 1965
Baculites anceps LAMARCK, p. 648. Baculites anceps LAMARCK. – HOWARTH, p. 363, pl. 4, fig. 4; pl. 5, figs. 4-5; pl. 6, figs. 1-5; text-figs. 2-3, 5-12 (with full synonymy). 1975 Baculites sp. A. – HÜNICKEN & COVACEVICH, p. 144, pl. 1, figs. 1-4; text-figs. 3-4. 1986 Baculites sp. – STINNESBECK, p. 204, pl. 9, figs. 3, 5; text-fig. 24A, a, b. 1986b Baulites anceps LAMARCK. – KENNEDY, p. 189, pl. 20, fig. 2, pl. 28, figs. 3, 11-13, 19-23, text.-fig. 11C, D (with full synonymy). 1986c Baculites anceps LAMARCK. – KENNEDY, p. 58, pl. 11, figs. 12-14, pl. 12, figs. 7-11, text-figs. 3E-H; 7A-C. 1993 Baculites anceps LAMARCK. – WARD & KENNEDY, p. 52, fig. 45.2.
Type: Neotype, designated by HOWARTH (1965: 365, pl. 5, fig 5), is BMNH 32573 from the Calcaire à Baculites in northwestern France.
R e ma r k s : Baculites huenickeni is characterised by an ovoid to subpentagonal whorl section, flat to slightly rounded dorsum and almost straight ventrolateral flanks (Fig. 44), as well as prorsiradiate ribs that weaken towards the venter. STINNESBECK (1986) discussed this species exhaustively.
M aterial: 40 specimens, all well-preserved internal moulds of phragmocones. Only the best-preserved specimens were measured and listed.
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Ammonites from the Maastrichtian Quiriquina Formation in central Chile
Fig. 38. a-b: Menuites gerardoi n. sp., CPUC/Q/SV/2845, x0.4.
D e s c r ip tio n : Whorl section ovoid, higher than wide. In early growth stages (Wh < 20 mm), dorsum rounded, flanks rounded, and maximum width near mid-flank. Venter sharp and flat. In following growth stages (Wh > 20 mm), dorsum rounded and flanks slightly rounded. Maximum whorl width at mid-flank. Venter sharply rounded and flat to slightly rounded (Fig. 44). Prorsiradiate ribs between dorsum and ventrolateral area. Concave and undulating, ventrally projected, gradually thining towards aperture and interrupted by keel. Ribs fine in juveniles (Wh < 20 mm) and spaced every 1-2 mm (rib index of 10-20 with Wh 20); gradually thicker in adult stages (Wh > 20 mm) and spaced every 12 mm (rib index 2-3 with Wh 30). Dimensions Wb CPUC/Q/ LT/3601 18.0 CPUC/Q/ LT/590 20.0
Wh
CPUC/Q/ CO/3600 CPUC/Q/ CO/3520 CPUC/Q/ SV/259 CPUC/Q/ CO/3213 CPUC/Q/ SS/3193 CPUC/Q/ CO/2928 CPUC/Q/ TO/3204 CPUC/Q/ TO/3202 CPUC/Q/ CO/3515 CPUC/Q/ TO/3203
Wb/Wh L
(35.0) (0.51)
95.0
30.0
54.0
0.66
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19.0
30.0
0.63
95.0
-
-
-
87.0
15.0
(28.0) 0.54
62.0
(14.0) 26.0
(0.53)
81.0
13.0
23.0
0.57
61.0
14.0
21.0
0.66
56.0
16.0
21.0
0.76
86.0
13.0
20.0
0.65
57.0
12.0
(18.5) (0.64)
112.0
12.0
18.0
52.0
0.66
223
224
C. Salazar et al.
Fig. 39. a-b: Menuites gerardoi n. sp., CPUC/Q/SV/2846, x0.4.
CPUC/Q/ LT/1666 CPUC/Q/ CO/3155 CPUC/Q/ CO/3444 CPUC/Q/ CO/2798 CPUC/Q/ TO/3201 CPUC/Q/ SS/3189 CPUC/Q/ SS/3184 CPUC/Q/ LI/2434 CPUC/Q/ CO/2803 CPUC/Q/ CO/2804
12.0
(17.0) (0.71)
43.0
11.5
17.0
0.68
82.0
12.5
16.5
0.75
31.0
12.0
16.0
0.75
51.0
12.0
16.0
0.75
66.0
11.5
16.0
0.72
82.0
11.0
16.0
0.69
32.0
10.5
15.0
0.70
30.0
9.0
15.0
0.60
60.0
9.0
14.0
0.64
51.0
CPUC/Q/ LI/2430 CPUC/Q/ TO/3211 CPUC/Q/ CO/2800 CPUC/Q/ CO/2805
(8.0)
14.0
(0.57)
30.0
10.0
13.5
0.77
50.0
9.0
13.0
0.69
43.0
9.0
12.0
0.75
45.0
Remarks : Baculites anceps is characterised by its ovoid whorl section, rounded dorsum and convex flanks (Fig. 44), by thick ribs on the flanks and fine ribs projected towards the venter (KENNEDY 1986b; WARD & KENNEDY 1993). The present material fits the description of Baculites sp. A of HÜNICKEN & COVACEVICH (1975) and Baculites sp. of STINNESBECK (1986). Baculites anceps of the Quiriquina Formation has a venter which is sharper than in the pacificus subspecies described by MATSUMOTO (1959). For instance, in B. anceps pacificus ribs pass to the ventral border (HÜNICKEN & COVACEVICH 1975). Baculites anceps anceps is a European form wich differs by a sharper ventral
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Ammonites from the Maastrichtian Quiriquina Formation in central Chile
225
Fig. 40. a-b: Menuites gerardoi n. sp., a: CPUC/Q/SV/1464, x0.3; b: CPUC/Q/SV/1453 x0.3.
Cocholgüe, Tomé, Lirquén, San Vicente and Santa Sabina, Baculites anceps is present in the lowermost metres of the unit with calcareous sandstone concretions. In the Danish Chalk sections, the species appears to be restricted to the upper Maastrichtian Belemnella kazimiroviensis Zone. It also occurs in the upper Maastrichtian “Calcaire à Baculites” of French Normandy, the Netherlands and the former USSR (KENNEDY 1986b). In the Biscay Region, Baculites anceps is restricted to the lower Maastrichtian (WARD & KENNEDY 1993). This taxon has a European and IndoPacific distribution.
border and by aspects of the suture, principally narrow lateral saddles and umbilical lobules (HÜNICKEN & COVACEVICH 1975). Baculites huenickeni resembles our specimens, but the whorl section of this species is ovoid-subpentagonal, the dorsum straight and flanks are almost flat (Fig. 44). O c c u r r e n c e : In the Quiriquina Formation, Baculites anceps is abundant in the unit of cross-bedded sandstone near the base of the sequence at Las Tablas and may also occur in the first meter of the coquina layers (Fig. 2). At
eschweizerbart_xxxx
226
C. Salazar et al.
4-9; pl. 3, figs. 1-8; pl. 4, figs. 1-8; pl. 5, figs. 1-4; text-figs. 6-28. 1986 Eubaculites lyelli (D’ORBIGNY). – STINNESBECK, p. 207, pl. 9, figs. 6-8; text-fig 24D. 1986 Eubaculites lyelli (D’ORBIGNY); KENNEDY et al., p. 1016, pl. 1, figs. 1-3, pl. 2, figs. 3-8, 13-21 (with full synonymy). 1986b Eubaculites lyelli (D’ORBIGNY). – KENNEDY, p. 195, pl. 27, figs. 5-8; pl. 32, figs. 13-14. 1992 Eubaculites carinatus (MORTON). – HENDERSON et al., p. 150, figs. 6F-G, 14-16, 17A-C, G-J, 18-20 (with additional synonymy). 1993 Eubaculites carinatus (MORTON). – WARD & KENNEDY, p. 53, fig. 43.8-43.9, 43.13 1993 Eubaculites carinatus (MORTON). – KLINGER & KENNEDY, figs. 7A-E, 21-30, 31A-G, 32-35, 36E-F, 37-38, 42A, 52G-H (with additional synonymy). 1995 Eubaculites carinatus (MORTON). – COBBAN & KENNEDY, p. 26, figs. 14.1, 14.5-14.7, 15.4, 15.615.18, 16.13-16.15, 16.23, 16.24, 16.28-16.30, 17.52-17.59, 18.1-18.44. 1996 Eubaculites carinatus (MORTON. – KENNEDY & COBBAN, fig. 3.1-3.3, 3.7-3.12 Type: Holotype, by monotypy, is the original of MORTON (1834, pl. 13, fig. 1) from the Maastrichtian Prairie Bluff of Alabama, no. 72866 in the collections of the Academy of Natural Sciences, Philadelphia. M aterial: 52 well-preserved phragmocones. Only the best-preserved specimens were measured and listed.
Fig. 41. Diplomoceras cylindraceum (DEFRANCE, 1816), CPUC/Q/SV/573, x1.
D es cription: Whorl section ovoid to subpentagonal, higher than wide, and dorsum flat (Fig. 44). Flanks slightly rounded. Ventrolateral flanks convergent and separated from venter by narrow longitudinal groove. Venter sharp and narrow with flat keel. Maximum whorl width at midflank (Fig. 44). During ontogeny, whorl section changes progressively from ovoid to subpentagonal. Ornament of thick and concave simple ribs, with wide interspaces over 5 mm between the ribs (rib index of 6-7 with Wh 35). Ventrolateral secondary ribs fine and projected towards aperture.
Genus Eubaculites SPATH, 1926 Ty p e s p e c ie s : Baculites vagina FORBES var. ootacodensis STOLICZCKA, 1866, p. 199, pl. 90, by original designation.
Eubaculites carinatus (MORTON, 1834) Figs. 44e, 45 a-e, 46 a-g
Dimensions CPUC/Q/ CO/3106 CPUC/Q/ CO/3524 CPUC/Q/ CO/3089 CPUC/Q/ CO/3440 CPUC/Q/ LT/2156 CPUC/Q/ CO/3291 CPUC/Q/ CO/3215
1834 1846
Baculites carinatus MORTON, p. 44, pl. 13, fig. 1. Baculites vagina FORBES in DARWIN, p. 126, pl. 5, fig. 3. 1847 Baculites lyelli D’ORBIGNY, pl. 1, figs. 3-7. 1850 Baculites lyelli D’ORBIGNY, p. 215. ? 1895 Baculites vagina FORBES. – STEINMANN, p. 89, pl. 6, fig. 4. ? 1904 Baculites vagina FORBES. – WILCKENS, p. 188. ? 1930 Baculites vagina FORBES. – WETZEL, p. 90, pl. 10, figs. 3-4. 1953 Eubaculites lyelli (D’ORBIGNY). – SPATH, p. 46 f. 1975 Eubaculites lyelli (D’ORBIGNY). – HÜNICKEN & COVACEVICH, p. 149, pl. 1, figs. 5-12; pl. 2, figs.
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Wb
Wh
Wb/Wh L
-
-
-
160.0
23.5
35.0
0.67
145.0
22.0
35.0
0.63
85.0
(23.0) 33.0
(0.70)
158.0
22.0
30.0
0.73
51.0
19.0
29.0
0.65
28.0
20.0
28.0
0.71
80.0
Ammonites from the Maastrichtian Quiriquina Formation in central Chile
Fig. 42. Diplomoceras cylindraceum (DEFRANCE, 1816), CPUC/Q/CO/2077, x1.
CPUC/Q/ CO/2926 CPUC/Q/ TO/3206 CPUC/Q/ TO/3209 CPUC/Q/ LM/3181 CPUC/Q/ CO/3107 CPUC/Q/ CO/2935
16.0
26.0
0.62
(19.0) (25.0) (0.76)
125.0
17.0
79.0
25.0
0.68
CPUC/Q/ TO/3515 CPUC/Q/ CO/3141 CPUC/Q/ TO/3208 CPUC/Q/ LT/3187 CPUC/Q/ CO/3573 CPUC/Q/ CO/2925
43.0
(20.0) (24.0) (0.88)
78.0
15.0
24.0
0.63
101.0
15.5
23.5
0.66
57.0
eschweizerbart_xxxx
15.0
23.0
0.65
82.0
17.5
23.0
0.76
69.0
16.0
23.0
0.69
67.0
13.0
23.0
0.56
52.0
14.0
22.0
0.64
47.0
14.0
21.0
0.66
49.0
227
228
C. Salazar et al.
Fig. 43. a-g: Baculites huenickeni STINNESBECK, 1986, a-b: CPUC/Q/CO/3503, x1; c-d: CPUC/Q/LT/269, x0.75; e-f: CPUC/Q/TO/3504, x1; g: CPUC/Q/CO/2563, x1. h-n Baculites anceps LAMARCK, 1822, h-i: CPUC/Q/CO/2803, x1; j: CPUC/Q/SS/3189, x1; k: CPUC/Q/CO/3515, x1; l-m: CPUC/Q/CO/3600, x1; n: CPUC/Q/TO/3204, x1.
CPUC/Q/ TO/3514 CPUC/Q/ CO/3428 CPUC/Q/ TO/3207
13.5
20.0
0.68
93.0
13.5
20.0
0.68
126.0
12.0
20.0
0.60
58.0
CPUC/Q/ LM/3183 CPUC/Q/ LM/3186 CPUC/Q/ CO/3524
eschweizerbart_xxxx
14.0
19.0
0.74
50.0
13.0
18.0
0.72
52.5
12.0
18.0
0.66
34.0
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229
Fig. 44. Whorl sections of baculitids from the Quiriquina Formation. a-b: Baculites anceps LAMARCK 1822, a: CPUC/Q/CO/3600; b: CPUC/Q/LT/3601. c-d: Baculites huenickeni STINNESBECK, 1986, c: CPUC/Q/LT/269; d: CPUC/Q/CO/2563; e: Eubaculites carinatus (MORTON, 1834), CPUC/Q/CO/3291.
CPUC/Q/ LM/3191 CPUC/Q/ LM/3198 CPUC/Q/ CO/3365 CPUC/Q/ CO/2565 CPUC/Q/ CO/3517 CPUC/Q/ CO/2568 CPUC/Q/ LI/2433 CPUC/Q/ CO/3292
abundant in the unit with calcareous sandstone concretions (Fig. 2). Elsewhere, the species is recorded from the Maastrichtian of the Netherlands, northern Spain, southwestern France, the Biscay region, Austria, California, South India, Patagonia, Mozambique, Zululand, South Africa, Western Australia and Argentina (HENDERSON et al. 1992; WARD & KENNEDY 1993). Eubaculites carinatus is thus cosmopolitan, with the exception of northern high latitudes (HENDERSON et al. 1992). In the Biscay region, Eubaculites carinatus is restricted to the upper Maastrichtian A. mayaroensis Zone (WARD & KENNEDY 1993).
12.0
17.0
0.71
68.0
12.0
17.0
0.71
36.0
12.0
17.0
0.70
66.0
11.0
17.0
0.65
65.0
10.5
16.5
0.64
50.0
12.0
17.0
0.70
46.0
11.5
16.5
0.69
41.0
Genus Trachybaculites COBBAN & KENNEDY, 1985
5.5
9.0
0.61
29.0
Type s pecies : Baculites columna MORTON, 1834, p. 44, plate 19, fig. 8, Maastrichtian of Alabama (COBBAN & KENNEDY 1995).
R e ma r k s : Eubaculites carinatus is a senior synonym of Eubaculites lyelli (KENNEDY et al. 1986). In adult stages, Eubaculites carinatus is easily differentiated from other Quiriquina baculitids by its pyriform (subpentagonal) whorl section, the flat venter and prominent ribs. Juvenile growth stages of Eubaculites carinatus resemble Baculites huenickeni, but in adult gowth stages the ribs of the latter species are thinner, flanks are slightly parallel to convex and the venter is rounded (Fig. 44). Baculites anceps differs by its ovoid whorl section and rounded dorsum and flanks (Fig. 44). Eubaculites vagina is similar to E. carinatus, but the whorl section is more angular and its ornament consists of two rows of tubercles on the middle flank and on the dorsolateral border (KLINGER & KENNEDY 1993). HENDERSON et al. (1992) and COBBAN & KENNEDY (1995) presented a complete discussions of this species.
Trachybaculites vicentei STINNESBECK, 1986 1986 Baculites vicentei STINNESBECK, p. 203, pl. 9, fig. 4; pl. 10, fig. 3; text-fig. 23a-e. Type: Holotype is IPB V3/240, designated by STINNESBECK (1986: 203), from the Maastrichtian Quiriquina Formation at San Vicente, Central Chile. Remarks : Baculites vicentei was first described for the Quiriquina Formation by STINNESBECK (1986). Its characteristic round whorl section and simple suture line distinguish the species from other baculitids of the Quiriquina Formation and elsewhere. KLINGER & KENNEDY (2001) included the species to the genus Trachybaculites.
O c c u r r e n c e : In the Quiriquina Formation (sections Las Tablas, Cocholgüe, Tomé, Lirquén and Laguna Lo Méndez), E. carinatus is rare in the unit with coquina layers, but
O ccur rence: Baculites vicentei was recorded by STINNESBECK (1986) from the San Vicente section, from the unit
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Genus Hoploscaphites NOWAK, 1911. Type s pecies : Scaphites constrictus J. SOWERBY, 1817, p. 189, pl. A, fig 1, by original designation.
Hoploscaphites constrictus quiriquiniensis (WILCKENS, 1904) Figs. 47, 48 a-k 1904
Scaphites constrictus quiriquiniensis WILCKENS, p. 189, pl. 17, figs. 3-8. ? 1953 Hoploscaphites quiriquiniensis. – SPATH, p. 14, pl. 10, fig. 8. 1982b Hoploscaphites constrictus. – BIRÓ, p. A2, pl. 2, figs. 1-3; pl. 3, figs. 4-6 (non constrictus J. SOWERBY). 1986 Hoploscaphites quiriquiniensis. – STINNESBECK, p. 208, pl. 6, figs. 4-5. Type: Holotype is IPB V 257, the original of WILCKENS (1904, pl. 6, fig. 5). M aterial: 51 specimens, fifteen of wich are complete and well preserved. Only the best-preserved specimens were measured and listed. D es cription: Coiling evolute. Whorl section discoidal, higher than wide. Umbilical border rounded and umbilical wall straight. Flanks straight and subparallel, venter rounded. Shell ornamented by dense and fine ribs, initiating on umbilical border in row of fine and small tubercles. They fork into equidistant secondary ribs near mid-flank and again on ventral shoulder (50-85 ribs on ventral area of the last whorl). Ribs are concave near umbilicus, convex near mid-flank and concave on venter. Body chamber of adults with rows of small tubercles on edge of venter. Early whorls of phragmocone lack tubercles. Suture line subdivided into subrectangular slightly rounded elements. L1 asymmetric and divided into two auxiliary lobes. External auxiliary lobe asymmetrical and with simple terminations. Internal auxiliary lobes biphylloid and asymmetrical, with simple terminations. L2 symmetrical and with biphylloid terminations. E/L1 slightly asymmetrical, divided into seven asymmetrical saddles with subrounded and simple elements. E/L1 higher than E/L2. Saddle E/L2 slightly asymmetrical and divided into three auxiliary saddles with simple and biphylloid terminations (Fig. 47). Fig. 45. a-d: Eubaculites carinatus (MORTON, 1834), a-b: CPUC/Q/CO/3524, x1; c-d: CPUC/Q/CO/3291, x1.
Dimensions D CPUC/Q/ CO/2667 34.0 53.0 CPUC/Q/ CO/3260 32.0 CPUC/Q/ CO/3427 31.0 CPUC/Q/ CO/3319 27.0
with calcareous sandstone concretions, in the Eubaculites carinatus and Baculites anceps zones (Fig. 2).
Superfamily Scaphitaceae GILL, 1871 Family Scaphitidae GILL, 1871 Subfamily Scaphitinae GILL, 1871
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Wb
Wh
Wb/Wh U
U/D
(10.5) 11.5 13.0 28.5
(0.91) 0.45
3.0
0.08
9.0
0.66
9.5
0.30
(6.0) (16.0) (0.37)
4.0
0.13
(7.0) (13.0) (0.54)
3.0
0.11
13.5
Ammonites from the Maastrichtian Quiriquina Formation in central Chile
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Fig. 46. a-g: Eubaculites carinatus (MORTON, 1834), a-b: CPUC/Q/SS/3181, x1; c: CPUC/Q/CO/3141, x1; d: CPUC/Q/TO/3514, x1; e: CPUC/Q/SS/3186, x1; f-g: CPUC/Q//LT/3187, x1.
CPUC/Q/ CO/3411 CPUC/Q/ CO/3382H CPUC/Q/ CO/3382G CPUC/Q/ CO/3382F CPUC/Q/ CO/2345 CPUC/Q/ CO/3320
23.0
(6.0) 11.0
(0.54)
4.5
0.19
20.0
(5.0) 9.0
0.55
4.5
0.23
19.5
6.5
10.0
0.65
3.0
0.15
19.0
4.5
8.0
0.56
2.5
0.13
19.0
6.5
11.0
0.59
4.0
0.21
18.0
5.0
8.5
0.58
3.0
0.16
Fig. 47. Suture line of Hoploscaphites constrictus quiriquiniensis (WILCKENS, 1904) (CPUC/Q/CO/3382H).
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Fig. 48. a-k: Hoploscaphites constrictus quiriquiniensis (WILCKENS, 1904), a-b: CPUC/Q/CO/3260, x1; c: CPUC/Q/CO/3382A, x2; d: CPUC/Q/CO/3382H, x2; e-f: CPUC/Q/CO/3382D, x2; g-h: CPUC/Q/CO/3411, x2; i-j: CPUC/Q/CO/2667, x1; k: CPUC/Q/CO/3319, x2.
CPUC/Q/ CO/3382E CPUC/Q/ CO/3261 CPUC/Q/ CO/2347 CPUC/Q/ CO/3382A CPUC/Q/ CO/3382D CPUC/Q/ CO/3382B CPUC/Q/ CO/3321 CPUC/Q/ CO/3382C
18.0
(5.0) (8.5)
(0.58)
3.0
0.16
17.5
6.5
9.5
0.68
2.0
0.11
17.5
5.5
8.5
0.65
3.5
0.20
16.5
5.0
7.5
0.66
3.0
0.18
15.0
4.5
7.0
0.64
3.5
0.23
14.0
4.0
6.0
0.66
3.0
0.21
14.0
5.0
6.5
0.77
2.5
0.17
11.5
3.5
5.0
0.70
2.5
0.22
loscaphitidae from the Quiriquina Formation differ from typical material of H. constrictus such as the specimens figured by KENNEDY (1986c), MACHALSKI (2005) and H. constrictus constrictus in VAN DER TUUK (1987). For instance, the suture line contains subrectangular-rounded elements, coiling is evolute, and whorl section is compressed whereas European material is usually characterised by a suture line with rounded elements, and an involute and inflated whorl section. H. constrictus niedzwidzkii (see VAN DER TUUK 1987) shows a close morphological resemblance to specimens from the Quiriquina Formation, but is more compressed. We therefore follow WILCKENS (1904), who differentiated Hoploscaphites constrictus quiriquiniensis as a separate subspecies for the Quiriquina material. O ccur rence: In the Quiriquina Formation (sections Cocholgüe and Dichato), this taxon is abundant in the upper portion of the unit with calcareous sandstone concretions, in the Zone “without Baculitids” (Fig. 2). Hoploscaphites constrictus is recorded at Kronsmoor in north Germany,
R e ma r k s : Hoploscaphites constrictus is well known for its wide range of variation and sexual dimorphism (KENNEDY1986c; MACHALSKI 2005). Even though, Hop-
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BROILI, F. (1930): Plesiosaurierreste von der Insel Quiriquina. – Neues Jahrbuch für Mineralogie, Geologie und Paläontologie, Beilage-Band, (B), 63: 497-514. COBBAN, W. & KENNEDY, W. J. (1991): Upper Cretaceous (Maastrichtian) ammonites from the Nostoceras alternatum Zone in southwestern Arkansas. – United States Geological Survey, Bulletin, 1985: E1-E6. – (1995): Maastrichtian Ammonites chiefly from the Prairie Bluff Chalk in Alabama and Mississippi. – Journal of Paleontology, 69: 40-65. COLLIGNON, M. (1954): Ammonites néocrétacées du Ménabe (Madagascar). III, Les Kossmaticeratidae. – Travaux du Bureau Géologique, 62: 1-59 – (1956): Ammonites néocrétacées du Menabe (Madagascar) IV: Les Phyllocératides; V: Les Gaudrycératides; VI: Les Tetragonitidae. – Annales Géologiques du Service des Mines de Madagascar, 23: 107 pp. – (1969): Atlas des fossiles caractéristiques de Madagascar (Ammonites),15(Campanien inférieur). – 216 pp.; Tananarive (Service Géologique). – (1971): Atlas des fossiles caractéristiques de Madagascar (Ammonites), 17 (Maestrichtian). – 82 pp.; Tananarive (Service Géologique). – (1977): Ammonites néocrétacées de la Nouvelle Caledonie. – Bureau de Recherches Géologiques et Minières, Bulletin, Section 2, 4 (1): 7-36. DARWIN, C. (1846). Geological Observations on South America. – 279 pp.; London (Smith Elder & Co.). DEFRANCE, M. J. L. (1816-1830): Zoologie, Conchyliologie et Malacologie, 1816-1830, Vol. 3, 492 + 174 pp. DEL VALLE, R. A., FOURCADE, N. H. & RINALDI, C. A. (1976): Sobre la presencia de Kitchinites darwini (STEINMANN) en el Cretácico superior de la Isla Vicecomodoro Marambio, Antártica. – Contribución Científica del Instituto Antártico Argentino, 195: 1-33. DOUBINGER, J. (1972): Évolution de la flore (pollen et spores) au Chili Central (Arauco), du Crétacé supérieur au Miocène. – Société de Biogéographie, 1972: 18-25. FATMI, A. N. & KENNEDY, W. J. (1999): Maastrichtian ammonites from Balochistan, Pakistan. – Journal of Paleontology, 73: 641-662. FORBES, E. (1846): Report on the Cretaceous fossil invertebrates from southern India, collected by Mr. Kaye and Mr. Cunliffe. – Transactions of the Geological Society of London, 2 (7): 97-174. FÖRSTER, R. & STINNESBECK, W. (1987): Zwei neue Krebse, Callianassa saetosa n. sp. und Homolopsis chilensis n. sp. (Crustacea, Decapoda) aus der Oberkreide Zentral-Chiles. – Mitteilungen der Bayerischen Staatssammlung für Paläontologie und historische Geologie, 27: 51-65. GABB, J. C. (1860): Description of Some New Species of Cretaceous Fossils from South America, in the Collection of the Academy. – Proceedings of the Academy of Natural Sciences, Philadelphia, 1860: 197-198. GASPARINI, Z. & BIRO, L. (1986). Osteopygis sp. (Reptilia, Testudines, Toxochelyidae) tortuga fósil de la Formación Quiriquina, Cretácico Superior, Sur de Chile. – Revista Geológica de Chile, 27: 85-90.
where the first specimen appears 3.5-5.0 above the base of the Belemnella lanceolata Zone, lower Maastrichtian (WARD & KENNEDY 1993). Hoploscaphites constrictus is known from the upper Maastrichtian of the Netherlands (VAN DER TUUK 1987) and central Europe (MACHALSKI 2005). In the Biscay region of France and Spain, in Germany, Denmark, France, southern Sweden, Poland, Austria and Belgium, the species is recorded from the upper Maastrichtian (WARD & KENNEDY 1993).
Acknowledgements We are grateful to the late LAJOS BIRÓ-BAGÓCZKY who collected the major part of the fossil material discussed here. We thank GERARDO FLORES MIRANDA (University of Concepción) and STEPHAN UNREIN (University of Karlsruhe) for preparation of ammonites and JOHARA BOURKE and CHRISTINA IFRIM for helpful comments on the manuscript. We further acknowledge the careful and detailed rewiews of Dr. JOHN JAGT and Dr. HERBERT SUMMESBERGER. Financial support to this project was donated by the Deutsche Forschungsgemeinschaft (STI 128/6).
References AGUIRRE, L., HERVÉ, F. & GODOY, E. (1972): Distribution of metamorphic facies in Chile. – Kristallinikum, 9: 7-19. ARKELL, W. J. (1950): A classification of Jurassic ammonites. – Journal of Paleontology, 24: 354-365. BANDEL, K. & STINNESBECK, W. (2000): Gastropods of the Quiriquina Formation (Maastrichtian) in Central Chile: Paleobiogeographic relationships and the description of a few new taxa. – Zentralblatt für Geologie und Paläontologie, 2000 (7-8): 757-788. BIRKELUND, T. (1993): Ammonites from the Maastrichtian White Chalk in Denmark. – Bulletin of the Geological Society of Denmark, 40: 33-81. BIRÓ, L. (1982a): Revisión y redefinición de los “Estratos de Quiriquina”, Campaniano-Maastrichtiano, en su localidad tipo en la Isla Quiriquina, 36º 35’ Lat. S, Chile, Sudamérica, con un perfil complementario en Cocholgüe. – Actas III Congreso Geológico Chileno, Concepción, A: 29-64. – (1982 b): Hoploscaphites constrictus (J. SOWERBY) en la Formación Quiriquina, Campaniano-Maastrichtiano, Región del Bío-Bío, Chile, Sudamerica. – Actas III Congreso Geológico Chileno, Concepción, A: 1-16. – (1982 c): Contribución al conocimiento de Naefia neogaeia WETZEL, Coloidea, en la Formación Quiriquina, Campaniano-Maastrichtiano, Región del Bío-Bío, Chile, Sudamerica. – Actas III Congreso Geológico Chileno, Concepción, A: 1-28. BLASCO DE NULLO, G., NULLO, F. & PROSERPIO, C. (1980): Santoniano-Campaniano. Estratigrafía y contenido Ammonitífero. Cuenca Austral. – Revista Asociación Geológica Argentina, 35 (4): 467-493. BOULE, M., LEMOINE, P. & THÉVENIN, A. (1906-1907): Paléontologie de Madagascar, III. Céphalopodes crétacés des environs de Diego-Suarez. – Annales de Paléontologie, 1: 173-192; 2: 1-56.
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at Cerralvo, Nuevo León, Northeastern Mexico. – Palaeontology, 47: 1575-1627. JONES, D. L. (1963): Upper Cretaceous (Campanian and Maastrichtian) ammonites from southern Alaska. – United States Geological Survey, Professional Papers, 432: 1-53. KENNEDY, W. J. (1986a): Campanian – Maastrichtian ammonites from northern Aquitaine, France. – Special Papers in Palaeontology, 36: 145. – (1986b): The ammonite fauna of the type Maastrichtian with a revision of Ammonites colligatus BINKHORST, 1861. – Bulletin de l'Institut Royal des Sciences Naturelles de Belgique, Sciences de la Terre, 56: 151-267. – (1986c): The ammonite fauna of the Calcaire à Baculites (Upper Maastrichtian) of the Cotentin Peninsula (Manche, France). – Palaeontology, 2: 25-83. KENNEDY, W. J., BILOTTE, M., LEPICARD, B. & SEGURA, F. (1996): Upper Campanian and Maastrichtian ammonites from the Petites-Pyrénées, southern France. – Eclogae geologicae Helvetiae, 79: 1001-1037. KENNEDY, W. J. & COBBAN, W. A. (1996): Maastrichtian ammonites from the Hornerstown Formation in New Jersey. – Journal of Paleontology, 70: 798-804 KENNEDY, W. J. & HANCOCK, J. M. (1993): Upper Maastrichtian ammonites from the Marnes de Nay between Gan and Rébénacq (Pyrénéés-Atlantiques), France. – Géobios, 26: 575-594. KENNEDY, W. J. & HENDERSON, R. A. (1992a): Heteromorph ammonites from the Upper Maastrichtian of Pondicherry, south India. – Palaeontology, 35: 693-731. – (1992b): Non-heteromorph ammonites from the Upper Maastrichtian of Pondicherry, South India. – Palaeontology, 35: 381-442. KENNEDY, W. J. & KLINGER, H. C. (1976): Cretaceous Faunas from Zululand and Natal, South Africa. The ammonite family Phylloceratidae. – Bulletin of the British Museum (Natural History), Geology, 27: 347380. – (1977): Cretaceous Faunas from Zululand and Natal, South Africa. The ammonite family Tetragonitidae Hyatt, 1900. – Annals of the South African Museum, 73: 149-197. – (1979): Cretaceous Faunas from Zululand and Natal, South Africa. The ammonite family Gaudryceratidae. – Bulletin of the British Museum (Natural History), Geology, 31: 121-173. – (2006): Cretaceous faunas from Zululand and Natal, South Africa. The ammonite family Pachydiscidae SPATH, 1922. – African Natural History, 2: 17-166. KENNEDY, W. J. & SUMMESBERGER, H. (1986): Lower Maastrichtian ammonites from Neuberg, Steiermark, Austria. – Beiträge zur Paläontologie von Österreich, 12: 181242. KILIAN, W. & REBOULD, P. (1909): Les Céphalopodes néocretacés des iles Seymour et Snowhill. Wiss. – Ergebnisse der Schwedischen Südpolar-Expedition (1901-1903), 3 (6): 1-75. KLINGER, H. C. & KENNEDY, W. J. (1993): Cretaceous faunas from Zululand and Natal, South Africa. The heteromorph ammonite genus Eubaculites SPATH, 1926. – Annals of the South African Museum, 102: 185-264.
GILL, T. (1871): Arrangement of the families of mollusks. – Smithsonian Miscellaneous Collections, 227: xvi + 49 pp. GROSSOUVRE, A. DE (1894): Recherches sur la Craie Supérieure, 2, Paléontologie. Les ammonites de la Craie Supérieure. – Mémoires pour Servir à l’Explication de la Carte Géologique Détaillée de la France. – 264 pp.; Paris (Imprimerie nationale). – (1901): Recherches sur la Craie Supérieure, part 1, no 2. Stratigraphie générale. – Mémoirs pour Servir à l’Explication de la Carte Géologique Détaillée de la France, 561-1013; Paris (Imprimerie nationale). HAUER, F. V. (1858). Ueber die Ammoniten der Gosauschichten. – Beitraege zur Palaeontologie von Oesterreich, 1: 7-14. – (1866). Neue Cephalopoden aus den Gosaugebilden der Alpen. – Sitzungsberichte der kaiserlichen Akademie der Wissenschaften Wien, mathematisch-naturwissenschaftliche Classe, 53: 300-308. HENDERSON, R. A. (1970): Ammonoidea from the Mata Series (Santonian – Maastrichtian) of New Zealand. – Special Papers in Palaeontology, 6: 1-82. HENDERSON, R. A., KENNEDY, W. J. & MCNAMARA, K. J. (1992): Maastrichtian heteromorph ammonites from the Carnarvon Basin, Western Australia. – Alcheringa, 16: 133-170. HENDERSON, R. A. & MCNAMARA, K. J. (1985): Maastrichtian non-heteromorph ammonites from the Miria Formation, Western Australia. – Palaeontology, 28: 35-88. HOEPEN, E. C. N. VAN (1921): Cretaceous Cephalopoda from Pondoland. – Annals of the Transvaal Museum, 8: 1-48. HOWARTH, M. K. (1958): Upper Jurassic and Cretaceous ammonite faunas of Alexander Land and Graham Land. – Falkland Islands Department of Survey, Scientific Reports, 21: 1-16. – (1965): Cretaceous Ammonites and Nautiloids from Angola. – Bulletin British Museum Natural History, Geology, 10 (10): 337-412. – (1966): Ammonites from the Upper Cretaceous of James Ross Island Group. – Bulletin of the British Antarctic Survey, 10: 55-69. HÜNICKEN, M. (1965): Algunos cefalópodos Supracretácicos del Río Turbio (Santa Cruz). – Universidad nacional de Córdoba, Serie de Ciencias Naturales, 52: 49-80. HÜNICKEN, M. A. & COVACEVICH, V. (1975): Baculitidae en el Cretácico Superior de la Isla Quiriquina, Chile, y consideraciones paleontológicas y estratigráficas. – Actas del Primer Congreso Argentino de Paleontología y Bioestratigrafía, Tucumán, Argentina, 2: 141-172. HUPÉ, L. H. (1854): Zoología. – In: GAY, C. (Ed.): Historia física y política de Chile, 8, 499 pp.; Paris. HYATT, A. (1889): Genesis of the Arietidae. – Smithsonian Contributions to Knowledge, 673: xi + 238 pp. – (1900): Cephalopoda. – In: ZITTEL, K. A. V. (Ed.): Textbook of Palaeontology. – viii + 306 pp.; London & New York (Macmillan). IFRIM, C., STINNESBECK, W. & LÓPEZ-OLIVA, J. G. (2004): Maastrichtian Cephalopods from the Méndez Formation
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Ammonites from the Maastrichtian Quiriquina Formation in central Chile
235
– (1947): A note on the Japanese Pachydiscinae. – Scientific reports of the Department of Geology. Faculty of Sciences, Kyushu University, 2: 34-46 [in Japanese]. – (1959). Upper Cretaceous Ammonites of California, Part II. – Memoirs of the Faculty of Science, Kyushu University, (D), Geology, Special Volume, 1, 1-172. MATSUMOTO, T. & YOSHIDA, S. (1979): A new gaudryceratid ammonite from eastern Hokkaido. – Transactions and Preceeding of the Palaeontological Society of Japan, 114: 65-76. MEEK, F. B. (1857): Description of new organic remains from the Cretaceous rocks of Vancouver Island. – Transaction of the Albany Institute, 4: 37-49. – (1876): A report on Kaikoura peninsula and Amuri Bluff. – Report of the Geological Survey of New Zealand Explorations, 9: 172-184. MORTON, S. G. (1834): Synopsis of the organic remains of the Cretaceous groups of the United States. Illustrated by nineteen plates, to which is added an appendix containing a tabular view of the Tertiary fossils discovered in America. – 88 pp.; Philadelphia (Key & Biddle). NISHIDA, M. (1985): A report of the botanical survey to Bolivia and Southern Chile (1983). – 36 pp.; Chiba (Chiba University, Faculty of Science). NISHIDA, M., OSHAWA, T. & NISHIDA, H. (1990): Anatomy and affinities of the petrified plants from the Tertiary of Chile ( VI ). – Botanical Magazine Tokyo, 103: 255-268. NOWAK, J. (1911): Untersuchungen über die Cephalopoden der oberen Kreide in Polen. II. Teil. Die Skaphiten. – Bulletin de l`Academie des Sciences de Cracovie, Classe des sciences Mathematiques et Naturelles, (B), Sciences Naturelles: 547-589. ODIN, G. S. (1996): Definition of a Global Boundary Stratotype Section and Point for the Campanian/Maastrichtian Boundary. – Bulletin de l´Institut Royal des Sciences Naturelles de Belgique, Sciences de la Terre, Supplément, 66: 17-111 OLIVERO, E. B. (1984): Nuevos ammonites Campanianos de la Isla James Ross, Antartida. – Ameghiniana, 21 (1): 53-84. OLIVERO, E. B. & ZINSMEISTER, W. J. (1989): Large heteromorph ammonites from the Upper Cretaceous of Seymour Island, Antarctica. – Journal of Paleontology, 63: 626-636. ORBIGNY, A. DE (1840-1842): Paéontologie française; Terrains Crétacés. 1. Cephalopodes. – 1-120 (1840), 121-430 (1841), 431-662 (1842); Paris. – (1842): Voyage dans l’Amérique méridionale 18261833, tome 3 (3-4). – 289 + 188 pp.; Paris. – (1847) Géologie (Paléontologie), Atlas de Géologie. – In: DUMONT D’URVILLE, M. J. (Ed.): Voyage au Pol Sud et dans l’Océanie sur les corvettes l’Astrolabe et la Zélée, 1838-40; Paris. – (1850): Prodrome de Paléontologie stratigraphique universelle des animaux mollusques et rayonnées, 2, 428 pp.; Paris (Masson). PARADA, M. A., LÓPEY-ESCOBAR, L., OLIVEROS, V., FUENTES, F., MORATA, D., CALDERÓN, M., AGUIRRE, L., FÉRAUD, G., ESPINOZA, F., MORENO, H., FIGUEROA, O., MUNOZ ˜ -BRAVO, J., TRONCOSO-VÁSQUEZ, R. & STER, C. R. (2007): Andean Magmatism. – In: MORENTO, T. &
KLINGER, H. C. & KENNEDY, W. J. (2001): Stratigaphic and geographic distribution, phylogenetic trends and general comments on the ammonite family Baculitidae GILL, 1871 (with an annotated list of species referred to the family). – Annals of the South African Museum, 107: 1-290. KLINGER, H. C., KENNEDY, W. J., LEES, J. A. & KITTO, S. (2001): Upper Maastrichtian ammonites and nannofossils and a Palaeocene nautiloid from Richards Bay, Kwa-Zulu, South Africa. – Acta Geologica Polonica, 51: 273-291 KOSSMAT, F. (1895): Untersuchungen über die Südindische Kreideformation. Erster Theil. – Beiträge zur Paläontologie Österreich-Ungarns und des Orients, 9: 97-203. – (1897): Untersuchungen über die südindische Kreideformation. Zweiter Theil. – Beiträge zur Paläontologie Österreich-Ungarns und des Orients, 11: 1-46. LAMARCK, J. B. (1799): Prodrome d’une nouvelle classification des coquilles. – Mémoires du Muséum d’Histoire Naturelle, 63-90; Paris. – (1801): Système des animaux sans vertèbres. – vii + 432 pp.; Paris (Déterville). – (1822): Historie naturelle des animaux sans vertèbres, 7: 711 pp.; Paris (Verdière). LAHSEN, A. & CHARRIER, R. (1972): Late Cretaceous Ammonites from Seno Skyring-Strait of Magellanes Province, Chile. – Journal of Paleontology, 46/4: 520532. LAMBRECHT, K. (1929): Neogeornis wetzeli n. gen. n. sp., der erste Kreidevogel der südlichen Hemisphäre. – Paläontologische Zeitschrift, 11: 121-129. LI, L., KELLER, G. & STINNESBECK, W. (1999): The late Campanian and Maastrichtian in northwestern Tunisia: palaeoenvironmental inferences from lithology, macrofauna and benthic foraminifera. – Cretaceous Research, 20: 231-252. MACELLARI, C. E. (1986): Late Campanian – Maastrichtian ammonite fauna from Seymour Island (Antarctic Peninsula). – Memoirs of the Paleontological Society, 18: 1-55. MAEDA, S., FULLER, R. C., CORVALÁN-DIAZ, J., TAZKE, H. & KAWABE, T. (1981): On Pacitrigonia hanetiana from the Quiriquina Formation, Quiriquina Island, Chile. – Paleontological Studies on the Andes, 2; Chiba (Geological Laboratory, Faculty of Science, Chiba University). MACHALSKI, M. (2005): Late Maastrichtian and earliest Danian scaphitid ammonites from central Europe: Taxonomy, evolution, and extinction. – Acta Palaeontologica Polonica, 50 (4): 653-695. MARSHALL, P. (1917): Geology of the central Kaipara. – Transactions of the New Zealand Institute, 49: 433-450. – (1926): The Upper Cretaceous ammonites of New Zealand. – Transactions and Proceedings of the New Zealand Institute, 56: 129-210. MATSUMOTO, T. (1938): Zelandites, a genus of Cretaceous Ammonite. – Japanese Journal of Geology and Geography, 15: 137-148. – (1942): A short note on the Japanese Phylloceratidae. – Proceedings of the Imperial Academy Tokyo, 18: 674676.
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236
C. Salazar et al.
WARD, P. D. & KENNEDY, W. J. (1993). Maastrichtian ammonites from the Biscay Region. – The Paleontological Society, Memoirs, 34: 1-58. WELLER, S. (1903): The Stokes collection of Antarctic fossils. – Journal of Geology, 11 (4): 413-419 WETZEL, W. (1930): Die Quiriquina-Schichten als Sediment und paläontologisches Archiv. – Palaeontographica, 73: 49-104. – (1960): Nachtrag zum Fossilarchiv der Quiriquina Schichten. – Neues Jahrbuch für Geologie und Paläontologie, Monatshefte, 1960: 439-446. WIEDMANN, J. (1962): Unterkreide-Ammoniten von Mallorca. 2. Lieferung: Phylloceratina. – Abhandlungen der Mainzer Akademie der Wissenschaften, mathematischnaturwissenschaftliche Klasse, 1963: 141-264. – (1966): Stammesgeschichte und System der posttriadischen Ammonoideen, ein Überblick. – Neues Jahrbuch für Geologie und Paläontologie, Abhandlungen, 125: 49-79; 127: 13-82. WILCKENS, O. (1904): Revision der Fauna der Quiriquina Schichten. – Neues Jahrbuch für Mineralogie, Geologie und Paläontologie, Beilage-Band, 18: 181-284. WOODS, H. (1906): The Cretaceous fauna of Pondoland. – Annals of the South African Museum, 4: 275-350. WRIGHT, C. W., CALLOMAN, J. H. & HOWARTH, M. K. (1996): Cretaceous Ammonoidea. – Treatise on Invertebrate Paleontology, Part L, Mollusca 4. – xx + 362 pp.; Lawrence & Boulder (Geological Society of America & University of Kansas press). YAZIKOVA, E. A. (1994): Maastrichtian ammonites and biostratigraphy of the Sakhalien and the Shikotan Islands, Far East Russia. – Acta Geologica Polonica, 44: 277303. ZINSMEISTER, W. J., FELDMANN, R. M., WOODBURNE, M. O. & ELLIOT, D. H. (1989): Latest Cretaceous/earliest Tertiary transition on Seymour Island, Antarctica. – Journal of Paleontology, 63: 731-738. ZITTEL, K. A. V. (1884): Cephalopoda. – In: ZITTEL, K. A. V. (Ed.): Handbuch der Paläontologie, 1 (Abteilung 2, Lieferung 3), 329-522; München & Leipzig (Oldenbourg). – (1895): Grundzüge der Palaeontologie (Palaeozoologie). – VII + 972 pp.; München & Leipzig (Oldenbourg).
GIBBONS, W. (Eds.): The Geology of Chile, 115-146; London (The Geological Society of London). PÉREZ D’A., E & REYES, B. R. (1978): Las Trigonias del Cretácico superior de Chile y su valor estratigráfico. – Boletín de Investigaciones geológicas, 34: 67 pp. PHILIPPI, R. A. (1887): Die tertiären und quartären Versteinerungen von Chile. – 266 pp.; Leipzig (Brockhaus). SALFELD, H. (1924): Die Bedeutung der Konservativstämme für die Stammesentwicklung der Ammonoideen. – 16 pp.; Leipzig. SEUNES, J. (1890): Recherches géologiques sur les terrains sécondaires et l’Eocène inférieur de la région souspyrénéenne du sud-ouest de la France (Basses-Pyrénées et Landes). – 250 pp.; Paris (Dunod). SHIMIZU, S. (1934): Ammonites. – In: SHIMIZU, S. & OBATA, T. (Eds.): Cephalopoda. Iwanami’s lecture series of Geology and Palaeontology. – 137 pp.; Tokyo [in Japanese]. – (1935): The Upper Cretaceous cephalopods of Japan, Part 1. – Journal of the Shanghai Science Institute, 2 (2): 159-226. SOWERBY, J. (1817): The Mineral Conchology of Great Britain, 2; London (published by the author). SPATH, L. F. (1922): On the Senonian ammonite fauna of Pondoland. – Transactions of the Royal Society of South Africa, 10: 113-148. – (1926): On new ammonites from the English Chalk. – The Geological Magazine, 3: 77-83. – (1927): Revision of the Jurassic cephalopod fauna of Kachh (Cutch), part 1. – Memoirs of the Geological Survey of India, Palaeontologica Indica (New Series), 9: 1-71. – (1953): The Upper Cretaceous Cephalopod fauna of Graham Land. – Falkland Island Dependencies Survey, Science Reports, 3: 1-60. STEINMANN, G. (1895): Die Cephalopoden der QuiriquinaSchichten. – Neues Jahrbuch für Mineralogie, Geologie und Paläontologie, 10: 64-94. STEINMANN, G., DEECKE, W. & MÖRICKE, W. (1895): Das Alter und die Fauna der Quiriquina Schichten in Chile. – Neues Jahrbuch für Mineralogie, Geologie und Paläontologie, 10: 1-118. STINNESBECK, W. (1986). Zu den faunistischen und palökologischen Verhältnissen in der Quiriquina Formation (Maastrichtium) Zentral-Chiles. – Palaeontographica, (A), 194: 99- 237. – (1996): Ammonite extinctions and environmental changes across the Cretaceous-Tertiary boundary in central Chile.. – In: MCLEOD, N. & KELLER, G. (Eds.): Cretaceous-Tertiary Mass Extinctions: Biotic and Environmental Changes, 289-302; New York (Norton). STOLICZKA, F. (1866): The fossil cephalopoda of the Cretaceous rocks of southern India (Ammonitidae). – Memoirs of the Geological Survey of India, Palaeontologica Indica, 41-216. TORRES, T. & BIRÓ, L. (1986): Xilotomía de Coníferas fósiles de la Isla Quiriquina, Chile. – Comunicaciones, 37: 65-80. VAN DER TUUK, L. A. (1987): Scaphitidae (Ammonoidea) from the Upper Cretaceous of Limburg, the Netherlands. – Paläontologische Zeitschrift, 61: 57-79.
Manuscript received: January 19th, 2009. Revised version accepted by the Stuttgart editor: June 2nd, 2009. Addresses of the authors: CHRISTIAN SALAZAR, Prof. Dr. WOLFGANG STINNESBECK Institut für Geowissenschaften, Universität Heidelberg, INF 234, 69120 Heidelberg, Germany; e-mails:
[email protected];
[email protected]. Dr. LUIS ARTURO QUINZIO-SINN, Departamento Ciencias de la Tierra, Universidad de Concepción, 160 C Concepción, Chile; e-mail:
[email protected]
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